soils of central and northern new brunswick

SOILS OF
CENTRAL AND NORTHERN NEW BRUNSWICK
New Brunswick
Soil Survey Report No. 12
Research Branch - Potato Research Centre - Fredericton New Brunswick
2005
Agriculture and
Agri-Food Canada
Agriculture et
Agroalimentaire
Canada
Canada
SOILS OF
CENTRAL AND NORTHERN NEW BRUNSWICK
New Brunswick Soil Survey Report No. 12
H. W. Rees, S. H. Fahmy, C. Wang and R. E. Wells
Potato Research Centre
Agriculture and Agri-Food Canada
Fredericton, New Brunswick
PRC Contribution No. 05-01
(Map sheet)
Agriculture and Agri-Food Canada
Research Branch
2005
Copies of this publication are available from:
Potato Research Centre, Agriculture and Agri-Food Canada
P. O. Box 20280, 850 Lincoln Road,
Fredericton, N ew Bru nsw ick, E3B 4Z7
New Brun swick Department of Agriculture, Fisheries and Aquaculture
Box 6000, Lincoln Road,
Fredericton, New Brunswick, E3B 5H1
Electron ic cop ies of th is pub lication an d dig ital ma ps ar e availab le
for downloading free of charge from the Agriculture and Agri-Food Canada
web site of the Can adian Soil Information S ystem (Can SIS) at:
http://sis.agr.gc.ca/c ansis
Correct citatio n as follow s:
Rees, H. W ., Fahmy, S. H., W ang, C. and W ells, R. E. 2005 . Soils of Central and No rthern New Brunsw ick.
Potato Research Centre, Research Branch, Agriculture and Agri-Food Canada, Fredericton, N. B. 137 pp
with map.
iii
CONTENTS
ACKN OW LEDGM ENTS. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . vii
SUMM ARY. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . viii
INTRODUCTION. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
1
PART 1. GENERAL DESCRIPTION OF THE AR EA.. . . . . . .
L o c a t io n a n d e x te n t . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Land use. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
F o r e s tr y . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
A g r ic u l tu r e . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
M in in g . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
R e c r e a tio n . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
L a n d o w n e r sh ip . . . . . . . . . . . . . . . . . . . . . . . . . .
P h y s io g r a p h y , to p o g r a p h y , d r a in a g e a n d b e d ro c k g e o lo g y
Climate. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
A t m o s p h e r i c c li m a t e . . . . . . . . . . . . . . . . . . . . . .
S o i l c li m a t e . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
V e g e ta tio n . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
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3
3
3
3
4
4
4
5
5
8
8
9
9
PART 2. SOIL FORMATION AND CLASSIFICATION. . . . . . .
S ur fic ial g eo log y.. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
S oil p ar en t m ate ria ls . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
M i n e r a l so i ls . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
O r g a n i c s o i l s. . . . . . . . . . . . . . . . . . . . . . . . . . . . .
So il develop m ent and soil form ing factors. . . . . . . . . . . . .
S o i l p r o f il e . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
S y s te m o f so il c la s s if ic a tio n . . . . . . . . . . . . . . . . . . . . . . . .
S o i l O r d e r s in c e n tr a l a n d n o r th e n N e w B r u n s w i c k . . . . . .
B r u n i s o l ic S o i ls . . . . . . . . . . . . . . . . . . . . . . . . . . .
G l e y s o l ic S o i ls . . . . . . . . . . . . . . . . . . . . . . . . . . .
L u v i s o l ic S o i ls . . . . . . . . . . . . . . . . . . . . . . . . . . . .
O r g a n i c S o i ls . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Po dzolic Soils . . . . . . . . . . . . . . . . . . . . . . . . . . . .
R e g o s o l ic S o i ls . . . . . . . . . . . . . . . . . . . . . . . . . . .
I m p a c t o f a g r ic u ltu r e o n so il c la s s if ic a tio n . . . . . . . . . . . . .
R e l a tio n s h ip b e tw e e n s o il c la s s if ic a tio n a n d s o il m a p p in g .
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11
11
11
11
12
13
14
15
16
16
16
16
16
16
19
20
20
PART 3. SOIL MAPPING METHODOLOGY.. . . . .
O ffic e m eth od s.. . . . . . . . . . . . . . . . . . . . . . . . .
F ield m eth od s.. . . . . . . . . . . . . . . . . . . . . . . . . .
M ap sy m bo l. . . . . . . . . . . . . . . . . . . . . . . . . . .
Land types . . . . . . . . . . . . . . . . . . . . . .
S o i l c o r r e l a ti o n w i th e s t a b l is h e d s o i l c o n c e p t s .
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21
21
21
22
27
27
KEY AND GENERAL DESCRIPTION.
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31
31
31
31
35
37
38
40
42
44
47
PART 4. SOIL ASSOCIATION IDENTIFICATION
K e y t o s o i l a s s o c i a t io n p a r e n t m a t e r ia l s . . . . .
S o i l a s so c ia tio n g e n e ra l d e s c rip tio n . . . . . . . .
A c a d ie S i d in g A s s o c ia tio n . . . . . . . . .
B ar rie au -B uc tou ch e A ss oc iatio n.. . . .
B elld un e R ive r A ss oc iatio n.. . . . . . . .
B i g B a l d M o u n ta in A s s o c ia tio n . . . . .
B o s t o n B r o o k A s s o c ia tio n . . . . . . . . .
C a r i b o u A s s o c ia tio n . . . . . . . . . . . . . .
C a r l eto n A s s o c ia tio n . . . . . . . . . . . . .
C a t a m a r a n A s s o c ia tio n . . . . . . . . . . . .
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iv
G a g e to w n A s s o c ia tio n . . . . . . .
G ra nd F alls A ss oc iatio n.. . . . .
G uim on d R ive r A ss oc iatio n.. .
H olm es ville A ss oc iatio n.. . . . .
In ter va l A ss oc iatio n.. . . . . . . .
Ja cq ue t R ive r A ss oc iatio n.. . . .
Ju nip er A ss oc iatio n.. . . . . . . . .
L av illette A ss oc iatio n.. . . . . . .
L o n g L a k e A s s o c ia tio n . . . . . . .
M alis ee t A ss oc iatio n.. . . . . . . .
M cG ee A ss oc iatio n.. . . . . . . . .
M un iac A ss oc iatio n.. . . . . . . . .
N iga do o R ive r A ss oc iatio n.. . .
P ar lee ville A ss oc iatio n.. . . . . .
P op ple D ep ot A ss oc iatio n.. . . .
R ee ce A ss oc iatio n.. . . . . . . . . .
R i c h ib u c to A s s o c ia tio n . . . . . .
R i v e r b an k A s s o c ia tio n . . . . . . .
R o g e r s v ille A s s o c ia tio n . . . . . .
S ton y B ro ok A ss oc iatio n.. . . . .
S t. Q ue ntin A ss oc iatio n.. . . . . .
S u n b u r y A s s o c ia tio n . . . . . . . .
T eta go uc he A ss oc iatio n.. . . . .
T eta go uc he F alls A ss oc iatio n..
T hib au lt A ss oc iatio n.. . . . . . . .
T r a c a d ie A s s o c ia tio n . . . . . . . .
T ua do ok A ss oc iatio n.. . . . . . . .
V iole tte A ss oc iatio n.. . . . . . . .
L and type s. . . . . . . . . . . . . . . . . . . . . . .
S a l t M a r sh . . . . . . . . . . . . . . . .
San d D unes. . . . . . . . . . . . . . .
W a ter. . . . . . . . . . . . . . . . . . . .
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PART 5. ELECTRONIC DATA FILES. . . . . . .
F ile s tru ctu re .. . . . . . . . . . . . . . . . . . . . . . .
P ro jec t F ile (P F ).. . . . . . . . . . . . . .
P oly go n a ttrib ute tab le file (P A T )..
S oil M ap U nit F ile (S M U F ).. . . . .
S oil N am e F ile (S N F ).. . . . . . . . . .
S oil L ay er F ile (S L F ).. . . . . . . . . .
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103
103
103
104
104
104
105
PART 6. INTERPRETATIONS - SINGLE FACTOR AND GENERAL AGRICULTURE AND
FORESTRY RATINGS . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
S i n g le - fa c to r so il m a p u n it c o n d itio n s . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
C a n a d a L a n d I n v e n to r y C l as s if ic a tio n . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
S oil c ap ab ility c las sific atio n f or ag ric ultu re .. . . . . . . . . . . . . . . . . . . . . . . . . .
L a n d cap a b ility clas s ificatio n fo r fore s try . . . . . . . . . . . . . . . . . . . . . . . . . . . .
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107
107
110
110
111
REFERENCES . . . . . . . . . . . . . . . . . . . . . .
G LO SSA RY - G EN ER AL TER M S. . . . . . .
GLOSSARY - ROC K TYPES . . . . . . . . . . .
APPENDIX - COM M ON AND SCIENTIFIC
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127
129
135
137
.................
.................
.................
NAM ES OF TREES.
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49
51
53
55
57
59
61
63
65
67
68
71
73
74
76
77
80
82
84
85
87
89
91
92
94
96
98
100
102
102
102
102
v
LIST OF TABLES AND ILLUSTRATIONS
TABLES
1.
2.
3.
4.
5.
S o i l a s s o c ia t io n m e m b e r s o f t h e ce n t ra l a n d n o r th e r n N e w B r u n s w i c k m a p a r e a c la s s if ie d
ac co rd ing to th e C an ad ian S ys tem of S oil C las sific atio n .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
S oil m ap pin g le ge nd .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
C or re latio n o f so il as so cia tion s m ap pe d in ce ntr al a nd no rth er n N ew B ru ns w ick w ith
es tab lish ed so il se rie s .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
K ey to s oil a ss oc iatio n p ar en t m ate ria ls in the ce ntr al a nd no rth er n N ew B ru ns w ick m ap ar ea ..
S ele cte d in ter pr eta tion s o f so il m ap un its . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
18
23
28
32
112
FIGURES
1.
2.
3.
4.
5.
6.
7.
8.
9.
10 .
11 .
12 .
13.
14 .
15 .
16 .
17.
18 .
19 .
20 .
21 .
22 .
23 .
24 .
25 .
26 .
27 .
28.
29.
30 .
31.
32 .
33 .
34 .
35.
36 .
37 .
38.
39 .
40 .
A r e a s o f N e w B r u n s w i c k fo r w h i c h re c o n n a is s a n ce s o il s u rv e y s h a v e
N e w B r u n s w i c k S o il S u r v e y . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
P hy sio gr ap hic re gio ns of the su rv ey ar ea .. . . . . . . . . . . . . . . . . . . . .
B ed ro ck ge olo gy of the su rv ey ar ea .. . . . . . . . . . . . . . . . . . . . . . . . . .
C l i m a t ic z o n e s w i th i n th e s u r v e y a re a . . . . . . . . . . . . . . . . . . . . . . . .
F or es t reg ion s a nd se ctio ns w ithin the su rv ey ar ea .. . . . . . . . . . . . . . .
D iag ra m m atic ho riz on pa ttern s o f v ar iou s s oil p ro files .. . . . . . . . . . .
L oc atio n o f m ap pe d A ca die S idin g s oils . . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d B ar rie au -B uc tou ch e s oils . . . . . . . . . . . . . . . . . .
W ell d ra ine d B ar rie au -B uc tou ch e s oil p ro file . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d B elle du ne R ive r so ils . . . . . . . . . . . . . . . . . . . . .
W ell d ra ine d B elle du ne R ive r so il pr of ile . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d B ig B ald M ou nta in s oils . . . . . . . . . . . . . . . . . .
B i g B a l d M o u n t a in s o i l a s s o c i a ti o n l a n d s c a p e s h o w i n g “ t o r s ” . . . . . .
W ell d ra ine d B ig B ald M ou nta in s oil p ro file . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d B os ton B ro ok so ils . . . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d C ar ibo u s oils . . . . . . . . . . . . . . . . . . . . . . . . . . .
W e l l d r a i n e d C a r i b o u s o i l p r o f il e , v e n e e r p h a s e . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d C ar leto n s oils . . . . . . . . . . . . . . . . . . . . . . . . . . .
W ell d ra ine d C ar leto n s oil p ro file . . . . . . . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d C ata m ar an so ils . . . . . . . . . . . . . . . . . . . . . . . . .
M od er ate ly w ell d ra ine d C ata m ar an so il pr of ile . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d G ag eto w n s oils . . . . . . . . . . . . . . . . . . . . . . . . . .
R ap idly dr ain ed G ag eto w n s oil p ro file . . . . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d G ra nd F alls so ils . . . . . . . . . . . . . . . . . . . . . . . .
R ap idly dr ain ed G ra nd F alls so il pr of ile . . . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d G uim on d R ive r so ils . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d H olm es ville so ils . . . . . . . . . . . . . . . . . . . . . . . .
W e l l d r a in e d H o l m e s v i ll e s o il p ro f il e , c u l ti v a te d . . . . . . . . . . . . . . . .
P r o v in c ia l s o il b a d g e . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d I nte rv al s oils . . . . . . . . . . . . . . . . . . . . . . . . . . .
I n te r v a l s o il a s so c ia tio n la n d s c a p e . . . . . . . . . . . . . . . . . . . . . . . . . . .
Im pe rfe ctly dr ain ed In ter va l so il pr of ile . . . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d J ac qu et R ive r so ils . . . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d J un ipe r so ils . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ju n i p e r so i l as s o ciatio n lan d s c ap e an d surfa c e s tone s /bo ulde rs . . . . .
W ell d ra ine d J un ipe r so il pr of ile . . . . . . . . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d L av illette so ils . . . . . . . . . . . . . . . . . . . . . . . . . .
L a v i lle tte s o il a s so c ia tio n la n d s c a p e . . . . . . . . . . . . . . . . . . . . . . . . . .
L oc atio n o f m ap pe d L on g L ak e s oils . . . . . . . . . . . . . . . . . . . . . . . . .
W ell d ra ine d L on g L ak e s oil p ro file . . . . . . . . . . . . . . . . . . . . . . . . . .
b e e n p u b lis h e d b y
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1
6
7
9
10
17
31
35
36
37
38
39
39
39
41
42
43
45
46
47
48
49
50
51
52
53
55
56
56
57
58
58
59
61
61
62
63
64
65
66
vi
FIGURES cont’d
41 .
42 .
43 .
44 .
45 .
46 .
47 .
48 .
49 .
50 .
51 .
52.
53 .
54 .
55 .
56 .
57 .
58 .
59 .
60 .
61 .
62 .
63 .
64 .
65 .
66 .
67 .
68 .
69 .
70 .
71 .
L oc atio n o f m ap pe d M alis ee t so ils . . . . . . . . . . . .
L oc atio n o f m ap pe d M cG ee so ils . . . . . . . . . . . . .
W ell d ra ine d M cG ee so il pr of ile . . . . . . . . . . . . .
L oc atio n o f m ap pe d M un iac so ils . . . . . . . . . . . . .
L oc atio n o f m ap pe d N iga do o R ive r so ils . . . . . . .
W ell d ra ine d N iga do o R ive r so il pr of ile . . . . . . . .
L oc atio n o f m ap pe d P ar lee ville so ils . . . . . . . . . .
L oc atio n o f m ap pe d P op ple D ep ot s oils . . . . . . . .
L oc atio n o f m ap pe d R ee ce so ils . . . . . . . . . . . . . .
W ell d ra ine d R ee ce so il pr of ile . . . . . . . . . . . . . .
L oc atio n o f m ap pe d R ich ibu cto so ils . . . . . . . . . .
W e l l d r a i n e d R i c h i b u c t o s o i l p r o f i le , v e n e e r p h a s e
L oc atio n o f m ap pe d R ive rb an k s oils . . . . . . . . . .
R ap idly dr ain ed R ive rb an k s oil p ro file . . . . . . . . .
L oc atio n o f m ap pe d R og er sv ille s oils . . . . . . . . . .
L oc atio n o f m ap pe d S ton y B ro ok so ils . . . . . . . . .
M od er ate ly w ell d ra ine d S ton y B ro ok so il pr of ile
L oc atio n o f m ap pe d S t. Q ue ntin so ils . . . . . . . . . .
L oc atio n o f m ap pe d S un bu ry so ils . . . . . . . . . . . .
W ell d ra ine d S un bu ry so il pr of ile . . . . . . . . . . . . .
L oc atio n o f m ap pe d T eta go uc he so ils . . . . . . . . .
L oc atio n o f m ap pe d T eta go uc he F alls so ils . . . . .
W ell d ra ine d T eta go uc he F alls so il pr of ile . . . . . .
L oc atio n o f m ap pe d T hib au lt so ils . . . . . . . . . . . .
W ell d ra ine d T hib au lt so il pr of ile . . . . . . . . . . . . .
L oc atio n o f m ap pe d T ra ca die so ils . . . . . . . . . . . .
P oo rly dr ain ed T ra ca die so il pr of ile . . . . . . . . . . .
L oc atio n o f m ap pe d T ua do ok so ils . . . . . . . . . . . .
W ell d ra ine d T ua do ok so il pr of ile . . . . . . . . . . . .
L oc atio n o f m ap pe d V iole tte s oils . . . . . . . . . . . .
M od er ate ly w ell d ra ine d V iole tte s oil p ro file . . . .
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67
69
70
71
73
73
75
76
78
79
80
81
82
83
84
86
87
88
89
90
91
92
93
94
95
97
97
98
99
100
101
v ii
ACKNOWLEDGMENTS
T h e a u th o r s e x te n d s p e cia l r e co g nitio n to th e
fo llo w in g : D . K e y s , fo r m e r ly N e w B r u n s w i c k
D ep ar tm e n t o f N a t u r a l R e s o u r c e s , M i n e r a l
R e s o u r c e s B r a n c h , P e atlan d In v en to ry S e c tio n , w h o
p r o v id e d inf or m atio n o n th e o rg an ic s o ils o f t h e ar e a ;
B . M . S m ith ( re tired ), N ew B ru ns w ick D ep ar tm e n t
o f N a tu r a l R e s o u r c e s, F o r e s t M a n a g e m e n t B r a n c h ,
w h o su pp lie d d a t a f r o m t h e N e w B r u n s w i c k F o r e s t
I n v e n to r y ; s ta f f o f th e A n a l y ti c al S e rv ice L ab o ra tory
o f A gr icu ltu r e C a n a d a ' s L a n d R e s o u r c e R e s e a r c h
C e n t r e ( n o w A g r ic u ltu re an d A g ri-F o o d C ana da ’s
E ast e r n C e r e a l a n d O ils e e d R e s e a rc h C e n t re ) , w h o
c o n d u c t e d s o il c h e m i c al an d p hy sic al a na lys es in
s up p o r t o f fie ld w o r k ; a n d th e m a n y o th e r s w h o
a s s is te d in f ie ld w o r k , la b o r a to r y a n aly s e s , a n d
dr af ting .
L a bo ra tory a n d o f f ic e s p a c e w e r e p ro v id e d b y
A gric ulture C a n a d a 's F r e d er ic to n R e s e a r c h S t a tio n
( n o w A g r i c u ltu r e a nd A gr i-F oo d C an ad a’ s P ota to
R es ea rc h C en tre ).
T h e s o il m a p a n d i ll u st ra t io n s w e r e p re p a r e d b y J a n e t
C u m m in g s an d A nd ré V illen eu ve , C an ad ia n S oil
I n fo r m a t io n S ys tem (C an S IS ), E as ter n C er ea l a n d
O i ls e e d R es ea rc h C en tre , A g r ic u ltu r e an d A g r i -F o o d
C a n a d a , O t ta w a .
A c k n o w l e d g m e n t is m a d e to G a r y P a t te r so n , A c t in g
N a t io n a l So il C orre la tor, A gric ulture a n d A g r i -F o o d
C a n a d a , T ru ro , N ov a S co tia, fo r h is t ec h n i c a l r e v ie w
of the m an us cr ipt.
v iii
SUMMARY
The area surveyed encompasses most of central and northern
New Brunswick, occupying 2.79 million ha (6.89 million ac)
or approxim ately one third o f the total land area of the
province. T his includes all of Restigouche and Gloucester
counties, most of No rthumberland co unty, the northern half
of Yo rk county and the northeast tip o f Carleton co unty. The
survey area occupies parts of the Maritime Plain, New
Brunswick Highlands, Chaleur Uplands and Notre Dame
Mo untains of the Appalachian Region. The level to gently
undulating landsc apes of the M aritime P lain alon g the G ulf
of St. Lawrence are strongly contrasted by the rugged, more
hilly nature of the Highlands, Uplands and M ountains,
which reach elevations of in excess of 80 0 m. T he area is
drained mainly by tributaries of the Saint John River to the
west, the Miramichi River to the east and the Restigouche
and Nep isiguit Rivers to the north.
Despite its mid-latitude maritime location, the survey area
has a modified continental climate with prevailing westerly
winds blowing offshore, resulting in a more extre me climate
similar to inland Canad a. Within the survey area two
influences dominate the climate - the moderating effect of
the Atlantic Ocean along the eastern shore and the cooling
effect of increased elevations in central and northwestern
New Brunswick. Annual daily mean air temperature ranges
from 2.0 to 5.2 oC. The southern and eastern most areas have
the longest frost-free periods with in excess of 130 d ays
while in the central and northwestern regions the average
frost-free perio d is less than 90 days. Annual precipitation
ranges from 1000 to over 1200 mm per year, of which 280
to 380 cm (280 to 380 mm of water equivalent) occur as
snowfall. Mean annual soil temp erature varies fro m 2 to
8°C.
Bedrock geolo gy is relatively sim ple and uncomplicated in
the northeastern Maritime Plain portion of the survey area,
with 90% underlain by horizontal to gently dipping, Pennsylvanian age, sedimentary rocks, predominately gray-green
sandstone. The Chaleur U pland and Notre Dame M ountains
to the west are underlain by a mixture of vertically-standing
greywacke, slate, sand stone, limeston e and conglome rate
with minor volca nic roc ks of rhyo lite, trachyte a nd basaltic
flows. The M iramichi Highlands are underlain by a number
of bedrock types, with the northern p ortions consisting of
formations of silicic volcanic rocks, rhyolite, rhyoliteporphyry, silicic tuffaceous rocks and metamorphosed
equivalents, quartz and quartz-feldspar schist, with some
mafic volcanic flows. The southern portion is rich in
granites and granodiorites with argillaceous sedimentary
rocks, greywacke, quartz, conglomerate and minor
limestone, tuff and volcanic flows.
Central and northern New Brunswick includes parts of three
major forest regions - the Acadian, G reat La kes-St.
Lawrence and Boreal Forest Regions. Impeded draina ge in
the lowlands has lead to a prevalence of pure stands of black
spruce, red spruce, and balsam fir or mixed wood in which
these species are associated with eastern white pine, red
maple, trembling aspen, sugar maple, yellow birch, and
white birch. While the higher altitudes of the New
Brunswick Highlands section are dominated by coniferous
forests of balsam fir, black spruce, white spruce and white
birch, at lower altitudes, crests and upper slopes are forested
with sugar maple, yellow birch and beech; middle slopes
include a com pon ent of red and white spruce, eastern
hemlock and balsam fir; and lower slopes and depressions
support primarily coniferous stands of spruces, fir, eastern
white cedar and tamarack. The Chaleur Uplands are
similarly characterized by forests of sugar maple, beech and
yellow birch on the hill tops with balsam fir and spruce in
the valleys. In the northwest, the Notre Dam e Mo untains are
dominated by coniferous forest cover types of balsam fir,
black spruce and white spruce with some eastern white cedar
and white birch.
Forest production and forestry-related ac tivities constitute
the single largest land use. More than 90% of the area is
productive woodland, whereas less than 2% of the land base
is used for agricultural purposes. Most of the agricultural
activity in the survey area is scattered along the north shore
from Campb ellton and Dalhousie through Belledune and
Bathurst over to Caraquet and then south along the east
coast from Shippegan and Tracadie down to the
Newcastle-Chatham area, and somewhat inland along the
Miramichi River and its tributaries. Another area of
agricultural significance is the St. Quentin-Kedgwick area.
In general, farmlands occur in small parcels interspersed
between larger areas of forested land.
Soil parent materials vary widely but are dominated by icedeposited sediments. G laciers, which covered the entire
region during Wisconsin glaciation, scoured all preglacial
surfaces and su bseq uently deposited a man tle of glacial drift
of varying thickness. Thickness of the drift generally ranges
from less than 1 to 2.5 m . Of the glacial materials, thin
deposits consisting of less than 1 m of loamy-textured,
com pact, lodgment tills or slightly thicker 1 to 2 m of coarse
loamy-textured, loose, ablational till, are by far the most
abundant. The general direction of glacier movement was to
the southeast. Thus, texture, color and coarse fragment
lithology of lodgment tills closely resemble the underlying
bedrock or bedrock to the northwest. Ablation tills may
have a more wide-ranging lithological composition and
weaker ties to the underlying bedrock type. Excluding the
northern half of the Acadian Peninsula where reddish brown
tills are common, most tills are yellowish to olive brown or
grey. Relatively few glac iofluvial d epo sits are present.
Following deglaciation, the lowlands portion of the survey
ix
area was submerged by sea water. However, marine d epo sitions are confined to a narrow zone along the coastline. Bo th
fine- and coarse-textured marine sediments occur. Soil and
climatic conditions of the region promote paludification
(the formation of peat), especially in the lowlands portion.
Some bogs have attained thicknesses of more than 5 m.
Alluvial deposits, although associated to some degree with
most stream and river co urses, are restricted in are a.
Of the nine orders defined in The Canadian System of Soil
Classification, six are present in the study area: Brunisolic,
Gleysolic, Luviso lic, Organic, P odz olic, and Regosolic
orders. Podzo lization is the dominant soil-forming process.
W ell-drained Podzo ls dom inate the morainal tills in the
Upland and H ighland areas while imp erfectly drained Luvisols and poorly drained Gleysols do minate the mo rainal tills
on the M aritime P lain lowlands. Luvisolic d evelo pme nt in
these acidic materials is weak ly expre ssed. In general, the
strongest Luviso lic development is found in the marine clays
scattered along the coast.. Well- and imperfectly drained,
coarse-textured, marine and glaciofluvial deposits are also
Podzols. Their po orly drained counterparts are usually
Brunisols. Regosols are found on alluvial sites where
ongoing deposition disrupts horizon formation. Soils of the
Organic order are either deep accumulatio ns of poorly to
very poorly drained sphagnum, or thinner deposits of
mod erately decomposed sedg e-spha gnum or we ll
decomposed forest peats. They occur throughout the study
area but are most prominent in the Maritime Plain.
Reduced soil quality for biological growth as a result of low
fertility (cause d by a lack of available nutrients, high acidity,
and low exchange capacity), and adverse climate, prevails
throughout the survey area, as it does throughout most of
Atlantic Canada. Undesirable soil structure and low permeability, often resulting in excess soil moisture, are
inherent limitations in the compa ct lodgment tills. Slope
limitations occur throughout much of the upland and
highland areas. Exce ssive stoniness plagues the looser,
ablational tills. Low m oisture-holdin g capacity affects the
coarse-textured marine and glaciofluvial materials. The
more fertile alluvial deposits are subject to flooding. M ost
organic soils are conside red as nonprod uctive forest lands,
and their potential for agricultural development is, at best,
mod erate.
Interpretations for agriculture and forestry uses vary greatly
with soil material an d site co nditions. Alluvial deposits are
the best sources for topsoil. Sands are abundant along the
coast, but deposits are typically thin in nature. Gravel
reserves are scattered sparsely throughout the inland portion
of the survey area. Organic soils are potential sources of
horticu ltural and fuel pea t.
x
1
INTRODUCTION
Soil survey is "the whole procedure involved in making a
soil resource inventory. It includes the initial plan, the field
investigations, creating the legend, drawing the map,
describing and sa mpling the soils, analysing the samples,
writing the report and preparing the interpretations" (Mapping S ystems W orking Group , 198 1).
This repo rt is the twelfth in a series dealing with soils and
landscapes in New Brunswick (Fig. 1). The area is located
in central and northern New Brunswick. Soils were mapped
at a l:250 000 exploratory level, with the objectives of
providing an inventory of soil resources by showing their
distribution on a map and describing their characteristics and
limitations. Such base information is a prerequisite for
competent resource management and land use planning.
Information provided in this report was designed to be
multipu rpose in nature.
Initial soils mapping was conducted from 1978 to 19 81, and
the information was placed on open file. This publication
prese nts the comple ted results of the survey, consisting of
two co mpo nents-- the re port and the soil map.
The report is divided into six parts. Part 1 describes the
location and extent of the surveyed area, the present land
uses, and the natural resources - physiog raphy, topo graphy,
drainage, vegetation, climate, and bedrock geolo gy. Part 2
discusses soil formation and explains how soils are classified. It also outlines soil parent materials and modes of
deposition and summarizes soil development and the system
of classification used. Part 3 deals with soil mapping
procedures. Part 4 includes a key to soil association parent
materials and describes the m app ed so il associations in
terms of topographic conditions, material composition,
drainage, classification, and related soils. Part 5 outlines
how the data is stored in electronic files that allow for
greater ability to manipulate and apply the information in a
consistent and timely manner. Part 6 presents general
interpretations of the soil map units for agriculture and
forestry.
W hile the text of the report provides technical information
on soil and landsca pe pro perties and rates general
suitabilities of the mapped soils, the distribution (location
and extent) o f the vario us kinds of soils are displayed on a
1:300,000 scale line map located in the pocket on the inside
of the back cover of the report. A published map scale of
1:300,000 was used for logistical reasons - overall map size,
and the ability to present the entire map on one sheet. The
map includes a map legend which briefly summarizes soil
properties and landscape features typical of each mapped
soil asso ciation or land type.
Figure 1. Areas of New Brunswick for which reconnaissance
soil surveys have been published by New Brunswick Soil
Survey.
Information provided in this report is relevant for provincial,
regional and national land use planning,, but it should also
prove useful to urban developers, foresters, highway
engineers, land use planners, and interested memb ers of the
public, as well as to farmers, agricultural engineers, and
agrono mists.
Limitations to the use of the soils information conveyed by
the soil map and report must be app reciated. T he da ta
presented is generally only for soil materials to a depth of
one metre. Discussions on materials below 1 metre are
estimates based on occa sional field observations. Also, the
reliability and accuracy of this data is commensurate with a
1:250 000 map scale. B ecause of this exploratory scale of
mapping, significant areas o f soils that differ from the
identified dominant soils may be included in the map units.
Enlargement or “blowing up” of this map can cause a
serious misund erstand ing of the detail of mapping and can
result in erroneous interpretations. The inform ation in this
soil survey provides a preliminary definition or overview of
the general qualities of the different land areas within the
mapped area. It does not eliminate the need for on-site
investigation, testing and analysis before implementing any
intended use.
2
3
PART 1. GENERAL DESCRIPTION OF THE AREA
LOCATION AND EXTENT
The area surveyed enco mpa sses mo st of central and northern
New Brunswick. The location of the map area, with respect
to other p ublished soil survey re port map areas, is shown in
Fig. 1. More spec ifically its boundary runs east along the
New Brunswick - Quebec border to Chaleur Bay, south
along the Northumberland Strait coastline to M iramichi Ba y,
west along the Little SW M iramichi River to longitude 65 o
45 ', south to latitude 46 o 30', west to longitude 66 o 30', south
to latitude 46 o 00 ', west to the Nac kawic Stream , northwest
along the Nackawic Stream to longitude 67 o 22.5 ', north to
latitude 46 o 30', east to longitude 67 o 00', north to the
Victoria county line, northeast along the Victoria county line
to the York county line, northeast along the Y ork county
line to the Northumbe rland county line, northwest along the
Northumberland county line to the Restigouche county line,
and then northwest along the Restigouche county line to the
New Brunswick - Quebec border. This includes all of
Restigouche and Gloucester counties, m ost o f
Northumberland county, the northern ha lf of Yo rk county
and the northeast tip of Carleton county. It covers par ts of
the national topographic map-sheets (1:250,000 scale) for
Bathurst (21-P), Campb ellton (21-O), Edmund ston (21-N),
Matane (22 -B), Moncton (21 -I), and Wood stock (21-J).
The survey area occupies 2.79 million ha (6.89 million ac)
or approxim ately one third of the total land area of the
province. The principal centres of population within the area
are the cities of Bathurst (pop. 15,705) and Campbellton
(9,818), the towns of Cara quet (4,31 5), D alhousie (5,707),
Lameque (1,571), Newcastle (6,284), Shippagan (2,726) and
Tracad ie (2,45 2) and the m ajor villages o f Atholville
(1,694), Balmoral (1,823), Bas Caraquet (1,859 ), Beresford
(3,652), Charlo (1,603), Neguac (1,755), Petit Rocher
(1,860) and Saint Quentin (2,334).
LAND USE
Major land users within the survey area are forestry,
agriculture, urbanization, mining and recreation. Land use
status is summarized below:
Forest
Agriculture
Old Fields
Water
Open Wetlands
Occupied (cities, towns, airports, etc.)
Facilities (ro ads, p ower lines, etc.)
Source: Smith (1982).
92.9%
2.0%
0.8%
0.9%
1.9%
0.6%
0.8%
Forestry
Forested lands account for 9 2.9% of the survey area. Th is
represents in excess of 2.59 million ha. Of these forested
lands 93.4% is stocked, 3.9% is disturbed (planted, cut or
burnt) and 2.7% is nonproductive (Smith 1982). Average
volume of harvestable wood (greater than 12 cm dbh,
diameter at breast height or 4.5 ft above the forest floor)
varies from 50 to 125 cubic metres per hectare (Smith
1982). The coa stal lowlands around P oint V erte, B athurst,
Caraquet, Burnsville, Tabusintac and C hatham average only
50 to 90 m3/ha. The de pleted cond ition of these forests is
due to insect infestations (primarily spruce budworm),
disease, fire and mismanagement (high-grading, little or no
reforestation, etc.)
This area of northeastern New
Brunswick has experienced the most severe levels of annual
burn in the province. Mean annual burn is 0.43%, which
represents a fire rotation pe riod of about 230 years (W ein
and Moore, 1977.). In contrast to this, the central and
western uplands average 90 to 125 m 3 of merchantable wood
volume per hectare. The most prod uctive re gions w ithin this
area are aro und S tates B rook-M enneval in the northwest and
S e r p e n t i n e L a k e -T u a d o o k L a k e - M c K e n d r i c k
Lake-Hayesville-Coldstream-M illville in the sou thwest,
where average hectare yields are 110 to 125 m 3. Spruce
budworm infestations are a se rious p roblem, but their
control through aerial spray programs is probably more
successful than in settled areas where spraying was either
banned or less effective due to the sporadic pattern of
application. North central and northwestern New Brunswick
are also areas of low annual burn. Large fires have only
occurred recently, corresponding to improved access for tree
harvesting and recreation .
Softwoods pred ominate, esp ecially spruce and balsam fir,
with lesser amounts of jack pine, white pine, red pine and
cedar. Hardwoods, sugar maple, red maple, yellow birch,
white birch, ash, beech and poplar, make up 15 to 45% of
the forest community. (See the section on vegetation for a
more detailed account of species distribution.). However,
the total hardwood harvest is only about 10% of the total
wood fibre harvest, indicating that hardwood is being
significantly under-utilized.
W hile forest harvesting operations are for the most part
labor intensive, skidders and chainsa ws are increasingly
giving way to more highly mechanized systems (feller
bunchers, short wood harvesters, etc.). Most of the wood
fibre harvested is consumed by the pulp and paper indu stry.
Several pulp and paper mills are located within the study
area (Athoville, Dalhousie, Bathurst, Newcastle) and a
number in close proximity (Nackawic, Edmundston).
Products produced include kraft pulp, groundwood pulp,
sulphide pulp, container board and newsprint. There are
numerous sawmills operating within the area. Many of the
4
smaller mills are p ortab le or home-m ade and o perate
intermittently. However, there are also a number of larger
mills with annual production exceeding 3 million fbm (footboard-measure, equivalent to a piece of wood measuring 12"
x 12" square by 1" thick ). In addition to the pulpwood and
sawlogs, other softwood products include veneer logs,
"stud" logs, poles and cedar logs. Hardwood products
include venee r logs, sp oolw ood and fuelwood. Christmas
tree and maple syrup production are other wood land uses.
Although small in land area involved, they are important
assets in local econo mics.
In the southern portion of the survey area there is some
general farming in the Stanley-Williamsburg and Burtts
Corner-M illville areas. Dairy o perations are particularly
prevalent in the Burtts Corner-Millville area.
Agriculture
Agricultural land use within the study area accounts for
app roxim ately 2% of the total land area, representing some
55,800 ha of cleared land (Smith 1982). An additional 0.8%
or 21,000 ha is abandoned farmland consisting of old fields
reverting to forest. This indicates a 27 % reduction in
farmland, which is comparable to the provincial decline of
35% in total imp roved farm land o ver the perio d 1961 to
1981 (N. B. Department of Agriculture and Rural
Developm ent 198 1). Agricultural development is strongly
related to the land base. W ith the exception of the
Kedgwick-St. Quentin area, all of the central and
northwestern portions of the study area are completely
devoid of farmed land. Climatic, topo graphic and /or soil
conditions are too severe to permit agricultural
establishm ent. Undulating and gently rolling topography
coupled with more suitable soil parent materials (ie less
stony and rocky), have allowed for a successful agricultural
sector in the Kedgwick-St. Quentin vicinity, built around a
worked farmland base of about 8,00 0 ha. M ixed farming is
the norm , howe ver, some specialization has take n place in
potato production. Other field crops include hay, oats and
barley and minor amounts of mixed grain and corn.
Metallic mineral occ urrences are con centrated in the central
h i gh l a nd s p o r t i o n o f th e s t u d y a r e a f ro m
Campbellton-Bathurst south to Fredericton.
Hugh
zinc-copper-silver deposits were found near B athurst in
1952. They are presently being mined by Brunswick Mining
and Smelting Corporation Limited. A second operation,
Heath Steele M ines Limited, located northwest of
Newcastle, was closed down due to low world metal prices.
Other metallic mineral discoveries include gold, iron,
uranium, mang anese, cobalt, nickel, tin, tungsten, beryl and
flourite.
Most of the agricultural activity in the survey area is
scattered along the north shore from Campbellton and
Dalhousie through Belledune and Bathurst over to Caraquet
and then south along the east coast from Shippegan and
Tracad ie down to the Newcastle-Chatham area, and
somewhat inland along the M iramichi River and its
tributaries. Farmlands occur in small parcels interspersed
between larger areas of forested land. Most of the
topography is level to undulating and so it holds more
prom ise for agriculture, however, it is more likely that early
settlement patterns are responsible for this agricultural
development. For many, farming has supplemented logging
or fishing, or vice versa. Farming is genera l in nature,
including the pro duction of cattle, hogs and poultry and
dairy and the associated cultivation of fields crops such as
hay, oats, barley and small areas of mixed grains and corn.
Vegetab le production of potatoes, cabbage, cauliflower,
carro ts and the like is for lo cal consumption. Wild
blueberries are a traditional crop which is being encouraged
through land clearing and m anagem ent of natural stands.
M ining
As a result of its comp lex geo logical history, central and
northen New Brunswick possess a great variety of mineral
resources. These include metals, non-metallic industrial
minerals, fuel-energy resources and structural materials (N.
B. Dep artment of Commerce and D evelopment No d ate).
No n-metallic industrial minerals include limestone, granite,
phosphate, marb le, diab ase, slates and silica. Only the
limestone and silica are being actively worked and extracted.
Bo th are at sites near Bathurst.
Fuel-energy resources are limited in their abundance.
Drillings have revealed coal deposits scattered along the
N o r t h u m b e r l a n d S h o r e f r o m T a b u s i n ta c t o
Shippegan-Caraquet, but quantities and quality do not
warrant development at the present time. Explorations have
identified uranium deposits in the central highlands which
show potential. Organic soils in the northeast are a source
of peat which is presently being " mined" for horticultural
purpo ses. Suitability as an energy source is being
considered. Experimentation with peat fueled greenhouse
heating was tried.
Sand, gravel and other aggregate structural materials are
quarried throughout the area. Mo st such operations are
relatively small, servicing local nee ds on ly. Processing may
or may not involve some screening. Some bedrock
materials, granites, slates, sandstone, etc., are also being
utilized for things such as building materials, road fill and
riprap.
Recreation
The recreational base in central and northern New
Brunswick includes over 350 km of coastline, 2.7 million ha
of wilderness land and hundreds of small rivers, lakes and
streams (N. B. Department of Comm erce and Developm ent
No date). Recreational use of the land has become
increasingly important in recent years. Most of the
recreational activity is centered on hunting and fishing.
5
Numero us species of both large and small game abound:
moose, deer, bear, coyote, bobcat, muskrat, raccoon, fox,
mink, rabb it, ducks, geese, partridge and woo dcock. Mo st
noteworthy to the fisherman are the abundant salmon
streams, the Nashwaak, the Restigouche and the headwaters
of the infam ous M iramichi. Othe r recreational activities
include canoeing, hiking, swimming, rock collecting, and
nature watching in the summer, and snowshoeing, skiing and
snowmobiling in the winter. There are several game refuges
and provincial p arks. M ount Carleton P rovincial Park in
north central New Brunswick is particularly scenic. It also
encompasses the highest peak in the province, Mount
Carleton, at 820 m above sea level (asl).
Land O wnership
Land ownership is divided into three categories: Crown
land, 70%; large freehold , 9%; and small freehold, 21%
(Smith 1982). Crown lands are administered by the
provincial governme nt. Freehold refers to lands that are
privately owned . Small freehold are parcels with less then
200 ha of land, usually in or adjacent to settled areas; large
freeho ld are parcels with more than 200 ha of land. The
basic land tenure pattern of the study area was determined
by early settlement. Land ownership impacts directly on
land use. D istribution of small freehold properties is almost
identical to that of farmland distribution. Early land grant
patterns and su bseq uent sub division of these original parcels
from generation to generation has resulted in numerous
relatively small land holdings. This is further aggravated by
the urbanization of rural lands. Large freehold properties
are concentrated in the southern por tion of the survey area
around Tuad ook Lake, Hayesville and N apadogan. Less
extensive blocks of large freehold are found along the
northwestern boundary, adjac ent to M adawaska and V ictoria
Coun ties. As with C rown land, all large freehold is forested.
In all freeho ld land, both large and sm all, the mineral rights
have been retained by the Province.
PHYSIOGRAPHY, TOPOGRAPHY, DRAINAGE AND
BEDROCK GEOLOGY
Most of the major landforms in central and northern New
Brunswick are the result of tectonic (broad regional
assemblage of structural or d eform ational features o f the
earth crust) and erosional forces at play over the past
135,000,000 years (Rampton et al. 1984). The survey area
occupies parts of the Maritime Plain, New Brunswick
Highland s, Chaleur U pland s and No tre Dame M ountains
(Fig. 2) of the Appalachian Region (B ostock 1970).
The Maritime P lain po rtion is also know n as either the
Central and Eastern Lowlands (Putnam 195 2) or the New
Brunswick Lowlands (Weeks 1957, Rampton et al. 1984).
It rises from sea level along the N orthumbe rland Strait to
elevations greater than 150 m (500 ft) at its western boundary where it grades into the M iramichi Highlands portion
of the New B runswick Highland s. The M aritime P lain is
characterized by flat to gently undulating landscapes.
Because of its flatness and owing to the nature of the soil
parent materials depo sited during glaciation and post glacial
marine submergence, drainage is for the most part imperfect.
Drainage is highly dependent upon relief. W ell drained so ils
are restricted to crests and upper slope positions. More
extensive areas of better drainage are associated with steeper
slopes along the transition to the New Brunswick Highlands
or where streams are more strongly incised. The Nashwaak
Hills are an example of this. They are well drained b ecause
of higher relief. The Nashwaak H ills are also the only
portion of the Maritime Plains within the study area that do
not drain into the Gulf of St Lawrence. The Nashwa ak H ills
drain via the N ashwa ak and Saint Jo hn Rivers into the Bay
of Fundy. T he Central Lowlands and the southern portion
of the Acadian P eninsula subd ivisions o f the M aritime P lain
are draine d by the Miramichi River into the Gulf of St
Lawrence. The Central Lowlands consist of broad flat areas
with weakly expressed valleys. Other than for the areas
adjacent to the Southw est M iramichi River where local relief
is more pro noun ced, draina ge is at best fair. A very poo rly
defined north-south oriented trough called the CurventonBathurst Valley (Rampton et al. 1984) occurs along the
western edge of the Acadian Peninsula, separating it from
the New B runswick Highlands. The C urventon-B athurst
Valley bottom is imperfect to poorly drained, with somewhat
better drainage in the series of benches forming the valley
sides. Troug h drainage is either north via the Nepisiguit
River or south via the No rthwest M iramic hi River. The
Acadian Peninsula is a gently sloping, eastward-facing
impe rfectly drained plain that descends from 150 m
elevation adjacent to the Curventon-Bathurst Valley to sea
level along the coast. It is drained by the Bartibog,
Tabusintac, Tra cadie and Pokemouche rivers into the Gulf
of Saint Lawrence. Areas of better drainage occur where
these rivers are more dee ply incised into the bedrock. The
Maritime Plain is dominated by grey-green Pennsylvanian
sandstone bedrock (Fig. 3) with only minor locally occurring
shale, siltstones and conglomerates. Some redbeds occur,
the largest concentration of which are in an area south of
Bathurst.
The New B runswick Highlands with their more rugged and
hilly landscapes are in stark contrast to the gently undulating
Maritime Plain. Rampton et al (19 84) subd ivided this
portion of the study area into four major divisions: the
Eastern, Northern, Central and Southern Miramichi
Highland s. The Eastern M iramichi Highlands are essentially
a transition zone between the Maritime Plain and the new
Brunswick Highlands proper. E levations are typ ically below
350 m and landforms gently rolling with moderately good
drainage.
Gauthier (1983) described the No rthern
Miramichi Highlands as having “the highest sum mits of New
Brunswick. They form a central undulating high plateau
with an ave rage elevation well ab ove 600 metres. Mount
Carleton is the highest peak with an elevation of 820
6
Figure 2. Physiographic regions of the survey area based on Bostock (1970 ) as modified by Rampton et al. (1984).
metres.” Relief exceeds 200 m and streams are deeply
incised resulting in a preponderance of well drained
conditions. As a result of deep entrenching, the streams are
typically rock-walled.
Some less elevated broad
depression areas occur to the south and east of this central
core zone . Drainage is provided by the Nepisiguit R iver to
the north, the Miramichi River to the east and the Tobique
and Serpen tine Rivers to the west. The Central and
Southern Miramichi Highlands are progressively lower in
elevation and less pronounced in topography, grading from
a more hilly aspect in the Central Miramichi Highlands to
rolling landscapes in the Southern Miramichi Highland
subd ivision. Elevations range from 350 to 600 m in the
Central Miram ichi Highlands but seldo m exc eed 300 m in
the Southern zone. W hile both areas are generally well
drained, impeded drainage occurs in some localized valleys
in the Central Miramichi Highlands and broader
depressional areas in the Southern M iramichi Highland s.
The Central Miramichi Highlands are drained solely by
tributaries of the Miramichi River. The Southern Miramichi
Highlands drain into the Saint John W atershe d primarily via
the Becaguimec, Keswick and N ashwaak Rivers. The
Miramichi Highlands are underlain by a number of bedrock
types. The northern portion co nsists of Ordovician
7
Figure 3. Bedro ck geo logy of the survey area b ased on P otter et al. (197 9).
formations of silicic volcanic rocks, rhyolite, rhyoliteporphyry, silicic tuffaceous rocks and metamorphosed
equivalents, quartz, and quartz-feldspar schist with some
mafic volcanic flows in a distinctive circular pattern. South
of this are parallel formations of Devonian granites and
granod iorites, Ordovician argillaceous sed imentary rocks,
greywacke, quartz, conglomerate and m inor limestone, tuff
and volcanic flows, and Silurian greywacke, slate, siltstone,
sandstone, conglome rate and limestone. M inor areas of
M ississippian and/or Pennsylvanian red to grey
conglomerate and siltston e are also present.
The Chaleur Uplands consist of a plateau extending from
west of the Restigouche River to a transition zone with the
New Brunsw ick Highlands that runs from north of Mount
Carleton over to B athurst. The eastern boundary of the
Chaleur Uplands (Fig. 3) is a mo dification of B ostoc k’s
(1970) physiographic divisions as suggested by Rampton et
al. (1984) to better align physiographic units with major
structural elements of the region. The Uplands tend to be
lower in elevation and less rugged than their adjacent
counterp arts, the New Brunswick Highlands on the east and
Notre Dame Mo untains on the west. Excluding the narrow
Chaleur Coastal Plain and the localized Campbellton Hills,
8
the Chaleur Uplands portion of the study area is dominated
by two subdivisions, the Saint Quentin Plateau and the
Jacquet Plateau. T he Jacquet Plateau is east of the
Up salquitch River. It consists of a north-sloping plateau
ranging in elevation from 450 m along its southern border
with the Highland s to less than 100 m as it approaches
Chaleur Bay. A series of northeast running ridges occur
south of Dalhousie. Drainage is via the deeply incised
Upsalquitch, Jacquet and Tetagouche Rivers in a northe rly
or northeasterly direction. These rivers are all steep-sided,
rock-walled, V-shaped drainage channels in their upper
reaches. Bedrock geology consists of Silurian and Devonian
greywacke, slate, shale, sandstone, limestone and
conglomerate with minor volcanic rocks of rhyolite, trachyte
and basaltic flows. The Saint Que ntin Plateau falls mostly
between the deeply incised R estigouche and Upsalquitch
Rivers. Elevations are in the 300 to 425 m range. Relief
averages less than 100 m and is co nsiderably less
pronounced than in the Highlands. Although drainage is for
the most part mode rate, the gently rolling to und ulating
nature of the landscapes lead to some low lying, flat areas
being poo rly drained. T he Camp bellton Hills are a localized
series of ridges and hills running parallel to the Restigouche
River from west of Dalhousie to the Upsalquith River.
Elevations are usually in excess of 300 m with relief varying
from 50 to 150 m, resulting in typically well drained
conditions. Und erlying bedro ck is a mixture of greywacke,
slate, sandstone and conglomerate, with some limestone and
volca nic rocks. The Chaleur Coastal Plain is a narrow (2-10
km wide), low lying (less than 80 m elevation), gently
sloping, imperfectly to moderately well drained, plain
adjacent to Chaleur Bay underlain by the same bedrock as
found in the adjoining Jacq uet Plateau..
The Kedgwick Ridge H ighlands subdivision of the Notre
Dame Mo untains occupies the area west of the Restigouche
River from the Restigouche County line north and west to
the Queb ec interprovincial border. As the name implies,
these highlands o r mountains are mo re rugg ed an d exhibit
greater relief than fo und in the Chaleur U pland s to the east.
Elevations range from 4 50 to 600 m with relief o f 100 to
250 m. More deeply incised tributaries of the Restigouche
River, including the Kedgw ick River, result in narrow
valleys and greater relief along the eastern edge of the area.
This area is predominately well drained. T he western half
of the subdivision is more rolling with less relief. Here,
broad, flatter valleys with poorer draina ge sep arate the well
drained uplands. The underlying bedrock consists of
Devonian shale, limestones and sandstone, with minor
greywacke, tuff and volcanic rocks.
CLIMATE
Atmosph eric climate
Despite its mid-latitude maritime location, the survey area
has a modified continental climate (Chapman and Brown
1966). The prevailing westerly winds in Maritime Canada
blow offshore, resulting in a mo re extre me climate sim ilar to
inland Canada (Dzikowski et al. 19 84). In general, weather
changes are numerous with the passage of low pressure air
masses from interior No rth Am erica. Summ ers are cool,
winters are cold and snowy, and springs are short and late.
Near the coast, the ocean moderates the continental
influence. Coastal areas tend to have long but cool growing
seasons, while sheltered inland valleys have shorter but
warmer growing seasons. Advantages of a prolonged
growing season along the co ast are o ffset by cooler
temperatures. However, the waters of the Gulf of Saint
Lawrence are warmer in the summer and colder (frozen) in
the winter than the Atlantic Ocean, resulting in less of a
mod erating effect.
Annual daily mean air temperature ranges from 2.0 to 5.2 oC.
W inter temperature extremes in Janu ary can drop do wn to
below -40oC in the highlands and uplands. Annual
precipitation ranges from 1000 to over 12 00 mm p er year,
of which 280 to 380 cm are snowfall. Snow cove r helps to
minimize the impact of low winter temperatures on ground
vegetation. Although slightly heavie r in late fall and early
winter, precipitation is distributed fairly evenly throughout
the year, providing adequate moisture (375 to more than 500
mm) during the growing season of May to September.
Occasional dry periods do occur. Excess moisture resulting
from snowmelt is common in spring.
Duration of daylight (sunrise to sunset) ra nges fro m ab out 9
hours in December to about 16 hours in June. However, the
rather cloud y cond itions typical of the area result in considerably less sunshine hours--especially along the coast of
the Northumbe rland Strait.
The average frost free period (days from last spring frost
until first fall frost) varies greatly depending upon latitude,
elevation, topography and distance from the coast. The
southern and eastern m ost areas have the longest frost-free
periods with in excess of 130 days (May 23 to September
30) while in the central and northwestern regions the
average frost-free period is less than 9 0 days (June 14 to
September 1).
Dzikowski et al. (1984) stratified the atmospheric climate of
the study area based on annual growing degree-days (above
5 oC) and M ay to September rainfall (Fig. 4). This map
provides information on the distribution of heat units and
growing season precipitation within the area. In general,
areas with higher heat units and moderate precipitation are
more favourable for agriculture. The Exploratory S oil
Survey of Central and Northern New Brunswick has areas
falling within climatic zones 2A, 2B, 3A, 3B, 3C, 3D, 4C
and 4D. W ithin these zones, annual degree-days (greater
than 5 oC) vary from 1200 to 1800 and M ay to September
precipitation from 350 to 550 mm. W hile other parameters
can be used to stratify climatic c ond itions, the m ap in F ig.4
9
complex and indirect. Soil climate resp ond s to atmospheric
climate, but these changes are a function of time and of soil
conditions--soil moisture content, depth, surface cover, and
site position. Based upon temperature and moisture
conditions for bio logically significant periods of the year,
Clayton et al. (1977) classified the so il climate of the
lowlands portion of the surveyed area as Humid B oreal and
for the uplands po rtions, primarily P erhum id Cryobo real.
The Humid Boreal areas are characterized by a mean annual
soil temperature, measured at a depth of 50 cm, of 5 to 8°C
and mean summer (June, July, and August) soil temperature
of 15 to 1 8°C. In most years, no soils are dry for as long as
90 consecutive days; thus, water deficits are slight during the
growing season (2.5 to 6.4 cm). A s with atmospheric climate, marine influence results in a modified regime along the
coast. The Perhumid Boreal areas are characterized b y a
mean annual soil temperature of 2 to 8°C and mean summer
soil temperature of 8 to 15 °C. Th e soils are mo ist all year,
seldom being dry, with no significant water deficits in the
growing season (less than 2.5 cm).
VEGETATION
Figure 4. Climatic zones within the survey area based on
Dzikowski et al. (1984).
provides a good representation of climatic trends and
variab ility within the study area. Within the survey area two
influences dominate the climate--the moderating effect of
the Atlantic Ocean along the eastern shore and the cooling
effect of increased elevations in central and northwestern
New Brunswick. Essentially, annual heat units decrease and
growing season rainfall increases along two transects going
from south to north and from east to west. T he mo re highly
elevated areas in the central and northern portions are colder
and receive more M ay to September precipitation than the
coastal and southern regions. The lower temperatures are a
function of more no rthern latitudes, higher elevations and
greater distance from the coast. As Dzikowski et al. (1984)
explain, lower precipitation along the coa st is “caused by the
air descending and warming, thus being able to hold more
water and producing less precipitation. In effect, the
topography shelters the se areas from storm winds. A ir
masses moving into north eastern coastal New Brunswick
have lost much of their moisture over the central highlands
resulting in lower precipitation in these areas.”
Soil climate
Although implications of the atmospheric climate have been
well documented, knowledge of the interaction between
atmo spheric and so il climates is essential for various land
uses, in particular, productive plan t growth as related to
subaerial development and for some engineering
app lications. This relationship, although possible, is often
According to Rowe (197 2), central and northern New
Brunswick includes parts of three major forest regions - the
Acadian, Great Lakes-St. Lawrence and B oreal Fo rest
Regions (Fig. 5). However, given that the survey area is on
the border of these zones, being at the southwestern extreme
of the Boreal Forest Zone, the eastern extreme of the Great
Lake s-St. Lawrence Forest Region and the northwestern
extreme of the Acadian Forest Region, the forest stands tend
to be somewhat intra-zon al.
Forests of the Notre Dame M ountains in western
Restigouche County are part of the Gaspe Section of the
Boreal Fore st Region. Although mixed conifer-hardwood
stands occur, the dominant forest cover type is conifers:
balsam fir, black spruce and white spruce, o ften with eastern
white cedar.
White birch is a common hardwood
com pon ent in these stand s.
East of this, the Chaleur Uplands fall in the Tem iscouataRestigouche Sectio n of the G reat La kes-St. Lawrence Forest
Region. Rowe (1972) describes these forests as
“characterized by sugar maple, beech and yellow birch on
the hill tops with balsam fir and white spruce in the valleys.
... Eastern white cedar of good size is common on lower
slopes. On hillsides an d low rocky knolls b alsam fir forms
mixtures with yellow birch, white birch and, formerly at
least, with the eastern white and red pines. Though much
reduced in impo rtance relative to their earlier status, the
pines are locally ab unda nt, and eastern white pine shows up
prominen tly in second growth stands which have sprung up
following fire. Alluvial flats support balsam poplar, black
ash, white elm and white spruce. Other species distributed
through the Section are red maple, white birch and jack pine,
10
Figure 5. Forest regions and sections within the survey area
based on Ro we (1972).
the latter species forming locally important pulpwood
stands. Both white birch and aspen regeneration are prolific
following fire. Black spruce and tamarack are found on
botto mland s and in bog gy areas.”
The New Brunswick Highlands and Maritime Plain portions
of the study area are part of the Acadian Forest Region.
Mo re specifically, Rowe (1972) has subdivided the New
Brunswick Highlands area into the New Brunswick Uplands,
Upper Miramichi-Tobique, Carleton and “Southern”
Uplands Sections. The Maritime Plain area falls within the
Eastern Lowlands Section. High altitudes result in the New
Brunswick Uplands Section being dominated by coniferous
forests, with a noticeable boreal similarity. Balsam fir, black
spruce, white spruce and white birch dominate. White pine,
eastern hemlock and red sp ruce o ccur sp orad ically. Coarser
textured soils and frequent forest fires has increased the
presence of trembling aspen, jack pine, white birch, eastern
white pine and red pine. Tolerant hardwoods are scarce.
The Uppe r Miramichi-Tobique Section has a more
pronounced hardwoo d compo nent. Crests and upper slopes
are forested with sugar maple, yellow birch and beech;
midd le slopes include a com pon ent of red and white spruce,
eastern hemlock and balsam fir; and lower slopes and
depressions support primarily coniferous stands of spruces,
fir, eastern white cedar and tamarack. Northern reaches of
this Section have a more boreal-like coniferous-dominated
forest type as found in the adjacent New Brunswick Uplands
Section. W hite birch, red maple and trembling aspen are
common successional species after harvesting and/or fire.
Grey birch, eastern white pine, red pine, jack pine, red
map le and black ash are restricted to local occurrences. A
small area of Carleton Section forest types occur along the
southwestern edge of the survey area. Hardwood stands of
sugar maple, beech, yellow birch, red maple and white ash
predominate but yellow birch, balsam fir, eastern hemlock
and eastern white pine occur in the mixed wood transitional
forests that grade into the higher altitudes of the Upper
Miramichi-Tob ique Section to the east. Poorly drained
areas support stands that include eastern white cedar, black
ash, red maple and white elm along with black spruce,
balsam fir and some eastern hemlock. Small areas of the
“Southern” Uplands Section occur just north of Fredericton
and along the eastern side of the New Brunswick Highland s.
Tolerant hardwoods - sugar maple, beech and yellow birch occupy crests and upper slo pes while red maple, white birch,
balsam fir, red spruce, eastern white pine and eastern
hemlock dom inate low er slopes. Black spruce, tamarack,
eastern white cedar and red map le populate poorly drained
areas.
On the Maritime Plain, impeded drainage has lead to a
prevalence of pure stand s of black spruce, red spruce, and
balsam fir or mixed wood in which these species are
associated with eastern white pine, red maple, trembling
aspen, sugar maple, yellow birch, and white birch. Forest
conditions and species distribution largely reflect the effect
of: a high level of annual burn; extensive logging activities;
and repeated infestations of spruce budworm. As a result,
correlation of vegetation with soils an d land form is poo r.
Balsam fir has been infested and defoliated by spruce budworm to the point that mature stand s are relatively sparse,
but regeneration of ba lsam fir is quite comm on thro ugho ut.
Pure stands of American beech, with some sugar maple and
yellow birch and a scattering of spruce and fir, are common
on exposed ridges. On extensive flat-lying poorly drained
areas, swamps and peat bogs of sphagnum moss-ericaceous
shrub complexes are interspersed with stands of black
spruce and tamarack, and some eastern white cedar.
Eastern hemlock, once well represented, is now limited in
extent, as the result of repeated cuttings and fires. Exposure
to wind reduces tree stature along the coast.
11
PART 2. SOIL FORMATION AND CLASSIFICATION
SURFICIAL GEOLOGY
Excluding the continuous processes of weathering, the
surficial geology of the survey area has de velop ed primarily
as a result of four primary phenomena: glaciation, submergence, alluviation, and paludification (Rampton et al. 1984).
Of these, the effects of glaciation are predominant, with other processes acting as modifiers While glacial and postglacial events over the more recent 600,000 years have lead
to only minor modifications of pre-glacial landscapes, they
have had m ajor impacts on so il parent material composition
and distribution. During one stage of the Pleistocene epoch,
W isconsinan ice covered the entire province of New
Brunswick. All preglacial surfaces were scoured and subsequently cove red b y a man tle of glacial drift of varying
thickness. W ith deglaciation, which is thought to have
occurred about 10,000 to 12,000 B P (before present), the
low-lying Maritime Plain was subjected to a period of
s hall o w marine submergence. Maximum ma rine
submergence is thought to have been about 120 m above sea
level (asl). Postglacial submergence was follo wed by a
period of emergence, during which the relative levels of the
land and ocean attained present day status. This emergence
was at least partially completed by 8000 BP. The most
active post-submergence processes of material deposition
are those of alluviation (materials deposited by present
rivers and streams) and paludification (the development of
organic deposits or peatlands), which continue at present.
SOIL PARENT M ATERIALS
Based on their parent materials, soils are divided into two
categories or group s: mineral soils and orga nic soils.
Mineral soils consist predominantly of mineral matter, or
natural inorganic compound s as found in sands, silts, clays
and rock fragme nts of gravels, cobb les, stones and bo ulders.
Essentially they have formed in unconsolidated bedrock
material that, in the case of central and northern New
Brunswick, has usually been displace d, as previously
mentioned. Organic soils consist of peat deposits that
contain more than 30% organic matter and are typically
greater than 40 cm thick, but often exceed 2 m in total
accumulation.
M inera l Soils
Residual - Soils formed from, or resting on, consolidated
rock of the same kind as that from which it was formed and
in the same locatio n are called re sidual soils. The ma terials
consist of unconsolidated or pa rtly weathered bedrock that
has deve loped as a result of in situ physical, chemical and
biological activities. D ue to a similarity in appearance and
com position, residual materials are o ften difficult to
differentiate from glacial tills. Only those areas dominated
by parent materials of a residual nature were included and
mapped in this category. Most exposed bedrock surfaces
have some weathering, b ut this is usually limited to the
upper 0.5 m of rock (Rampton et al. 1984). However,
deeper bedrock weathering is associated with some areas of
sandstone bedrock in the Maritime Plain and granitic
bedrock in the New Brunswick Highlands. These areas of
more deeply weathered bedrock are thought to be preglacial
in origin (Chalmers 1888, W ang et al. 1981). While the
sandstone bedrock may be weathered to a depth of up to 2
m in some loca lized areas o f the M aritime P lain, it is
generally overlain by othe r soil form ing parent materials and
mapped accordingly. More deeply weathered granites are
scattered throughout the New Brunswick Highland s. These
deposits are extensive eno ugh to have b een map ped as a
unique soil association They also occur as undesignated
com pon ents of related till soils. Rotting of granitic bedrock
has produced ellipsoidal-shaped tors or core stones on some
of the highe r mountain p eaks. A ma ntle of grus, consisting
of coarse-grained fragments resulting from the disintegration
of the granite, occurs over most such areas. In gene ral, soils
mapped as residual consist of a complex mixture of
disintegrated bedro ck, colluvium (materials deposited by
mass-wasting, usually at the base of a steep slope) and some
glacial till ma terial.
Glacial Till - Morainal till of varying thickness was
deposited as either ablatio n till or lod gment (basal) till as a
result of glacial activity during the last ice age. The glacial
deb ris was typically deposited as a mo rainal blanket o f 1 to
2 m in thickness but with some veneer depositions (less than
1 m) and some areas of greater accumulation (greater than
2 m). As Rampton et al. (1984) state “even though they
consist dom inantly of till, in ma ny places they comprise a
complex of ablation till, lodgment till, glaciofluvial depo sits,
glaciolacustrine deposits, colluvium, and weathered
bedrock.”
Lodgment tills are dense and compact due to the pressure
applied by the weight of the glacial ice that plastered them
in place and subsequently overrode them as the glaciers
advanced. Ablation till is that material carried on top of or
within the glacier and is generally stonier and usually not
compacted. It is released from the glacier in the ablation
zone, the area where melting occurs at a greater rate than
accumulation. As the ice melts, material is released from the
glacier where it may accumulate to a thickness of many
metres, creating an ablation moraine. In general, true
ablation tills tend to be thicker than lodgment tills. Ablation
till generally exceeds 5 m in thickness (Rampton et al.
1984), however, areas of negligible coverage are also
commo n. Thin ablation de posits are considered to be the
result of rapid retreat of the glacial ice, not allowing for any
significant accumulation of ablation debris. Most lodgment
12
tills have some capping of ablation material, albeit very thin.
Slowly retreating or stationary d ebris-rich ice she ets resulted
in thicker ribbed, humm ocky and rolling ab lational till
depo sits.
Differentiation of ablational from lo dgm ent till materials is
almost impossible where the ablational capping over
lodgment till is thin and soil formation has obliterated the
interface. Identification is made more difficult where the
ablation and lodgment tills are alike in texture and colour.
Similar difficulties in identification occur where tills are
shallow and soil forming processes have been active
throughout the depo sit thickness. Even in lodgm ent tills,
soil forming processes loosen the upper 50 cm of material.
Some materials deposited as ablation debris now have
relatively compact subsoils, a development that Rampton et
al. (1984) attribute to postglacial processes. Representative
ablatio nal tills that are considered to be “no ncompa ct” still
have subsoils which are den ser than the surfac e soil due to
the weight o f overlying materials. No attemp ts were made
to differentiate compact ablational till from compact
lodgment till. Soil materials with similar physical and
chemical properties were grouped together, regardless of
original mode of deposition.
In areas of high bedrock relief, glacial erosion has resulted
in most lodgm ent till dep osits being relatively thin veneers.
Texture, colour and coarse fragment lithology of lodgment
tills closely resemble the underlying bedrock, or at least the
bedrock that is in an up -flow glacial direction, usua lly
northwest. Ablation tills may have a more wide-ranging
lithological composition and weaker ties to the underlying
bedrock type. Excluding the northern half of the Acadian
Pen insula where redd ish bro wn tills are comm on, most tills
are yello wish to o live bro wn or grey.
Meltwaters from the glacier have often reworked the surface
of the till to give it a glaciofluvial appearance. This may
happen to such an extent that it is very difficult to
differentiate between a highly reworked ablation till and a
glaciofluvial deposit.
For the purpo se of mapping, tills with compact subsoils were
considered to be lodgment tills and tills with non-compact
subso ils were considered to be ablatio n tills. Lodgment and
ablation tills were further categorized on the basis of soil
parent material particle size class, reaction, colour and
lithology.
Fluvial - All sediments, past and present, deposited by
flowing water, are fluvial. This includes glaciofluvial
materials that were moved by glaciers a nd sub sequently
sorted and deposited by streams flowing within and from the
melting ice, forming outwash plains, deltas, kames, eskers,
and kame terraces. Alluvial materials deposited by modern
rivers and streams are also included in the “fluvial”
designation. Glaciofluvial deposits are usually stratified
sands and gravels and exhibit some degree of sorting,
depending upon the amount of water working to which they
have been subjected. T heir pa rticle size ranges from
coarse-loamy to sandy-skeletal.
Although many
glaciofluvial deposits occur along present-day drainage
channels, other, such as eskers, which have formed in
tunnels and channels within the glacier ice, are notorious for
traversing landscapes with little regard to existing
topography. Because of water working actions, glaciofluvial
coarse fragments are strongly rounded. The coarse-textured,
highly permeable nature of glaciofluvial sediments means
that most soils develop ed on these m aterials are well
drained, unless drainage is impeded topographica lly.
Gra velly, cobbly and bouldery alluvial materials are found
in up-stream locations. Finer-textured alluvial sedim ents
consisting of fine sands, silts and clays and organic materials
form terraces and floodplains along lower stretches of
streams and rivers. Alluvium is commonly underlain by
glaciofluvial sediments.
Marine - Post glacial marine submergence resulted in sands
of varying thicknesses being deposited on the tills and a
general reworking of surficial materials in the Maritime
Plain portion of the study area. These sandy deposits range
up to several metres in thickness, but also commonly occur
as thin veneers over either glacial tills or bedrock. Thick
dep osits of reworked marine, or possibly lacustrine clays,
are also found well above present day sea levels. Since
many of these deposits contain remn ants of glacial materials,
they more ap tly may be considered as “glacial marine”. A
report by the Maritime Resource Management Service
(1978) describes the depositional environment for materials
on the Chaleur Coastal Plain as follows: “Marine depo sits
are associated with the invasion and recession of marine
waters on and from the land . During deglaciation, the
earth’s crust was still depressed from the weight of the
glacial ice sheet and the sea was able to encroach upon the
land surface. The marine submergence extend ed inland to
78 metres above the present sea level in the Jacquet River
area... The uplift was very gradual, thereby creating a
suitable depositional environment for extensive marine
sedim ents along the coast.... Much of the study area along
the coast north of Peter’s River consists of a complex of
raised beach ridges, strand lines and logoonal sediments.
Each beach system represents a shoreline which has been
washed by the waves o r tides of a sea undergoing a eustatic
decline in sea level relative to the uplifting land mass. The
material associated with these deposits is a well-graded,
gravelly loam exhibiting continuous stratification, which
indicates extensive washing and sorting.”
Or gan ic Soils
Three types of organic deposits have been identified and
mapped.
Bog - Bogs consist of sphagnum and to a lesser extent forest
peat materials. They have formed in an ombrotrophic
(nutrient poor) environment due to the slightly elevated
13
nature of the accumulation. This tends to disasso ciate them
from the nutrient-rich ground water of surrounding mineral
soils. These organic materials are extremely acid (pH less
than 4.5) and weakly to moderately deco mpo sed (fibric to
mesic). Bogs are associated with depressions where the
water table is at or near the surface for the entire year. Mo st
dep osits are virtually treeless, with the exception of some
severely stunted conifers around the periphery. They are
characterized by a ground vegeta tion cover of sphagnum
mosses and ericaceous shrubs. Bo g units mapp ed in this
survey are typically domed bogs on the M aritime Plain.
Fen - Fens consist of peat materials derived primarily from
sedges formed in a eutrop hic (nutrient rich) environment.
This is due to the clo se asso ciation of the material with
mineral-rich waters. F en ma terials are med ium acid to
neutral (pH 5.5 to 7.5) and mode rately to strongly
decomposed (mesic to humic). They are associated with a
nutrient-rich watertable that persists seasonally at or very
near the surfac e. M ost deposits have a low to medium
height shrub cover and sometimes a sparse layer of trees.
Stream fens are the most commo n type of fen found in the
survey area. M ost mapped fens have a surficial capping of
acidic sphagnum peat and are in a stage of transition towards
a bog enviro nment.
Swamp - These units are dominated by peat materials that
consist of moderately to strongly decomposed (mesic to
humic) forest peat. They have fo rmed in a eutro phic
environment resulting from strong water movement from the
margins with surrounding mineral soils. Forest peat
materials are medium acid to neutral (pH 5.5 to 7.5). They
are associated with stream courses and depressions where
standing to gently flowing waters occur seasonally or pe rsist
for long periods on the surface. The vegetative cover
usually consists of a thick forest growth of coniferous and
deciduous trees. Swamps were map ped in the highland and
upland areas of the survey area.
SO IL DEVELO PMENT
FACTORS
AND
SOIL
FORMING
Soil genesis or formation involves all the processes that are
respo nsible for the d evelo pme nt of soil. Although the
individual processes are numerous, studies have shown that
the kind o f soil that develops is largely controlled by five
major factors: climate (particularly temperature and
precipitation); parent material (mode of deposition, texture,
and mineralogical com position); top ography or relief (in
relation to soil drainage and rates of soil erosion); living
organisms (especially natural vegetation, but also animal
life); and time (the period over which the soil parent
material has been subjected to soil formation). T hese
factors were described in the preceding text under Part 1.
General Description of the Area.
Soils are very much products of their environme nts.
Different environmental cond itions result in dissimilar soil
formation. The differences in the types of soil formed is
dependant upon the magnitud e of variation in the soil
forming factor(s) involved.
Clima te is perhaps the most influential factor in determining
the degree of weathering and thus the d egree of soil
formation that occu rs. The rate of chemical reaction doubles
for every 10 oC rise in temperature (Brady, 1974) . Soil
temperature is highly dependant upon soil moisture.
Biochemical reactions and changes are sensitive to both soil
temperature and moisture. Within the study area, annual
precipitation (rain plus snow-water equivalent) averages
1000 to 12 00 m m. Under these levels of p recipitation, soil
materials that have good drainage are readily leached of
soluble and mobile materials which are either translocated
and redeposited within the profile, or lost entirely from the
soil body. Podzolization, or the downward movement of Fe
and Al and organic matter, is an end resu lt. Annu al air
temperatures vary from a high of 5 .2 oC in the lowlands to a
low of 2.0 oC in the central portion of the N. B. highlands.
Lower temperature s result in reduced rates of chemical
reactions. Evapotranspiration is also lower and thus there is
higher "effective" p recipitation, ie., more o f the rainfall
mov es through the soil profile becau se less water is lost by
evaporation from the soil or via the plant (transpiration).
Variations in soil solum development result. This usually
takes the form of increased accumulation of organic matter
in the upper B horizo n. The climatic influence is also
indirec tly expressed in its control over natural flora and
fauna (organisms), which are in themselves contrib uting soil
forming factors. Meso, or local, climate influences the way
soils develop , both directly as a result of temperature
variations and secondarily through type of vegeta tion. Local
topo graphy, steepness of the slope, aspect, exposure,
position on slope and type of vegetation all modify
meso climatic conditions (van Groenewoud, 1983) and thus
impact on soil formation.
Living organisms p lay a significant role in soil pro file
develop ment. Natural vegetation in particular is a critical
factor in determining soil characteristics. Different types of
organic debris (leaves, stems, branches, etc.) can vary
considerably in mineral element content. The litter from
deciduous trees is comparatively much higher in bases such
as calcium and potassium than is litter from coniferous trees.
The higher b ase status in deciduous litter usually results in
a greater rate of decomp osition in the forest duff layer. In
contrast to this, the organic acids from coniferous forest
litter strongly leaches the upper min eral soil layers.
W indthrows, or the uproo ting of trees, mixe s the soil.
Although animal b ioma ss in natural soil ecosystem s is
typically less than 1% of plant biomass (Buol et al, 1973),
anima ls create and foster change in soil conditions. In the
adjoining counties of Carleton, Victoria and Madawaska,
which are to the immediate west of the study area, Langmaid
(1964) found alteration in surface horizona tion o f virgin
forest soil profiles as a result of earthworm invasion.
14
M icro-organisms are involved in biochemical reactions.
Even man plays a role in his use of the land. Conversion of
forested land to farmland is a most dramatic change.
Parent material has been recognized as a significant soil
forming factor since the inception of p edo logy. M any soil
properties are inherited from the initial parent material.
Since most of our soils are relatively young in age,
geologically speaking, weathering and soil formation have
not drastically obliterated the inherited properties of the
initial parent material. Different modes of deposition yield
soil parent materials with different compositions and
prop erties. Basal or lodgment tills that are so prevalent
throughout the study area tend to yield compact, finer
textured deposits than ablational tills.
Glaciofluvial
sedim ents are usually readily previous, sandy or sandy
skeletal materials. The lithlogy of the bedrock materials
from which the regolith has be en derived determines the
mineralogy of the soil. The po tential fertility supplying
power of a particular rock type depends up on both its
inherent nutrient content and its weatherability, or the rate at
which nutrients can be released (Colpitts et al. 1995). Of all
the mineral comp onents the clay fraction is the most
important beca use it is the most active in terms of physical,
chemical and biological processes. Most of the clays in our
soils are inherited from the so il parent material. Little
formation or alteration of clay minerals has taken p lace in
the period since glaciation. Illite dominates, but most soils
have significant amounts of chlorite and small amounts of
kaolinite and vermiculite-montmorillonite (C layton et al.
1977). Where the initial parent material contained large
amo unts of free carbonates, the normal acid leaching process
is retarded until the free carbonates are leached from the
soil. During this time, clay moves from the upper part of the
profile and is redeposited in the B horizon. When leaching
has gone beyond this stage and the upper part of the profile
is sufficiently acid, podzolization takes place.
Top ography or relief has been related to the following so il
properties (Buol et al, 1973): (1) depth of the solum; (2)
thickness and organic matte r content of the A horizon; (3)
relative wetness of the profile; (4) degree of horizon
differentiation; (5) soil reaction; (6) temperature; and (7)
chara cter of the initial (parent) material. To a large degree
these effects are moisture related. The rugged topography
of central and northwestern New Brunswick is cond ucive to
more extensive areas of better drainage than in the flatter
Maritime Plain region of northeastern New B runswick,
where excess water tends to remain in the landscape for a
longer perio d of time. Soil profiles d evelo p acc ordingly.
Locally, drainage variation across toposequences has
significant impact on the degree and nature of so il
formation. Poorly drained soils have less distinct and duller
coloured horizons than well-drained soils. Material types
are associated with different positions in the landscape.
Depressional areas that are saturated with water for a large
part of the year encourage the accumulation of organic soils;
alluvial soils occupy along flood plains; and so on.
Top ography also modifies the climatic influence and is a
determining factor in native vegetation cover type.
The period or time that any given material is subjected to the
processes of weathering is another factor in soil formation
that canno t be over em phasized. Soils are routinely
subjected to new cycles of soil development over both the
short term (ie. vegetative cover changes, erosion, etc.) and
the long term (ie. land up lifting, world climatic cha nges,
etc.). However, from a comparative point of view, time zero
can be established at that point following the last major
catastrophic event (Boul et al. 197 3). In the Atlantic
Region, glaciation was the last major catastrop hic eve nt.
W hile some remnants of weathered bedrock in central New
Brunswick are considered to be in excess of 1 to 1.5 million
years old, for the mo st part, glacial sediments have o nly
been exposed to weathering for some 10,000 to 12,000
years. Postglacial marine submergence in the lowland
portion of the area has resulted in slightly shorter periods of
exposure, 8,000 to 10,00 0 years. Alluvial floodplain
sedimentation is an ongoing process, as is p aludification
(orga nic soil accumulation). Materials are constantly being
added to the surface of these deposits and soil development
reflects these conditions.
From the foregoing discussion it is easy to see that the soil
forming factors are interdependent and interactive. They are
simultaneously at work, altering and continuously modifying
the soil profile.
SOIL PROFILE
The soil profile is a vertical cross section of the soil through
all its horizons and extending into the parent material. A
soil horizon is a layer of soil approximately parallel to the
land surface that differs from adjacent genetically related
layers in properties such as colour, structure, consistence,
texture or chemical, biological and mineralogical
compo sition.
Organic layers are differentiated from mineral horizons and
layers on the basis of organic carbon. (Organic matter
content is about 1.7 tim es the organic carbon co ntent.)
Organic layers co ntain 17% or more o rganic carbon. Two
groups of organic layers are recognized. O, organic layers
have develop ed mainly from mosses, rushes, and woody
materials; and L -F-H, organic layers have developed
primarily from leaves, twigs, and woody materials with only
a minor compo nent of mosses. Organic horizons are found
in Organic so ils and comm only at the surface of mineral
soils.
Mineral horizons and layers contain less than 17% organic
carbon. The master mineral soil horizons, from the mineral
soil surface downward, are designated by the letters A, B,
and C. The A and B horizons represent the upper and mo st
weathered part of the soil profile. Collectively, they are
15
referred to as the solum. The A horizon is formed at or near
the surface in the zone of removal of materials in solution
and suspension, or maximum in situ accumulation of organic
carbon. The B horizo n is immediately below the A horizon.
It is usually characterized by either an enrichment in
materials leached from the A horizon (ie. clay, iron,
aluminum or organic matter) or some other form of
alteration in colour and/or structure. The underlying C
horizon is the relatively unweathered parent material from
which the soil has developed. It is com paratively unaffected
by the pedogenic (soil-forming) processes operative in the
A and B horizons. Lowercase suffixes are appended to the
master horizon designation to indicate the type of horizon.
Arab ic nume rals are used when further subdivision is
required. Roman nume rals are prefixed to horizon and layer
designations to indicate parent material discontinuities in the
profile. Bed rock (greater than 3 on M ohs' scale of hardness)
is designated as R.
Imperfectly draine d mineral soils have the same type and
arrangement of horizons as their well-drained counterparts,
but because they are periodically saturated, a condition
called "mottling" develops. Mottling, or the occurrence of
spots of different colours or shades interspersed within a
matrix colour, is indicative of zones of alternating good
(oxidized) and poor (reduced) aeration. In well drained sites
the soils are well oxidized an d red , yellow and reddish
brown colours develop. Where oxygen is lacking, reduction
results in grays an d blues. Po orly and very poorly drained
soils are waterlogged for a large part of the year, and so,
because of the resulting reduced grayish-blue colours, are
said to be "gleyed". Excessive moisture tends to retard
profile development and expression. Horizonation is not
nearly as evident as in well drained soils.
A com plete listing of all horizon nomenclature used in this
report is prov ided in the Canad ian System of Soil
Classification (Soil Classification Working G roup 199 8).
A profile that is under native vegetation and unmodified by
man is considered a “virgin” profile. In a virgin p rofile the
effects of soil formation are left relatively undisturbed or as
is. Most forest soils are considered as virgin sites,
regardless of whether or not they have been logged in the
past. Under these conditions the naturally occurring
sequences of soil horizons and layers are readily expressed
and recognized. The exception to this is where road
construction and other soil displacing activities have taken
place. In contrast to forest soil profiles, agricultural soils
show drastic variation in the surface layers as a result of
cultivation. The organic surface layer, A horizon and upper
B horizon are mixed together into a relatively homogeneous
plow layer, which is designate d as the A p horizon. M an's
activities not only alter the soil's physical and chemical
com position, but also modify the soil forming factors
themselves and thus impa ct on future soil develo pme nt.
SYSTEM OF SOIL CLASSIFICATION
The soils are classified in accordance with criteria
established by the Canadian System of Soil Classification
(So il Classification Working Group 1998). Soil
classification is based on a vertical section of the soil pro file
referred to as the contro l section. The con trol section is
typically 1 m for mineral soils and 1 .6 m for organic soils.
The Canadian system is a hierarchical organization of
categories that permit the consideration of soils at various
levels of generality. The taxa are based upon soil properties
that can be observed and measured objectively in the field,
or, if necessary, in the laboratory. T he system has a ge netic
bias in that soil properties that reflect genesis are favoured
as differentiae in the higher categor ies. There are five
different levels:
Order. Taxa at the order level are based on properties of the
pedon that reflect the nature of the soil environment and the
effects of the dominant soil-forming proce sses.
Great group. Great groups are soil taxa formed by the
subdivision of each order. Thus each great group carries
with it the differentiating criteria of the order to which it
belongs. In addition, taxa at the great group level are based
on properties that reflect differenc es in the strengths of
dominant processes or a major contribution of a process in
addition to the dominant one. For exam ple, in Luvic
Gleysols the d ominant pro cess is considered to be gleying,
but clay translocation is also a m ajor pro cess.
Subgroup. Subgroups are forme d by subdivisions of each
great group. Therefore they carry the differentiating criteria
of the ord er and the grea t group to which they belong.
Subgroups are differentiated on the basis of the kind and
arrangement of horizons that indicate: conformity to the
central concept of the great group, i.e. Orthic; intergrading
toward soils of another order, e.g. Gleyed or Brunisolic; or
additional special features within the control section, e.g.
Ortstein.
Fam ily. Taxa at the family level are formed by subdividing
subgroups. Thus they carry the differentiating criteria of the
order, great group, and subgroup to which they belong.
Families within a sub group are differentiated o n the basis of
parent material characteristics such as texture and
mineralogy, and soil climatic factors and soil reaction.
Series. Series are formed by sub divisions of families.
Therefore they carry all the differentiating criteria of the
order, great group , subgroup, and family to which they
belong. Series within a family are differentiated on the basis
of detailed features of the pedon. P edo ns belonging to a
series have similar kinds and arrangem ents of horizons
whose colour, texture, structure, consistence, thickness,
reaction, and composition fall within a narrow range.
16
SOIL ORDERS IN CENTRAL AND NORTHERN NEW
BRUNSWICK
Bruniso lic Soils
Most Brunisolic soils are well to imperfectly drained and
have developed on either coarse textured glaciofluvial
depo sits, or medium textured old (ancient) alluvial
sedim ents. They have sufficient profile development
to exclude them from the Regosolic order, but lack the
degree or kind of ho rizonation spe cified for other ord ers.
W ithin the mapping area of central and northern New
Brunswick, most Brunisols ca n be considered to be weakly
developed Podzo ls. They tend to have a brownish-coloured
Bm horizon which has an accumulation of illuvial Al and Fe
compounds and o rganic matter under a whitish-gray eluvial
Ae horizon. Significant areas of Dystric Brunisols occur
under virgin conditions. Materials are acidic and lack any
well developed mineral-organic surface horizon. Eluviated
Dystric Brunisol and Gleyed Eluviated Dystric Brunisol
(Fig. 6a) subgroups are present. Some of the Gleyed
Eluviated Dystric Brunisols are poorly drained coarse
textured glaciofluvial, marine or mora inal till sediments.
They have evidence of gleying but it is too weakly expressed
to meet the spe cifications of Gleysolic soils.
Gley solic Soils
Soils of the Gleysolic order have features indicative of
perio dic or prolonged saturation with water and reducing
conditions. They are associated with either a high groundwater table at some period of the year or temporary
saturation above a relatively imp erme able layer. Gleysols
occupy poorly drained landsc ape positions, lower slop es,
toes and d epressions in rolling and hilly top ography, and
depression to mid-slope and sometimes even upper slope
sites in level to gently undulating topography. Soil horizons
are subd ued in app earan ce and ma y be difficult to
differentiate due to the gleyed and/or mottled conditions
throughout the profile. Hydrophytic vegetation and surface
peaty layers are commonly associated features, although not
diagnostic. Gleysol, Humic Gleysol and Luvic Gleysol great
groups occur. They are separated on the basis of the
presence or absence of an Ah or Bt horizon. The following
subgroup members were identified as occurring within the
study area: Orthic Gleysols (Fig. 6b), Rego G leysols, Fera
Gleysols, Orthic Humic G leysols, Rego Hu mic Gleyso ls,
Orthic Luvic Gleysols, Humic Luvic Gleysols and Fera
Luvic Gleysols. With exception of organic so ils, Gleyso ls
have developed in every so il parent material type and almo st
all mappe d soil associations.
Luvisolic Soils
W ell to imperfectly drained mem bers o f several soil
associations are classified as Luvisols.
They have
developed in fine loam y morainal tills and clayey marine
sediments. Luviso ls are characterized by the presence of an
illuvial Bt horizon in which silicate clay has accumulated.
Clay suspended in the soil solution is moved do wnward in
the soil profile from the surface layers to a depth were the
soil solution ceases to mo ve or movement becomes very
slow. In the central and northern New Brunswick area,
Luviso lic soil development is for the most part weakly
expressed. The typical Luviso lic characteristics of a
mod erate to strong prismatic or blockly structured Bt
horizon and so lum of high base satura tion are not present.
W ithin the study area Luviso lic soil developm ent is most
pronounced in materials of neutral reaction, ie. the Caribou,
Carleton and T racad ie associations. Due to clima tic
conditions, only members of the Gray Luvisolic great group
are found . The subgroup s occurring within the study area
are:
Orthic G ray Luvisols, Gleyed Gray Luvisols,
Bru nisolic Gray Luviso ls, Gleyed B runisolic Gray Luvisols,
Podzo lic Gray Luvisols (Fig. 6c), and G leyed P odz olic
Gray Luvisols. The Podzolic Gray Luvisols are
"transitional" in that they have bisequal profile development
with a podzolic B horizon formed over the luvisolic Bt
horizon.
The B runisolic Gray Luvisols and Gleyed
Bru nisolic Gray Luviso ls can be considered to be "juvenile"
counterparts of the Podzolic Gray Luvisols and Gleyed
Pod zolic Gra y Luvisols.
Or gan ic Soils
Organic soils are composed largely of organic materials,
including soils commonly known as peats, mucks, bogs and
swamp s. They occur in poorly and very poorly drained
depressions and level areas saturated with water for
prolonged perio ds, and are derived from hydrophytic
vegetation (mosses, sedges, shrubs, etc.) that grow in such
sites. Organic soils have at least 40 cm of organic material,
with some hav ing in excess of 5 m. Organic so ils found in
the study area fall into the Fibrisol, Mesisol and Humisol
great groups. These subdivisions are based upon the degree
of deco mpo sition o f the organic material. The following
subgroups occur: Typic Fibrisols (Fig. 6d), M esic
Fibrisols, Terric Fibrisols, Hum ic Me sisols, Terric M esisols,
Terric Fibric Mesisols, T erric H umic M esisols, M esic
Humisols, T erric H umiso ls and T erric M esic H umiso ls.
Podzo lic Soils
In central and northern New Brunswick mo st of the we ll to
imperfectly drained mineral soils are members of the
Podzo lic order. See Table 1. This includes soils developed
in morainal till, marine, residual, glaciofluvial and ancient
alluvial parent materials. Podzo lization is the dominant type
of soil form ation in the regio n. The prevailing cool to cold,
humid to perhumid climatic conditions coupled with the
influence of forest/heath vegetation, is cond ucive to
pod zolic soil deve lopm ent. These soils are characterized by
the following horizon sequence: The surface L, F and H, or
possibly Of or Om horizo n, is underlain by a thin
discontinuous dark coloured Ah horizon and then by a light
ashy coloured eluvial Ae horizon . The Ae horizon breaks
abruptly into a reddish brown to almost black B horizon that
grades into a slightly modified BC horizon and then into the
parent material “C”). The podzolic B contains illuvial Fe, Al
and organic matter. It is the diagnostic horizon in terms of
morphological and chemical requirements. These and other
17
(a)
(b)
(c)
(d)
(e)
(f)
Figure 6. D iagrammatic horizon p atterns of various soil profiles.
technical criteria are detailed in the Canadian System of Soil
Classification (Soil Classification Working Group 1998).
The Podzo lic order is divided into great groups on the basis
of organic carbon content and related p roperties. B oth
Humo-F erric and Ferro-Humic P odzols are present. Six
subgroups occu r: Orthic Humo-F erric P odz ols (Fig. 6e),
Gleyed Hum o-Ferric Podzo ls, Fragic H umo-Fe rric Pod zols,
Luviso lic Hum o-Ferric Podz ols, Orthic Ferro-H umic
Podzo ls and G leyed F erro-Hum ic Po dzo ls. Som e poorly
drained soils have gley features but also a podzolic B
18
Table 1. Soil association members of the central and northern New Brunswick map area classified according to the Canadian System of
Soil Classification (1998)
Soil Association
Mode of
Deposition
Rapidly to Mod. Well
Drained
CSSC Subgroup(s)
Imperfect
Drained
Acadie Siding
Paludification
----
----
T.M, TFI.M, THU.M (T.H,
T.F)
Barrieau-Buctouche
Marine over
morainal till
O.HFP
GL.HFP, GLE.DYB
O.G, FE.G
Belldune River
Marine
O.HFP
GL.HFP
O.G, FE.G
Big Bald Mountain
Residual
O.HFP
GL.HFP
----
Boston Brook
Morainal till
O.HFP
GL.HFP
O.G
Caribou
Morainal till
PZ.GL, LU.HFP
GLPZ.GL, GLBR.GL
O.LG, O.HG
Carleton
Morainal till
PZ.GL, LU.HFP (O.HFP)
GLPZ.GL, GL.HFP
O.LG, O.G
Catamaran
Morainal till
O.HFP
GL.HFP
O.G, FE.G
Gagetown
Glaciofluvial
O.HFP, E.DYB
GL.HFP, GLE.DYB
GL.HFP, GLE.DYB, O.G
Grand Falls
Glaciofluvial
O.HFP
GL.HFP
GL.HFP, GLE.DYB, O.G,
R.G
Guimond River
Glaciofluvial
O.HFP, E.DYB
GL.HFP, GLE.DYB
GL.HFP, GLE.DYB, O.G
Holmesville
Morainal till
O.HFP
GL.HFP
O.G, FE.G
Interval
Alluvium
O.R, CU.R
GL.R, GLCU.R
R.G, R.HG
Jacquet River
Morainal till
O.FHP, O.HFP
GL.HFP
O.G, FE.G
Juniper
Morainal till
O.HFP
GL.HFP
O.G, FE.G, O.HG
Lavillette
Paludification
----
----
TY.F, ME.F
Long Lake
Morainal till
O.FHP, O.HFP
GL.HFP
O.G
Maliseet
Alluvium (ancient)
O.HFP
GL.HFP, GLE.DYB
GLE.DYB, O.G, R.HG
McGee
Morainal till
O.FHP, O.HFP
GL.HFP
O.G, R.G
Muniac
Glaciofluvial
O.HFP
GL.HFP
GL.HFP, GLE.DYB, O.G,
R.HG
Nigadoo River
Morainal till
O.FHP, O.HFP
GL.HFP
O.G, FE.G
Parleeville
Morainal till
O.HFP
GL.HFP
GLE.DYB, O.G
Popple Depot
Morainal till
O.FHP, O.HFP
GL.HFP
O.G, FE.G
Reece
Morainal till
O.HFP, FR.HFP
GL.HFP
FE.G
Richibucto
Marine
O.HFP, E.DYB
GL.HFP, GLE.DYB
GLE.DYB, O.G
Riverbank
Glaciofluvial or
Alluvial (ancient)
O.HFP
GL.HFP
GLE.DYB, O.G, FE.G
Poor to Very Poor
Drained
19
Table 1. Soil association members of the central and northern New Brunswick map area classified according to the Canadian System of
Soil Classification (1998) cont’d
Soil Association
Mode of
Deposition
Rapidly to Mod. Well
Drained
CSSC Subgroup(s)
Imperfect
Drained
Poor to Very Poor
Drained
Rogersville
Morainal till
O.HFP, FR.HFP, PZ.GL
GL.HFP, GLPZ.GL
O.LG, FR.LG
St. Quentin
Paludification
----
----
T.M, THU.M, T.H, TME.H
(ME.H, HU.M)
Stony Brook
Morainal till
PZ.GL, LU.HFP
GLPZ.GL, LU.HFP
O.LG, FE.LG
Sunbury
Morainal till
O.HFP
GL.HFP
GL.HFP, GLE.DYB, O.G
Tetagouche
Morainal till
O.HFP, O.FHP
GL.HFP
O.G, FE.G
Tetagouche Falls
Morainal till
O.HFP, O.FHP
GL.HFP
O.G, FE.G
Thibault
Morainal till
O.HFP
GL.HFP
O.G, FE.G
Tracadie
Marine or
Glaciolacustrine
O.GL, BR.GL
GL.GL, GLBR.GL
O.LG
Tuadook
Morainal till
O.FHP, O.HFP
GL.HFP
O.G, FE.G
Violette
Morainal till
O.HFP, PZ.GL
GL.HFP, GLPZ.GL
O.G, O.LG
Brunisols
E.DYB
GLE.DYB
Eluviated Dystric Brunisol
Gleyed Eluviated Dystric
Brunisol
Gleysols
O.G
FE.G
R.G
O.LG
FE.LG
HU.LG
O.HG
R.HG
Orthic Gleysol
Fera Gleysol
Rego Gleysol
Orthic Luvic Gleysol
Fera Luvic Gleysol
Humic Luvic Gleysol
Orthic Humic Gleysol
Rego Humic Gleysol
Luvisols
O.GL
GL.GL
BR.GL
GLBR.GL
PZ.GL
GLPZ.GL
Orthic Gray Luvisol
Gleyed Gray Luvisol
Brunisolic Gray Luvisol
Gleyed Brunisolic Gray Luvisol
Podzolic Gray Luvisol
Gleyed Podzolic Gray Luvisol
Organics
TY.F
T.F
ME.F
HU.M
T.M
TFI.M
THU.M
T.H
ME.H
TME.H
Typic Fibrisol
Terric Fibrisol
Mesic Fibrisol
Humic Mesisol
Terric Mesisol
Terric Fibric Mesisol
Terric Humic Mesisol
Terric Humisol
Mesic Humisol
Terric Mesic Humisol
Podzols
O.FHP
GL.FHP
O.HFP
GL.HFP
FR.HFP
LU.HFP
Orthic Ferro-Humic Podzol
Gleyed Ferro-Humic Podzol
Orthic Humo-Ferric Podzol
Gleyed Humo-Ferric Podzol
Fragic Humo-Ferric Podzol
Luvisolic Humo-Ferric Podzol
Regosols
O.R
GL.R
CU.R
GLCU.R
Orthic Regosol
Gleyed Regosol
Cumulic Regosol
Gleyed Cumulic Regosol
horizon. The podzolic B horizon takes precedence and the
soils are classified as gleyed subgroup mem bers of the
Podzo lic order.
Regosolic So ils
Regosolic soils are weakly developed. The Regoso lic soils
mapped in central and northern New B runswick lack
development of genetic horizons due to the youthfulness of
the material in which they are form ing, recent alluvium.
20
They are found along river and stream flood plains
throughout the study area. T he mo st pronoun ced soil
development is in the surface layer where a thin organic-rich
Ah horizo n is often p resent. Soil development in the rest of
the profile is usually co nfined to changes in colour due to
mottling or gleying. Buried mineral-organic layers and
organic surface horizons may also be found. Only members
of the Re goso l great group occu r. They are: Orth ic
Rego sols, Gleyed Regosols, Cumulic Regosols (Fig. 6f) and
Gleyed Cumulic Regoso ls. Collivial sites, with ac tive soil
deposition as a result of mass-wasting, usually at the base of
steep slopes, may also have regosolic profiles. However,
these sites are localized and have been included with glacial
till soils.
I M P A C T O F A G R IC U L T UR E
CLASSIFICATION
ON
S O IL
W hen land is brought into agricultural production the upper
profile sequence of mineral and organic horizons are mixed
together during cultivatio n to form an A p horizon. Soil
solum horizo ns are, in w hole or in part, incorporated into the
plow layer. Sinc e soils are classified on the basis of
diagnostic horizons that are in the soil solum, the
classification of a virgin soil profile may be different than
that of its cultivated counterp art. W ithin the survey area the
dep th of solum developme nt averages 40 to 50 cm. The
more strongly developed horizons are usually in the upper
solum near the surface. On average the furrow slice, that
portion of the soil turned or sliced by the plow, varies from
20 to 25 cm in thickness. This can account for 40 to 65% of
the average so lum thickness.
Cultivation of a soil can affect classification at the highest
taxa, the order and great grou p levels. Ferro -Hum ic Po dzo ls
are often altered to Humo-Ferric Podzols, Humo-Ferric
Podzols to Sombric Brunisols, and D ystric Brunisols to
either Som bric B runiso ls or Regosols. Subgroup
classifications are also affected . For example, P odz olic
Gray Luvisols often beco me B runisolic Gra y Luviso ls when
cultivated. This type of variation in classification between
cultivated and noncultivated conditions is dependent on the
nature of development of the soil involved and the degree of
disturbance it is subjected to. Many cultivated soils retain
their pre-cultivated classification status, others do not.
RELATIO NSH IP
BETW EEN
CLASSIFICATION AND SOIL MAPPING
SO IL
Soil mapping is the identification, description and
delineation on a m ap of contrasting segm ents of the
landscape based on a set of established differentiating
criteria. Soil mapping should not be confused with so il
taxonomy or classification. Soil classification systems are
methods of organizing information and ideas about soil in a
logical and useful manner. Even though map units are
described in terms of taxono mic classes, the mapping units
are not the same as so il taxa. The purp oses of soil
classification are:
to provide a framework for the
formulation of hypotheses about soil genesis and the
response of soil to management; to aide in extending
knowledge of soils gained in one area to other areas having
similar soils; and to provide a basis for indicating the kinds
of soils within mapping units (Canada Soil Survey
Committee, 1978)
The soils of the central and northern New Brunswick area
are mapped at the exploratory scale of 1:250,000. T he soil
association was used as the basic unit for soil mapping and
description. The soil associatio n is a grouping of soils that
have developed on similar parent material under similar
climatic conditions but vary in drainage d ue to to pog raphic
relief. The soil association is a broadly enough defined unit
to encompass the variation and range of soils that are
encountered within landscape units commensurate with the
1:250,000 scale of mapping.
Soil associations may co nsists of several subgroups (T able
1). Where patterns of soil development are simple, the
mapping units may consist of one associate (member of an
association) and possibly only one subgroup. These units
are relatively pure taxonomically speaking. In other areas
the com plexity of the landscape is such that soils with
contrasting properties cannot be separated and must be
included in the sam e unit. It is not p ossible to show the
geographic location of these different soils, but rather they
are complexed on the map. These units consist of two or
more associates. Since the Canadian System o f Soil
Classification is a national system designed to group
different soils across the entire co untry (ie. the whole
population of soils), it is understandable that in some regions
the soils have pro perties that strad dle the boundary line
between two taxa. For example, the well drained associate
of the McG ee Associatio n contains bo th Orthic Humo -Ferric
Podzo ls and Orthic Ferro-Humic Po dzols. These soils have
properties that are close to the taxono mic class bounda ry.
Drainage variations also result in differences in taxa at the
higher levels of classification for soils that are loca ted in
close proximity to each other. Well and imperfectly drained
Ho lmesville Association mem bers a re bo th Po dzo ls while
their poorly draine d counterp arts are Gleysols. Intrica te
drainage patterns are common and therefore so are complex
map units with two or more taxa.
21
PART 3. SOIL MAPPING METHODOLOGY
OFFICE METHODS
Initial efforts consisted of compiling existing information on
the physical resources of the study area that would be useful
to pred ict soil properties and distribution. Information was
collected on climate, vegetation, geology, physiography, and
geomorpho logy. This included bedrock and surficial
geology m aps, topo graphic maps, climatic parameter maps
(temperature, precipitation, etc.) and forest cover type m aps.
Previous soil map ping within the study area and soil survey
repo rts and ma ps from adjoining areas (See Fig. 1), were
used extensively to establish a preliminary field mapping
legend or key. A brief reconnaissance of the area was used
to corro borate the validity of the legend. Discrepancies were
rectified acco rdingly, additions were made were necessary,
and the preliminary legend was finalized.
Pho to interpretation played a major role in delineating the
various soil-landscape units. Aerial photographs taken
between 1976 and 198 1 at a scale of 1:63,360 were
interpreted in terms o f soil-landform patterns relevant to
soils mapping at the exploratory (1:250,000) level of
intensity. Tentative delineations were made on the basis of
major landforms. To pog raphic map s (1:50,00 0 scale with
25 or 50 ft contour intervals) were used to check the
accuracy of the delineation boundary lines and the
landform-slope designations. Surficial and bedrock geology
and photo interp retation were used to estimate soil parent
materials types. Aerial photographs were the basic tool used
to locate observation sites for ground truthing the predicted
map p olygons.
The majo r landfo rms (d efined as includ ing bo th materials
and form) used to stratify the survey are were:
1. Morainal sedim ents of comp act or non-compact glacial
till (lodgment and ablational) consisting of a nonstratified,
hetero geneous m ixture of particle sizes ranging from sand,
silt, and clay to gravels, cobbles, stones, and boulders; 10
cm to more than 10 m thick, but usually less than 3 m thick;
sandy, coarse loamy or fine loamy, with skeletal variations;
hilly, hummocky, ridged and sloping to rolling, undulating
and level.
2. Resid ual sed iments of unconsolidated or partly weathered
bedrock developed in place from the underlying
consolidated rock ; veneer (10 cm to 1 m thick); sandy
skeletal; rolling.
3. Fluvial sedime nts consisting of mode rately to well sorted
and stratified rounded gravels (and sometime cobbles),
sands, silts and occasionally clays deposited by flowing
water, both past and present (ie. glaciofluvials and alluvials);
usually more than 2 m thick a nd freq uently as m uch as 20 to
30 m thick; sa ndy ske letal, sand y or co arse loamy; level to
undulating or slop ing terraces, kame s, eskers, deltas and
floodplains.
4. Ma rine sediments of clay, silt and sand that are well to
mode rately well sorted and stratified as a result of having
settled from suspension in salt or brackish water, or having
accumulated through shoreline processes such as wave
action and lo ngsho re drift; ranging from thin discontinuous
veneers over bedrock or morainal depo sits, to in excess of
50 m thick; sa ndy, co arse loamy o r clayey; level to gently
undulating.
5. Colluvial sediments of nonsorted particle size classes
ranging from clay to boulders that are products of
mass-wasting and are the result of gravity-induced
mov ement; usually less than 1 m thick, commonly overlying
the Pleistocene till materials from which they have been
derived; coarse loamy to fine loam y, with skeletal variations;
hilly, sloping or hummocky. NOT E: In the final compilation
colluvial sediments were grouped with morainal deposits
due to there similarities and intermixed distributions.
6. Organic sediments consist of peat deposits containing
more than 30% organic matter by weight that are derived
from either sphagnum ma terials in an omb rotrophic
environment or sed ge-forest materials in a eutroph ic
enviro nment; at least 40 cm thick, but in excess of 5 m in
some depo sits; fibric, mesic, or humic; dome d, horizontal,
or bowl shaped.
7. Rock co nsists of undifferentiated, indurated materials of
bedrock origin that are at o r near the surfac e; the bedro ck is
at the surface or covered by less than 10 cm of regolith
material, usually glacial drift; igneous, metamorphic or
sedimentary rock; hilly, ridged, sloping or rolling
(associated with upper slope or crest positions).
FIELD METHODS
The conventional or "free mapping" ap proach to
soil-landscape information collection was employed.
Relationships between soils and landforms were established
by observing the soils on strategic points in the landscape,
such as crests, upper slopes, midslopes, lower slopes,
depressions, etc. Once these relationships were established
the frequency of observations was reduced to a relatively
few strategic p oints to verify the soil type or association.
These points were selected under stereoscopic examination
of aerial photographs. Accessibility limited the selection of
these points to locations alo ng road ways, power lines,
22
railroad tracks, etc. Ground accessibility was adequate to
traverse most map units. However, poor accessibility of a
few region s did dictate the use o f a helicopter for additional
field data collection. Field examination p oints were well
distributed throughout the area with at least one observation
point in 70 to 80% of the delineations. While intensity of
observations was heavily dep endent on accessibility, it also
varied with simplicity or complexity of the soil-landform
relationships. In complex areas the number of field checks
required to verify material co mpo sitions and distrib utions
was greater than in areas of more uniform soil develop ment.
Field inspec tions provid ed ground -truth data to improve the
quality and accuracy of the soil map. Information and
boundaries for soil-landscape units were extrapolated from
areas with ground inspections by interpretation of the aerial
photograp hs. In most cases a pit was dug by shovel to
expose the soil profile. Road cuts, gravel/fill pits and other
excavations were used to supplement profile data. Soil
observations in mineral soils were made to a depth of 1 m,
or to a lithic (bedrock) contact in shallow soils. Organic
soils were examined to a depth of 1.6 m , or to a mineral soil
contact, whichever was less. Each observation was described
in terms of specific soil and site criteria. Descriptions and
classifications were in accordance with procedures
established in the Canadian System of Soil Classification
(Soil Classification W orking Group 1998). Soil parameters
included: horizon or layer designations, depths, colour,
structure, consistence, mottles were present, reaction class,
texture and coarse fragme nt type and co ntent. Site
information consisted of: parent material mode of
deposition, surface exp ression, slope cha racteristics,
drainage and moisture regime, erosion features, surface
stoniness, depth to bedrock, land use and vegetation.
A number of representative soil profiles were described in
detail and sampled for laboratory analysis to characterize the
soil in terms of selected physical and chem ical prope rties.
Parameters in parentheses - material thickness, bo ulderiness
and rockiness - are only indicated in map symbols where
relevant.
The soil association is a natural group ing of so ils based on
similarities in climatic or ph ysiographic factors and so il
parent material. In this context it is similar to the concept of
the soil catena, in that it is a sequence of soils of about the
same age, derived from similar parent material, and under
similar climatic conditions, but having unlike characteristics
because of variations in relief and draina ge. T hirty six soil
associations are mapp ed. The soil associations are listed
alpha betically in the legend (Tab le 2) and described in terms
of: mode of deposition, description of the soil parent
material (family particle size class, compactness, reaction,
coarse fragme nt content, lithology), surface form and
physiographic region. This information is expanded upon in
the report (Part 4).
The remainder of the symbol is used to describe phases (ie.
material thickness, drainage, surface expression, slope,
boulderiness, rockiness). Phases describe characteristics that
are sp ecific to a given d elineatio n.
M aterial thickness indicates the average thickness of
regolith or soil material overlying solid bedrock.
Drainage refers to the actual moisture content in excess of
field capacity and the extent of the period during which such
excess water is present in the control section. For example,
in well dra ined so ils excess water flows do wnward rea dily
into underlying pervious material, or laterally as subsurface
flow. The water source is precipitation. In contra st, in poo rly
drained soils the water is removed so slow ly in relation to
supp ly that excess water is evident in the soil for a large part
of the time. W ater sources are subsurface and/or
groundwater flow in addition to precipitation. Established
drainage classes (Expert Committee on Soil Survey, revised
1982) of excessive, well, moderately well, imperfect, poor
and very poor are groupe d into seven d rainage catego ries.
MAP SYMBOL
The map symbol is the link between the soil map and the
repo rt. It is designed to convey information about the soils
and map units to the reader or user. M apped soil and nonsoil portions of the landscape are delineated on the soil map.
These delineations or polygons are labelled on the map by
a symbol which is made up of letters and numbers
representing classes of selected soil and landscape
properties. Descriptions or explanations for the various
com pon ents of the map symbol are provided in the map
legend (Table 2). The map symbol used for the purpose of
this survey is typically as follows:
Soil Association(s) (M aterial Thickness) Drainage
Surface Exp ression Slope (B oulder iness) (Ro ckiness)
Surface expression signifies a unique surface form
(assemblage of slopes) or pattern of forms that are repeated
in nature. For example, rolling is a very regular sequence of
mod erate slopes extend ing from rounded , sometimes
confined concave depressions to broad, rounded convexities
producing a wavelike p attern of mod erate re lief.
Slope quantifies the degree of inclination of the dominant
slopes within the map polygon. Slopes of similar magnitude
are group ed into seven classes expressed in percent slop e.
Boulderiness is defined as the percentage of the land
surface occupied by stones greater than 1 m in diameter.
Rockiness indicates the percen tage of the land surface
occupied by bedrock exposures (or soil material less than 10
cm thick over bedrock).
23
Table 2. Soil mapping legend
Soil Associations and Land Types:
Name
Symbol
Mode of
Deposition
Description of Soil Parent Material
Surface Form
Physiographic
Region
Acadie
Siding
AS
Paludification
40 to 160 cm of acidic, brown to dark brown,
mesic and humic sedge-sphagnum peats over
undifferentiated mineral soil deposits.
Flat, bowl
or horizontal
Maritime Plain
N. B. Highlands
BarrieauBuctouche
BB
Marine over
morainal till
20 to 100 cm of acidic, yellowish brown to
brown, sandy, noncompact marine sediments
with less than 20% (but usually less than
5%) coarse fragments of mostly gray-green
sandstones over acidic, yellowish brown to
dark reddish brown, loamy compact till with
15 to 20% coarse fragments of mostly gray-green
sandstone.
Undulating to
level blanket
or veneer
Maritime Plain
Belldune
River
BR
Marine
Acidic, reddish brown to yellowish brown
coarse loamy to sandy skeletal, noncompact, material
with 15 to 50% coarse fragments of conglomerate,
sandstone, siltstone, argillite and some limestone.
Undulating
Chaleur Uplands
Big Bald
Mountain
BM
Residual
Acidic, yellowish brown, sandy skeletal,
noncompact material with 15 to 50% coarse fragments
derived from feldspar rich granite weathered in situ.
Hilly to rolling
veneer
N .B. Highlands
Boston
Brook
BO
Morainal till
Acidic, olive to olive brown, fine loamy
(skeletal), noncompact, (but slightly firm),
material with 10 to 30% coarse fragments of
argillite, slate and fine-grained sandstones.
Rolling to hilly
veneers and
blankets
Chaleur Uplands
Caribou
CB
Morainal till
Neutral, olive to olive brown, fine loamy
noncompact (but slightly firm in the Bt and
C) material with 10 to 30% coarse fragments of
calcareous shale, argillite and slate and
some limestone.
Undulating,
rolling, hilly
sloping
blanket and
veneers
Chaleur Uplands
Carleton
CR
Morainal till
Neutral, olive to yellowish brown, fine loamy,
compact material with 10 to 30% coarse fragments
of calcareous shale, argillite and slate and
some calcite.
Rolling, undulating,
hilly and sloping
blankets and veneers
Chaleur Uplands
Catamaran
CT
Morainal till
Acidic, yellowish brown to olive brown,
coarse loamy, compact material with 10 to 25%
coarse fragments of granite, schist, quartzite,
slate and sandstone.
Rolling, undulating,
hilly and sloping
blankets and veneers
N. B. Highlands
Gagetown
GG
Fluvial
(Glaciofluvial)
Acidic, yellowish brown to brown, sandy
skeletal, noncompact sediments with 35 to 70%
coarse fragments of mixed igneous and
metamorphic and miscellaneous sedimentary
rocks.
Terraced,
undulating
and hummocky
N. B. Highlands
Maritime Plain
Grand
Falls
GF
Fluvial
(Glaciofluvial)
Acidic, olive to olive brown, sandy skeletal
noncompact sediments with 35 to 70%
fragments of noncalcareous slate, shale,
quartzites and sandstones.
Terraced
and hummocky
N. B. Highlands
Chaleur Uplands
Notre Dame Mtn
24
Table 2. Soil mapping legend cont’d
Name
Symbol
Guimond
River
GM
Mode of
Deposition
Physiographic
Region
Description of Soil Parent Material
Surface Form
Fluvial
(Glaciofluvial)
Acidic, olive to yellowish brown, sandy
skeletal, noncompact sediments with 35 to 70%
coarse fragments of soft gray-green sandstone.
Terraced,
undulating
and hummocky
Maritime Plain
Holmesville HM
Morainal till
Acidic, olive to olive brown, coarse loamy,
compact material with 10 to 30% coarse fragments
of quartzite and sandstones and miscellaneous
argillite, slate and schist.
Rolling, undulating
and hilly blankets
and veneers
Chaleur Uplands
Notre Dame Mtn
N. B. Highlands
Interval
IN
Fluvial
(Alluvial)
Acidic to neutral, olive to yellowish brown,
stratified coarse loamy and sandy, noncompact
sediments with very few coarse fragments of
undifferentiated lithologies.
Terraced and
undulating to level
Maritime Plain
N. B. Highlands
Jacquet
River
JR
Morainal till
Acidic, yellowish brown, coarse loamy,
noncompact material with 20 to 40% coarse
fragments of rhyolite and trachyte, with some
basalt and miscellaneous slate and greywacke.
Undulating to hilly
blankets and veneers
N. B. Highlands
Chaleur Uplands
Juniper
JU
Morainal till
Acidic, yellowish brown to brown, coarse loamy
to sandy (skeletal), noncompact material
with 20 to 50% coarse fragments of granite, granodiorite, diorite, granite gneiss and
miscellaneous volcanics.
Rolling and
hilly veneers and
blankets or
undulating to
hummocky
N. B. Highlands
Lavillette
LV
Paludification
Acidic, brown to dark reddish brown, fibric
(and minor mesic) sphagnum peats usually
thicker than 1.6 m over undifferentiated mineral
soil deposits.
Domed
Maritime Plain
Long Lake
LL
Morainal till
Acidic, olive brown, coarse loamy, compact
material with 20 to 40% coarse fragments of slate,
siltstone, argillite, schist and miscellaneous
quartzite and greywacke.
Rolling, hilly
and undulating
blankets and
veneers
N. B. Highlands
Chaleur Uplands
Maliseet
MA
Fluvial
Acidic, olive to yellowish brown, stratified
(Ancient alluvial) sandy to coarse loamy, noncompact sediments
with less than 10% coarse fragments of slate,
shale miscellaneous quartzite and volcanics.
Level and
terraced
Chaleur Uplands
Notre Dame Mtn
McGee
MG
Morainal till
Acidic, olive to olive brown, coarse loamy
(skeletal), noncompact material with 20 to 50%
coarse fragments of slate, argillite, schist,
greywacke and quartzite.
Rolling, hilly
and sloping
blankets and
veneers
N. B. Highlands
Chaleur Uplands
Notre Dame Mtn
Muniac
MU
Fluvial
(Glaciofluvial)
Neutral, olive to olive brown, sandy skeletal
noncompact sediments with 35 to 70%
fragments of calcareous slate, shale,
quartzites and sandstones.
Terraced
and hummocky
Chaleur Uplands
Nigadoo
River
NR
Morainal till
Acidic, yellowish brown, coarse loamy, compact
material with 15 to 30% coarse fragments of
metagabbro and metabasalt, with some granites,
conglomerate and metagreywacke.
Variable - undulating,
rolling, hilly, ridged
and hummocky
veneers and blankets
Chaleur Uplands
N. B. Highlands
Parleeville
PA
Morainal till
Acidic, dark reddish brown, coarse loamy,
noncompact material with 15 to 30% coarse
fragments of sandstone and conglomerate.
Rolling and
undulating
blankets and
veneers
Chaleur Uplands
N. B. Highlands
25
Table 2. Soil mapping legend cont’d
Name
Symbol
Mode of
Deposition
Popple
Depot
PD
Reece
Physiographic
Region
Description of Soil Parent Material
Surface Form
Morainal till
Acidic, yellowish brown to olive brown, coarse
loamy (skeletal), compact material with 20 to 40%
coarse fragments of rhyolite and trachyte, with some
basalt and miscellaneous slates and greywacke.
Rolling, hilly
and sloping
veneers and
blankets
N. B. Highlands
Chaleur Uplands
RE
Morainal till
Acidic, strong brown to dark yellowish brown, loamy,
compact material with 10 to 25% coarse fragments
of soft gray-green sandstone and miscellaneous
remnants of highly weathered shale.
Undulating
blankets and
veneers
Maritime Plain
Richibucto
RB
Marine
Acidic, yellowish brown to brown, sandy, noncompact sediments with less than 20% (but
usually less than 2%) coarse fragments of
soft gray-green sandstone.
Undulating and
level veneers,
blankets and
thicker deposits
Maritime Plain
Riverbank
RI
Fluvial
(Mixture of
glaciofluvials
and alluvials)
Acidic, yellowish brown to olive brown, sandy
noncompact sediments with less than 20% (but
usually less than 2%) coarse fragments of mixed
igneous, metamorphic and minor amounts of
sedimentary rock types.
Terraced and
level
Maritime Plain
N. B. Highlands
Rogersville RS
Morainal till
Acidic, brown, fine loamy, compact material
with 10 to 25% coarse fragments of sandstone,
granites, gneiss, schists and some volcanics and
miscellaneous remnants of highly weathered shale.
Undulating
blankets
Maritime Plain
Salt Marsh
SM
Marine
Undifferentiated marine deposits along
coast or tidal river, submerged at high tide
by salt water
Level
Maritime Plain
Chaleur Uplands
Sand Dune
SD
Aeolian
Low ridges of loose windblown sand along
the coast
Ridged
Maritime Plain
Chaleur Uplands
St. Quentin SQ
Paludification
Usually less than 160 cm of neutral, dark
brown, forest-fen peats over undifferentiated
mineral soil deposits.
Flat, bowl
and horizontal
Chaleur Uplands
Stony
Brook
SB
Morainal till
Acidic, red to reddish brown, fine loamy,
compact material with 10 to 25% coarse fragments
of soft gray-green sandstone and miscellaneous
remnants of highly weathered shale.
Undulating and
level blankets
and veneers
Maritime Plain
Sunbury
SN
Morainal till
Acidic, yellowish brown to brown, coarse loamy
to sandy (skeletal), noncompact material with
15 to 35% coarse fragments of soft gray-green
sandstone.
Undulating
blankets and
veneers
Maritime Plain
Tetagouche TT
Morainal till
Acidic, strong brown, fine loamy, compact
material with 10 to 25% coarse fragments of
metagabbro, metabasalt, metagreywacke and
conglomerate.
Undulating and
rolling with some
ridged and hilly
blankets and veneers
Chaleur Uplands
Tetagouche TF
Falls
Morainal till
Acidic, strong brown, loamy, noncompact
material with 15 to 35% coarse fragments of
metagabbro, metabasalt, metagreywacke and
conglomerate.
Rolling to hummocky
or ridged and hilly
veneers, blankets and
deeper phases
Chaleur Uplands
N. B Highlands
Thibault
Morainal till
Neutral, light olive brown, coarse loamy, noncompact material with 10 to 35% coarse fragments
of weakly calcareous shale, slate, quartzite,
argillite and sandstone.
Rolling and hilly
blankets and
veneers
Chaleur Uplands
Notre Dame Mtn
TH
26
Table 2. Soil mapping legend cont’d
Name
Symbol
Tracadie
TC
Tuadook
Mode of
Deposition
Physiographic
Region
Description of Soil Parent Material
Surface Form
Marine or
glaciolacustrine
Neutral, red to yellowish brown, clayey,
compact sediments with less than 2% coarse
fragments of undifferentiated lithologies.
Level and
undulating
blankets and
deeper phases
Maritime Plain
TU
Morainal till
Acidic, yellowish brown to brown, coarse loamy
(skeletal), compact material with 15 to 35% coarse
fragments of granite, granodiorite, diorite,
granite gneiss and miscellaneous volcanics.
Rolling, hilly
and sloping
blankets and
veneers
N. B. Highlands
Violette
VO
Morainal till
Acidic, light olive brown, fine loamy, compact
material with 10 to 25% coarse fragments of
quartzite, sandstone and miscellaneous shale,
argillite and slate.
Rolling, undulating
and hilly veneers
and blankets
Chaleur Uplands
N. B. Highlands
Water
WA
-
Small unnamed water bodies
-
All regions
Material Thickness:
v - veneer, less than 1 m to bedrock.
b - blanket, 1 to 2 m to bedrock.
Where no material thickness is indicated it can be assumed to be greater than 2 m.
Drainage:
1234567-
excessively, well and/or moderately well drained (greater than 80% of the area)
dominated ( greater than 40%) by excessively, well and/or moderately well drained with significant (20-40%) imperfectly drained
dominated by excessively, well and/or moderately well drained with significant poorly drained
dominated by imperfectly drained with significant excessively, well and/or moderately well drained
dominated by imperfectly drained with significant poorly and/or very poorly drained
dominated by poorly and/or very poorly drained with significant imperfectly drained
poorly and/or very poorly drained
Surface Expression:
h - hummocky: a complex sequence of slopes extending from somewhat rounded depressions or kettles of various sizes to irregular to conical knolls
and knobs. Elevation differences are usually less than 100 m.
I - inclined: a sloping, unidirectional surface with a general constant slope not broken by marked irregularities.
l - level: a flat or gently sloping, unidirectional surface with a generally constant slope not broken by marked elevations and depressions. Slopes
are generally less than 2%.
m - rolling: a very regular sequence of moderate slopes extending from rounded, sometimes confined concave depressions to broad rounded
convexities producing a wavelike pattern of moderate relief. Slope length is often 1.6 km or greater and gradients are greater than 5%.
r - ridged: a long, narrow elevation of the surface, usually sharp crested with steep sides.
s - sloping: an inclined multi-directional surface with variable slopes broken by marked irregularities.
t - terraced: a scarp face and the horizontal or gently inclined surface (tread) above it.
u - undulating: a very regular sequence of gentle slopes that extends from rounded, sometimes confined concavities to broad rounded convexities
producing a wavelike pattern of low local relief. Slope length is generally less than 0.8 km and the dominant gradient of slopes is 2-5%.
y - hilly: a very complex sequence of slopes extending from weakly to moderately incised depressions of various sizes to somewhat rounded crests
and peaks. Elevation differences are usually greater than 100 m.
An asterisk following the surface expression (eg. m*, etc.) indicates that the landform is significantly dissected by steeply incised drainage channels.
27
Table 2. Soil mapping legend cont’d
Slope:
Class
1
2
3
4
5
6
7
8
9
Rockiness:
% Slope
0-0.5
0.5-2
2-5
5-9
9-15
15-30
30-45
45-70
70-100
Class
R1
R2
Boulderiness:
% Surface
exposed
2-10
10-25
Distance (m)
between exposures
75+
25-75
Class
B1
B2
B3
B4
B5
% Surface
exposed
0.01-0.1
0.1-3
3-15
15-50
50+
Distance (m)
between exposures
30-10
10-2
2-1
1-0.1
less than 0.1
All delineations with exac tly the same symbol constitute a
map unit. Because of the open mapping legend approach
that is used in this soil survey, a majority of map units are
unique. These tend to be the simpler map units. M ap units
may contain one to three soil associations. Simp le map units
consist of 100% of soils that have properties as defined for
the designated so il association. Comp lex map units are used
to describe areas were a second and po ssibly third soil
association is significant in areal abundance, but so
intricately mixed with the dominant soil asso ciation that it
(they) can not be separated out at the 1:250,000 scale of
mapping. In complex map units consisting of two soil
associations, the first or do minan t soil association acco unts
for 70% of the area and the second or significa nt soil
association for 30%. In complex map units consisting of
three soil associations, the first soil association accounts for
50% of the area, the second soil association for 30% of the
area and the third soil association for 20% of the area.
Inclusions are areas of unspecified soil or nonsoil bodies
that occur within delineated map units. Typically up to 15%
of a mapped polygon may consist of inclusions of different
soil materials.
names have been used to indicate the kind of soil and/or nonsoil materials present. Three land types were mapped - salt
marsh, sand dune and water bodies. Where a land type has
been mapped, no additional information is provided on surface
texture, slope, drainage, etc.
The degree of detail that is required o r intended ultim ately
determines the minimum size area that should be depicted
on the soil map. At a mapping scale of 1:250,000, a map
area of 0.5 cm 2 represents 156 ha of land. This is the
smallest area that should be identified on the map, however,
in a few instances, areas smaller than this with highly
contrasting soil and landscape differences, were mapped.
In most of the earlier mapping programs the soil series was the
taxonom ic element employed to describe the mapping units.
The soil series provides more precise information about the
soil mapping unit than does the soil association. This was
appropriate because the scale of mapping of these earlier
surveys was of a more detailed nature (ie, larger scale). The
concept of the soil series has evolved over the years, it is
dynamic. Soil mapping in the Fredericton-Gagetown and
Woodstock areas during the late 1930's employed a concept of
the soil series that was somewhat analogous to a geological
formation based on origin of material, lithology, weathering
and colour, and subdivided into textural classes. This concept
has changed greatly over the years to the present day where the
soil series has precisely defined limits in terms of colour,
texture, structure, consistence, thickness and degree of
expression of horizons and of the solum, abundance of coarse
fragments, depth to bedrock, depth to free carbonates, pH, and
In total, 685 so il polygons were mapped with an average
polygon size of 4060 ha, a minimum polygon size of 37 ha
and a maximum polygon size of 43,236 ha.
Land Types
Natural and man-made units in the landscape that are either
highly variable in content, have little or no natural soil, or are
excessively wet, are referred to as land types. Connotative
SO IL CO RR ELA TIO N W ITH EST AB LISH ED SO IL
CONC EPTS
Soil correlation is the process of maintaining consistency in
naming and classifying soils. Over the years soil survey has
gradually defined and categorized many of the different soils
found in New Brunswick. The central and northern New
Brunswick area shares a common boundary with seven
regional reconnaissance soil survey areas (Fig. 1). Other
detailed or reconnaissance soil survey mapping has also been
conducted within the study area. There is a need to correlate
the soils mapped in these previous studies to the soil legend
used in this report. Table 3 is a summary of the relationships
among the soil associations used in the Exploratory Soil
Survey of Central and Northern New Brunswick and
established soil series from other survey areas in the province.
28
lithology, for mineral soils; and parent material botanical
origin, abundance of logs and stumps, calcareousness, bulk
density, mineral content, soil development, and mineralogy of
the terric layer, for organic soils. A few of the later date
reconnaissance-detailed surveys (ie. Rogersville-Richibucto,
Chipman-Minto-Harcourt) utilized an association-catena type
concept whereby each of the associates (association drainage
members) is basically equivalent to the soil series. Because of
drainage difference, the soil series that form a catenary
sequence can be quite dissimilar in soil profile horizons and
other properties. However, these soil series are closely
associated under field conditions and so the catenary
association is a very practical grouping for mapping the soils
of a region. By convention, the catena-association name is
taken from the name of the most rapidly drained member of the
drainage sequence. Referring to soils on a catenary basis was
also seen as a means of reducing the number of soil names
involved. A Cyr soil is simply referred to as a poorly drained
Grand Falls, a Blackville soil as an imperfectly drained Stony
Brook, and so on.
and land segments that are similar in geomorphic position,
landform, and soil properties. It is an amalgamation of
similar catenary associations. For example, as defined in this
report, the Juniper Association consists of the Juniper catena
(Juniper, Jummet Brook, and McKiel series) and the Irving
catena (Irving, Goodfellow and Halls Brook series). Both
catenas have developed in coarse loamy stony ablation or water
reworked till parent materials derived from gray and red
granites, with some basalts, felsites and volcanics in a rolling
to hilly or sloping landform. The soils and landscape
properties that are used to differentiate the two catenas are not
mappable at the exploratory level of investigation and so they
have been combined into one association, Juniper. The soil
properties for the "new" Juniper Association have ranges that
are broad enough to include both of the former catenas. In
other instances the soil association consists of only one
catenary association ie. the Interval catena (Interval, Waasis
and East Canaan series). Here the association definition is a
generalized catenary association description, expanded as
required to include variations found during mapping.
The soil association concept employed in the central and
northern New Brunsw ick survey area is more broadly defined
than the catenary association. It is a grouping of related soils
Table 3. Correlation of soil associations mapped in central and northern New Brunswick with established soil series as listed in "Soils of New
Brunswick: A First Approximation" (Fahmy et al. 1986)
Soil Association
Rapidly to Mod Well
Drained
Established New Brunswick Soil Series
Imperfectly
Drained
Acadie Siding
Barrieau-Buctouche
Poorly to Very Poorly
Drained
Acadie Siding*
Chelmsford*
Barrieau*
Bretagneville*
St. Charles*
Buctouche*
Cote d'Or
Shediac
Michaud
Neguac
Belldune River
Belldune River*
Durham Centre*
Green Point*
Big Bald Mountain
Big Bald Mountain*
Boston Brook
Boston Brook*
Skin Gulch
Yellow Brook
Caribou
Caribou*
Jardine*
Undine*
Harquail*
Quisibis*
Carlingford
Nickle Mills
Washburn
Five Fingers
Dube
Big Spring
Carleton*
Kedgwick*
Siegas*
Canterbury
Canterbury (Washburn)
Salmon
Bourgoin
Carleton
29
Table 3. Correlation of soil associations mapped in central and northern New Brunswick with established soil series as listed in "Soils of New
Brunswick: A First Approximation" (Fahmy et al. 1986) cont’d
Established New Brunswick Soil Series
Imperfectly
Drained
Soil Association
Rapidly to Mod Well
Drained
Catamaran
Catamaran*
Gagetown
Gagetown*
Geary
Penobsquis
Grand Falls
Grand Falls*
Sirois
Cyr
Guimond River
Guimond River*
Cocagne*
Lord and Foy*
St. Olivier
St. Theodule
Holmesville
Holmesville*
Johnville
Poitras
Interval
Interval*
Waasis
East Canaan
Jacquet River
Jacquet River*
Juniper
Juniper*
Irving*
Jummet Brook
Goodfellow
McKiel
Halls Brook
Lavillette
Poorly to Very Poorly
Drained
Lavillette*
Legaceville*
Long Lake
Long Lake*
Serpentine*
Britt Brook*
Blue Mountain
Adder
Portage Lake
Colter Mountain
Jenkins
Babbit Brook
Maliseet
Maliseet*
Flemming*
Benedict*
Wapske
Martial
Wapske
Kelly
McGee
McGee*
Glassville*
Nason
Temiscouata
Trafton
Foreston
Muniac
Muniac*
Ennishore
Cyr
Nigadoo River
Nigadoo River*
Parleeville
Parleeville*
Midland
Midland
Popple Depot
Popple Depot*
Reece
Reece*
Chipman
Pangburn
Richibucto
Richibucto*
Kouchibouguac*
Bay-du-Vin*
Chockpish*
Caissie*
Galloway*
Babineau*
Escuminac*
Miscou Island*
Cap Lumiere
Potters Mills
Napan
Nevers Road
Vautour
Fontaine
Smelt Brook
Briggs Brook
Riverbank
Riverbank*
Oromocto
Nevers Road
Rogersville
Rogersville*
Acadieville
Rosaireville
Baie-Ste.-Anne
30
Table 3. Correlation of soil associations mapped in central and northern New Brunswick with established soil series as listed in "Soils of New
Brunswick: A First Approximation" (Fahmy et al. 1986) cont’d
Soil Association
Rapidly to Mod Well
Drained
Established New Brunswick Soil Series
Imperfectly
Drained
St. Quentin
Poorly to Very Poorly
Drained
St. Quentin*
Stony Brook
Stony Brook*
Harcourt*
St. Gabriel*
Blackville
Coal Branch
North Forks
Shinnickburn
Grangeville
North Forks
Sunbury
Sunbury*
Big Hole*
Fair Isle*
Hoyt
Beaver Lake
Black Brook
Cork
Tetagouche
Tetagouche*
Tetagouche Falls
Tetagouche Falls*
Thibault
Thibault*
Monquart*
Guercheville
Lauzier
Tracadie
Tracadie*
Mount Hope*
Bouleau
Boland
Fundy*
Sheila
Cambridge
Canobie
Tuadook
Tuadook*
Redstone
Lewis
Violette
Violette*
* Catenary association name.
31
PART 4. SOIL ASSOCIATION IDENTIFICATION KEY
AND GENERAL DESCRIPTION
KEY TO SOIL ASSOCIATION PARENT
M ATERIALS
A key to the soil association parent materials in the central and
northern New Brunswick map area is presented in Table 4.
The soils are systematically keyed out using chemical,
physical, morphological and genetic properties and
characteristics of the parent material. The sequence of
parameters utilized includes, in mineral soils: mode of
deposition, particle size class, consistence, reaction class,
colour, and coarse fragment lithology; and in organic soils:
botanical origin, degree of decomposition, reaction class,
colour and thickness. The key provides a means to identify an
association, or of differentiating one association from another.
It is also an orderly arrangement of the distinguishing features
of a group of soils that facilitates the classification and
determination of relationships. Soils are grouped into similar
classes according to diagnostic characteristics. For example,
Reece, Stony Brook, Tetagouche, and Violette are all mineral
soils developed on glacial till deposits of fine loamy, compact,
acidic material. These soil associations are differentiated from
each other on the basis of more detailed characteristics, ie. soil
colour and coarse fragment lithology. A more general
grouping of soils would be that of all mineral soils developed
in marine sediments. This includes; Richibucto, a sandy
noncompact acidic material; Belledune River, a coarse loamy
to sandy skeletal noncompact acidic material; and Tracadie, a
clayey compact neutral material. The Reece-Stony BrookTetagouche-Violette grouping can be considered a fourth level
grouping (composition, mode of deposition, particle
size-consistence, reaction), whereas the Richibucto-Belledune
River-Tracadie grouping is a second level grouping
(composition, mode of deposition).
vegetative cover, and related associations and how they are
differentiated. Profile and/or landscape photographs are
included for some of the dominant soil associations. Summary
tabular information is provided at the end of each soil
association description.
Acadie Siding Association
The Acadie Siding Association is made up of soils which are
composed of organic materials. They consist of relatively thin
peatland deposits, averaging 0.4 to 1.6 m in thickness, with
weakly to well-decomposed sphagnum and sedge plant
remains. Acadie Siding soils have developed as a result of the
"gradual build-up" process (Tarnocai, 1981). This process
involves the invasion of poorly drained areas by hydrophytic
vegetation, particularly mosses and sedges. As plant debris
accumulates above the level of the surrounding nutrient rich
ground water, the deposition becomes more and more acidic
and "nutrient poor", or ombrotrophic. Essentially, they are flat,
basin or bowl bogs (Tarnocai 1981) that have developed on
horizontal or channel fens. Acadie Siding soils occur mostly
in the Maritime Plain portion of the survey area (Fig. 7) on
level to undulating landscapes with slopes of less than 5%.
Some scattered deposits are also found in the New Brunswick
Highlands. Although they only account for 45,435 ha,
representing less than 1.63% of the survey area, Acadie Siding
soils commonly occur as unmapped inclusions in other organic
soils map units, or with very poorly drained mineral soils.
SOIL ASSOCIATION GENERAL DESCRIPTION
A general description of each soil association is provided in the
following text. These descriptions include information on soil,
landscape and related attributes. A map of the survey area
shows the location of polygons where the soil association has
been mapped. The soil profile is discussed in terms of horizon
sequence and classification in the Canadian System of Soil
Classification (Canada Soil Survey Committee 1978),
texture, consistence, structure, colour, coarse fragment content
(G, gravels; C, cobbles; S, stones), reaction, moisture holding
capacity, available rooting zone, internal drainage, mottling,
gleying and inherent fertility. General landscape conditions
are discussed. These include; slope, surface expression,
elevation, material thickness, depth to bedrock, mode of
deposition, stoniness, boulderiness and drainage (catena
members, site drainage, runoff). Information is also provided
on location (ie. physiographic region, etc.) and extent,
Figure 7. Location of mapped Acadie Siding soils.
Acadie Siding peatlands usually have level or flat surfaces that
are not raised above the surrounding terrain. Although peat
depths are relatively uniform, they decrease in depth from the
32
Table 4. Key to soil association parent materials in the central and northern New Brunswick map area
I.
Mineral soils.
A. Soils developed on glacial till.
1. Sandy, non-compact.
a. Acidic.
I. Yellowish brown to brown; coarse fragments - granites, granodiorites, diorites, granite gneiss and miscellaneous
volcanics; frequently skeletal. ........Juniper
ii. Yellowish brown to brown; coarse fragments - soft grey-green sandstone; frequently skeletal. ........Sunbury
2. Coarse loamy, non-compact.
a. Acidic.
I. Olive to olive brown; coarse fragments - slate, argillite, schist, greywacke and quartzite; frequently skeletal...........McGee
ii Yellowish brown; coarse fragments - rhyolite, trachyte, basalt and miscellaneous slates and greywacke..........Jacket River
iii Yellowish brown to brown; coarse fragments - granites, granodiorites, diorites, granite gneiss and miscellaneous
volcanics; frequently skeletal. ........Juniper
iv. Yellowish brown to brown; coarse fragments - soft grey-green sandstone; frequently skeletal. ...........Sunbury
v. Dark reddish brown; coarse fragments - sandstone and conglomerate. ............Parleeville
b. Neutral.
I. Light olive brown; coarse fragments - weakly calcareous shales, slates, quartzites, argillites and sandstones. .........Thibault
3. Coarse loamy, compact.
a. Acidic.
I. Olive brown; coarse fragments - slate, siltstone, argillite, schists and miscellaneous quartzite and greywacke; frequently
skeletal. ........Long Lake
ii. Yellowish brown to olive brown; coarse fragments - quartzite, sandstone and miscellaneous argillite, slate and
schists. ........Holmesville
iii. Yellowish brown to olive brown; coarse fragments - granites, schists and quartzites. .......... Catamaran
iv. Yellowish brown to olive brown; coarse fragments - rhyolite, trachyte, basalt and miscellaneous slates and greywacke;
frequently skeletal. ..........Popple Depot
v. Yellowish brown; coarse fragments - metagabbro and meta basalt with some granites, conglomerate and metagreywacke..
.........Nigadoo River
vi. Yellowish brown to brown; coarse fragments - granites, granodiorites, diorites, granite gneiss and miscellaneous volcanics;
occasionally skeletal. ......Tuadook
4. Loamy, non-compact
a. Acidic.
I. Strong brown; coarse fragments - metagabbro and meta basalt with some granites, conglomerate and metagreywacke..
...........Tetagouche Falls
5. Fine loamy, non-compact
a. Acidic.
I. Olive to olive brown; coarse fragments - argillites, slates and fine grained sandstones. ...........Boston Brook
b. Neutral.
I. Olive to olive brown; coarse fragments - calcareous shale, argillite and slate and some limestone. ..........Caribou
6. Fine loamy, compact
a. Acidic.
I. Light olive brown; coarse fragments - quartzite, sandstone and miscellaneous shale, argillite and slate. ........ Viloette
ii. Yellowish brown to brown; coarse fragments - soft gray-green sandstone and miscellaneous remnants of shale. ........Reece
iii. Brown; coarse fragments - sandstones, granites, gneiss, schists, and some volcanics and miscellaneous remnants of
highly weathered shale ..........Rogersville
iv. Strong brown; coarse fragments - metagabbro and meta basalt with some granites, conglomerate and metagreywacke..
...........Tetagouche
v. Red to reddish brown; coarse fragments - soft gray-green sandstone and miscellaneous remnants of shale. ...
........Stony Brook
b. Neutral.
I. Olive to yellowish brown; coarse fragments - calcareous shale, argillite and slate and some calcite. .......... Carleton
B. Soils developed in residual materials.
1. Sandy skeletal, non-compact
a. Acidic.
I. Yellowish brown; coarse fragments - granite. ............................Big Bald Mountain
33
Table 4. Key to soil association parent materials in the central and northern New Brunswick map area cont’d
C. Soils developed in fluvial sediments.
1. Sandy skeletal, non-compact.
a. Acidic.
I. Olive to olive brown; coarse fragments - noncalcareous slate, shale, quartzite and sandstone. .........Grand Falls
ii. Olive to yellowish brown; coarse fragments - soft gray-green sandstone...........Guimond River
iii. Yellowish brown to brown; coarse fragments - mixed igneous, metamorphic and miscellaneous sedimentary.
.........Gagetown
b. Neutral.
I. Olive to olive brown; coarse fragments - calcareous slate, shale, quartzite and sandstone. ..........Muniac
2. Sandy, non-compact.
a. Acidic.
I. Yellowish brown to olive brown; coarse fragments - mixed. .......................Riverbank
3. Sandy to coarse loamy, non-compact.
a. Acidic.
I. Olive to yellowish brown; coarse fragments - slate, shale and miscellaneous quartzite and volcanics. .........Maliseet
4. Coarse loamy, non-compact.
a. Acidic to neutral.
I. Olive to yellowish brown; coarse fragments - none; floods. .......................Interval
D. Soils developed in marine sediments.
1. Sandy, non-compact.
a. Acidic.
I. Yellowish brown to brown; coarse fragments - soft gray-green sandstone. ........Richibucto
2. Coarse loamy to sandy skeletal, non-compact.
a. Acidic.
I. Reddish brown to yellowish brown; coarse fragments -conglomerate, sandstone, siltstone, argillite and some
limestone. .........Belldune River
3. Clayey, compact.
a. Neutral.
I. Red to yellowish brown; coarse fragments - very few, mixed. ..........Tracadie
E. Soils developed in marine or fluvial sediments over glacial till deposits.
1. Sandy, noncompact over loamy, compact.
a. Acidic over acidic.
I. Yellowish brown to brown; coarse fragments - very few, undifferentiated over yellowish brown to dark reddish brown;
coarse fragments - undifferentiated............Barrieau-Buctouche
II. Organic soils.
A. Soils developed in sphagnum peat.
1. Dominantly fibric.
a. Acidic.
I. Brown to dark reddish brown; usually greater than 160 cm thick. ...........Lavillette
B. Soils developed in sedge-sphagnum peat.
1. Dominantly mesic and humic.
a. Acidic.
I. Brown to dark brown; usually less than 160 cm thick. ..........Acadie Siding
C. Soils developed in forest-fen peat.
1. Dominantly mesic and humic.
a. Neutral.
I. Dark brown; usually less than 160 cm thick. ...........St. Quentin
34
centre of the deposit outwards. Inclusion of areas with
thicknesses of more than 1.6 m may occur. Pronounced
surface patterns are usually lacking with the exception of the
presence of intermittent to semi-permanent drainage courses.
Most deposits are topographically confined in depression-like
areas.
Vegetative cover is dominated by sphagnum mosses and
ericaceous shrubs, with varying amounts of sedges and reeds.
Most deposits are treeless or treed with stunted dwarf black
spruce and tamarack in the centre, but with increasing cover at
the margins. Those sites that are more strongly minerotrophic
(nutrient-rich) have increased concentrations of sedges,
grasses, reeds, and even herbs. They also have denser tree
cover.
Peat stratigraphy usually consists of a surface layer 20 to 100
cm thick of fibric (weakly decomposed) sphagnum peats with
some shrubby materials, over a layer of mesic (moderately
d e c o m p o s e d ) a n d / o r h u m ic (w e ll -d e co m p o s e d )
sedge-sphagnum to sedge peat. This material extends to the
terric (mineral) contact. The underlying mineral material is
variable, usually being whatever is the predominate material in
the surrounding area.
The surface peat is brown to dark reddish brown, acidic (pH
in H 2O of less than 4.5), low in bulk density (less than 0.1
g/cm 3), moderately rapid to rapidly permeable (saturated
hydraulic conductivity of 10 to 15 cm/hr), and highly fibrous
with a class 1 to class 4 rating on the von Post scale of decomposition. Properties of the subsurface peat differ, mostly as a
result of its more advanced state of decomposition and
different botanical origin. The subsurface peat is brown to
dark brown, acidic (pH in H2O of less than 4.5), moderate to
high in bulk density (approximately 0.15 g/cm 3), moderately
to very slowly permeable (saturated hydraulic conductivity of
1.0 to less than 0.1 cm/hr), and moderate to low in rubbed fibre
content with a class 5 to class 8 rating on the von Post scale of
decomposition.
Drainage is very poor. Water table levels are at or near the
surface throughout the year resulting in ponding. Ground
water is acidic to neutral and of low to moderate nutrient
status.
Acadie Siding soils are dominantly Terric Mesisols, Terric
Fibric Mesisols or Terric Humic Mesisols, but with significant
Terric Humisol and Terric Fibrisol components. Total
thickness of the organic material ranges from 40 to 160 cm
over the mineral soil (terric) contact. Variation in classification depends upon the relative thicknesses of the fibric
and humic layers in the profile. The fibric influence is largely
determined by the thickness of the surficial layer of weakly
decomposed (fibric) sphagnum material. Where fibric
materials dominate the control section, the profile is classified
as some form of Fibrisol, depending upon the significance and
degree of decomposition of other layers present. The degree
of decomposition of the underlying sedge-sphagnum material,
which varies from mesic to humic, also plays a major role in
the classification of Acadie Siding soils. Where the control
section of the profile is dominated by well-decomposed
sedge-sphagnum peats, the soil is classified as a Humisol.
Inclusions of areas of deeper deposition (i.e., nonterric) usually
consist of thicker layers of both fibric and mesic-humic peats,
which are classified as Typic Mesic Fibrisols or Typic Fibric
Mesisols.
Acadie Siding soils are associated with other organic soils, as
well as with poorly and very poorly drained members of some
mineral soils. Lavillette is a common organic soil associate.
Lavillette soils differ from Acadie Siding soils in that they
consist of deep, non-terric, weakly decom posed, fibric
materials found on well-developed, domed or raised bogs.
Lavillette soils usually have a distinctive circular surface
pattern not present on Acadie Siding soils. Very poorly or
poorly drained Barrieau-Buctouche, Richibucto, Reece, Stony
Brook and Sunbury mineral soils are also close associates.
Acadie Siding soils have been mapped less frequently with
Catamaran, Juniper, Long Lake and Tuadook mineral soils.
Acadie Siding soils are differentiated from mineral soils based
on the depth of organic material present. To be classed as
Acadie Siding, a soil must have at least 40 cm of dominantly
mesic or humic organic material or 60 cm of dominantly fibric
organic material, otherwise it is included with the appropriate
mineral soil association.
Acadie Siding soils are considered to have no immediate
potential for forest or agricultural crops. Costs associated with
development and management are considered to be excessive.
Summary of general characteristics of the Acadie Siding Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Degree of Decomposition
Botanical Composition
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: AS
: Maritime Plain, N. B. Highlands
: < 150 m
: 45,435 ha
: 1.63%
: Organic
: Basin or bowl bogs
: 0.4-1.6 m over mineral soil
: Brown to dark brown
: Moderately to very strongly decomposed
: Sphagnum and sedge peat
: Very low
: Flat (<1%) in an undulating landscape
(<5%)
: Very poor
: Terric Mesisol
Layer
Friable upper
soil material
Subsoil
material #1
Subsoil
material #2
Depth (cm)
0 - 60
60 - 120
> 120
Von Post rating
1-4
5-8
-
% Wood
10
10
-
35
Texture Class
-
-
Sandy clay
loam
% Sand
-
-
60
% Silt
-
-
16
% Clay
-
-
24
% Coarse
Fragments
-
-
20 angular
G/C
pH (H2 O)
< 4.5
< 4.5
4.5
BD (g/cm3 )
< 0.10
0.15
1.90
Ksat (cm/hr)
10 - 15
1.0 - < 0.1
0.1
AWHC (cm/cm)
0.10
0.20
< 0.10
Barrieau-Buctouche Association
The Barrieau-Buctouche association is made up of soils that
have developed in deposits consisting of acidic, sandy, marine
or marine modified glacial outwash sediments overlying
acidic, compact, fine loamy, morainal till materials. It
occupies the transition zone between Richibucto soils and
Stony Brook-Reece soils. Mapping of these types of transition
zones between material types is usually impossible at a scale
of 1:250,000. In most instances they are ill-defined areas
along map unit boundaries. However, as a result of postglacial
marine submergence, significant areas of the lowland plain
(Fig. 8) have a thin veneer (less than 1 m thick) of marine
sediments overlying the glacial till. Barrieau-Buctouche soils
are found at elevations of less than 50 m above sea level. They
occupy approximately 40,054 ha, or about 1.44% of the map
area.
Figure 8. Location of mapped Barrieau-Buctouche soils.
The underlying glacial till is basal or lodgment till, plastered
into place in successive layers and compacted by the weight of
glacier ice. It is a heterogeneous mixture of particle sizes
ranging from silts and clays to stones and boulders.
Subsequent to this was the deposition of well sorted sandy
marine or marine reworked glaciofluvial sediments. These are
weakly stratified sands, primarily medium to fine grained, but
with some fine gravels. The combined thickness of both
materials is usually 1 to 3 m, with most soils being mapped as
blankets. Barrieau-Buctouche soils occupy level to gently
undulating landforms. Surface expression conforms to the
configuration of the underlying bedrock. Most slopes are
between 0.5 and 3%. Steeper gradients are site specific or
occur along stream and river valleys. Well to moderately well
drained sites support stands of black spruce and balsam fir with
some jack pine and grey birch on the drier sites. Black spruce,
balsam fir, cedar, red maple and some yellow birch are typical
of ill-drained conditions.
The Barrieau-Buctouche association consists of well to
moderately well drained Orthic Humo-Ferric Podzols (Fig. 9),
imperfectly drained Gleyed H umo-Ferric Podzols and Gleyed
Eluviated Dystric Brunisols, and poorly to very poorly drained
Orthic Gleysols and Fera Gleysols. Although the B horizon in
well to imperfectly drained profiles appears morphologically
to be a Bf horizon, chemical analysis reveals that it just barely
exceeds the minimum requirements for sodium pyrophosphate
extractable Fe plus Al. Poorly drained soils lack the podzolic
B horizon. They have evidence of gleying that satisfies the
specifications of the Gleysolic order. Where hydrous iron
oxide has accumulated forming a Bgf horizon they are Fera
Gleysols, otherwise poorly to very poorly drained
Barrieau-Buctouche soils are classified as Orthic Gleysols.
Internal drainage is impeded by the presence of the underlying
compact, very slowly permeable (less than 0.1 cm/hr) glacial
till subsoil. Textural voids in the coarse textured sandy marine
surface sediments are conducive to rapid flow rates of in
excess of 15 cm/hr. This hydraulic discontinuity between the
surface and subsoil promotes internal lateral flow, with
downslope seepage of water. Perched water tables often result,
with a saturated zone at and just immediately above the
interface. Available water storage capacity is moderately low
(less than 0.15 cm/cm) throughout the profile . With exception
of the upper solum where slightly finer texture and the
presence of organic matter enhance moisture retention, the
coarser nature of the marine sand is not conducive to water
storage. On the other hand the glacial till subsoil is low in
available water storage capacity because of its limited total
porosity. Well to moderately well drained Barrieau-Buctouche
soils occupy crest and upper slope positions where
precipitation is the sole source of water. Excess precipitation
is laterally removed from the site as subsurface flow. Given
similar topographic conditions, well drained sites usually occur
where marine sediments are thicker (50 to 100 cm), and
moderately well drained where thinner cappings are present
(less than 50 cm). Imperfectly and poorly to very poorly
drained sites are strongly influenced by inflow (seepage) from
surrounding uplands. Prolonged saturation is due to both
perched and true groundwater tables. The undulating
36
configuration of the underlying till is conducive to localized
perched water tables which are created by spring snowmelt and
rejuvenated during the summer months by precipitation and
seepage. The association is dominated by imperfect drainage.
interface of the two materials. The textural profile consists of
sandy loam to loamy sand marine sediments over loam to clay
loam or sandy clay loam glacial till material. The marine
sediments are usually relatively free of coarse fragments (less
than 5%). Those coarse fragments that do occur are rounded
gravels derived from soft, gray-green Pennsylvanian
sandstone. The till materials have from 15 to 20% flat to
subangular cobbles and gravels of similar sandstone lithology.
Some remnant shale and siltstone chips are also present, but for
the most part the original clasts have disintegrated and been
incorporated into the soil matrix. Surface stones are
insignificant. Barrieau-Buctouche soils are low in natural
fertility and acidic throughout, pH(H 2O) 4.0 to 5.5. The solum
is very friable, weak platy (Ae) or weak granular (B). Subsoil
marine sediments are usually loose and structureless or single
grain. The underlying till is firm to compact and pseudoplaty
to weak medium subangular blocky or massive.
Barrieau-Buctouche soils have developed in two tiered
deposits of marine sediments over glacial till. They are
therefore intimately associated with soils that have developed
on either of their component parts, i.e., Richibucto sandy
marine soils, or Stony Brook and Reece fine loamy till soils.
The Richibucto association lacks the underlying till
component. The Stony Brook and Reece associations lack the
surficial mantle of marine sediments. Tracadie marine clays
and Guimond River glaciofluvial gravels are other waterdeposited soils that have been mapped with BarrieauBuctouche. Very poorly drained Barrieau-Buctouche soils have
also been mapped with Lavillette organic soils and Salt Marsh
land types.
Figure 9. Well drained Barrieau-Buctouche soil profile.
Soil formation averages 35 to 45 cm in depth. Depending
upon thickness of the marine mantle, this development may be
confined to the marine sediments, or may affect both materials.
In well to moderately well drained profiles the common
horizon sequence is either : LFH, Ae, Bf, BC, C, and IIC ; or
LFH, Ae, Bf, IIBC, and IIC. The profile is typically podzolic
in appearance with a thin LFH layer over an ash coloured
eluvial A horizon that has an abrupt lower boundary to a
reddish brown to yellowish brown Bf. Where present the C
horizon is yellowish brown to brown. The underlying IIC
horizon is either yellowish brown to brown, or red to reddish
brown. Imperfectly drained sites are not always podzols and so
there may be either a Bfgj or Bmgj horizon. There is also
usually a thin leached horizon, Aegj, immediately above the
second material. This layer is the result of lateral leaching.
Poorly drained profiles consist of LFH or O , Aeg, Bg or Bgf
and II Cg horizons. The surface organic layer is usually
thicker and strong mottling and/or gleying occurs along the
In terms of land use and biological production, the outstanding
features of the Barrieau-Buctouche association are the presence
of the relatively coarse fragment free sandy marine veneer and
the dense, compact, relatively impermeable nature of the
underlying till which limits moisture movement and root
penetration. Barrieau-Buctouche soils are also low in natural
fertility. While natural or inherent fertility of the soil is to a
large degree a function of soil mineralogy, it also relates to soil
nutrient retention. Coarser-textured soils that are low in clay
content tend to be more easily leached of nutrients than finertextured soils. Forest production, which is dependent on
natural fertility, is limited by these low levels of nutrients.
Summary of general characteristics of the Barrieau-Buctouche Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
: BB
: Maritime Plain
: <50 m
: 40,054 ha
: 1.44%
: Mineral
: Marine or outwash over compact glacial
till
: 1-3 m
: Yellowish brown to brown over
yellowish brown to reddish brown
: Sandy over loamy
: Grey-green sandstone over grey-green
sandstone plus red shale
37
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: Low
: Level to undulating (0-3%)
: Imperfect
: Gleyed Humo-Ferric Podzol
Layer
Friable upper
soil material
Subsoil
material #1
Subsoil
material #2
Depth (cm)
0 - 40
40 - 65
65 - 100+
Texture Class
Loamy sand
Sand
Sandy clay
loam
% Sand
85
93
53
% Silt
8
4
25
% Clay
7
3
22
% Coarse
Fragments
0
5 rounded G
20 subangular
G/C
pH (H2 O)
4.5 - 5.0
5.0
5.0 - 5.5
BD (g/cm3 )
1.15
1.40
1.90
Ksat (cm/hr)
45
50
0.1
AWHC
(cm/cm)
< 0.15
0.10
< 0.10
Belledune River Association
The Belledune River association consists of soils developed in
moderately thick (greater than 2 m) deposits of strong to
medium acidic, coarse loamy to sandy skeletal, non-compact,
marine sediments with coarse fragments of conglomerate,
sandstone, siltstone and some argillite and limestone.
Belledune River soils occur only on the lowlands portion of the
New Brunswick Highlands adjacent to Chaleur Bay (Fig. 10).
They are situated at elevations of less than to 50 m above sea
level. Belledune River marine sediments are underlain by
either glacial till, or lie directly on the bedrock. Belledune
River soils occupy approximately 27,854 ha or 1.00% of the
map area.
Belledune River soil parent materials are marine depositions
dominated by sand and silt. They were deposited in a brackish,
shallow water environment during postglacial marine
submergence and subsequently exposed when water levels
receded. Most land surfaces are gently undulating, with slopes
of 2 to 5%. Belledune River material consists of weakly
stratified marine sediments with coarse fragments and soil
particles poorly sorted according to size or weight. Because of
this, they are frequently referred to as being “dirty” sand and
gravel deposits. Belledune River soils may have enough
scattered surface stones to be a slight hindrance to cultivation.
Forest vegetative cover consists of species such as black
spruce, cedar, tamarack, red maple, trembling aspen and alder.
Figure 10. Location of mapped Belledune River soils.
Well drained Belledune River association soils are Orthic
Humo-Ferric Podzols (Fig. 11). Podzolization is strongly
expressed, even in sites that are less than well drained.
Imperfectly drained sites are Gleyed Humo-Ferric Podzols.
Poorly drained sites are Orthic Gleysols or Fera Gleysols.
Internal drainage is good . The profile consists of a moderately
rapidly permeable solum over a moderately permeable subsoil.
Saturated hydraulic conductivity values are greater than 2.5
cm/hr throughout the profile and greater than 5 cm/hr in the
solum. Available water storage capacity ranges from 0.20 to
0.10 cm/cm, the higher values being in the solum where finer
textures and organic matter contents enhance moisture
retention. Precipitation is the sole source of water supply on
well drained sites. Excess water flows downward into the
underlying subsoil. Imperfectly and poorly drained sites are
the results of high groundwater tables.
Solum development in Belledune River soils varies from 35 to
55 cm in thickness. The common horizon sequence is: LFH,
Ae, Bf, BC and C on well to moderately well drained sites;
LFH, Ae, Bfgj, BCgj or BCg and Cg on imperfectly drained
sites; and LFH or O, Aeg, Bg or Bgf and Cg on poorly or very
poorly drained sites. Although Belledune River soils have
formed in marine sediments, soil forming processes have
obliterated any evidence of material stratification in the solum.
Soil textures grade from a sandy loam to loam or silt loam
solum into a sandy loam to loamy sand subsoil. Coarse
fragment content ranges from 15 to 50%. Coarse fragments
are mostly subrounded to rounded gravels with some cobbles.
They are derived from conglomerate, sandstone, siltstone and
some argillite and limestone. These rock types result in a soil
that is moderately fertile. The profile is acidic throughout,
ranging from a pH(H 2O) of 5.0 to 6.0 . The parent material is
reddish to dark brown. The mineral soil profile consists of a
38
pinkish gray, friable, weak, fine platy Ae horizon over a strong
brown, very friable, weak to moderate, fine granular Bf
horizon which merges gradually into the friable, very weak,
subangular blocky BC and then C. Mottles and grayish gley
colours modify the profile morphology in imperfectly and
poorly drained sites. Only under the very wettest of conditions
is the general podzolic sequence not present.
Summary of general characteristics of the Belledune River Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: BR
: Chaleur Uplands
: <50 m
: 27,854 ha
: 1.00%
: Mineral
: Marine
:>2m
: Reddish brown to yellowish brown
: Coarse loamy to sandy
: Conglomerate, sandstone siltstone,
argillite and some limestone
: Medium
: Undulating (2-5%)
: Imperfect
: Gleyed Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Sandy loam, loam,
silt loam
Sandy loam to loamy
sand
% Sand
55
60
% Silt
28
30
% Clay
17
10
% Coarse
Fragments
20 rounded G
50 rounded G/C
pH (H2 O)
5.0
5.5
BD (g/cm3 )
1.30
1.55
Ksat (cm/hr)
10
2.5
AWHC (cm/cm)
0.20
0.10
Figure 11. Well drained Belledune River soil profile.
Big Bald Mountain Association
Belledune River association soils are often associated with
other water deposited materials - Tracadie and Gagetown.
Tracadie soils have developed in coarse fragment-free clayey
marine sediments and are readily differentiated from Belledune
River soils. Gagetown soils have developed in yellowish
brown glaciofluvial gravels.
The Big Bald M ountain association consists of soils that have
developed in thin veneers of acidic, sandy skeletal residual
material that has weathered in place from the consolidated
granite bedrock on which it lies. Big Bald Mountain soils were
first mapped in the vicinity of Big Bald Mountain in the
Central Highlands physiographic region (Fig. 12). They are
also found in other areas of the Central Highlands where
granitic bedrock occurs. Big Bald Mountain soils are mapped
at elevations of 400 to 600 m above sea level, and cover
approximately 15,394 ha, or about 0.55% of the map area.
Good internal drainage, adequate water and nutrient holding
capacities in the surface soil and medium natural fertility make
Belledune River soils productive for both agricultural and
forestry crops. The major limitation to land use is the
predominance of imperfectly and poorly drained conditions.
However, with moderate permeability in the subsoil, Belledune
River soils should be very responsive to tile drainage. Natural
drainage conditions will be more of a limitation to forestry
crops.
Big Bald Mountain soils are considered to have develop in situ
from the underlying feldspar rich granitic bedrock. Physical
and chemical transformations have taken place in the surface
of the parent bedrock which has disintegrated and decomposed
into rock fragments and soil debris. This type of accumulation
39
glaciers. The landforms have a strongly rolling to hilly surface
expression dominated by moderate to very strong slopes of 9
to 45%. Vegetation consists mainly of stunted, scattered
jackpine and spruce. Wild blueberry, interspersed with other
ericaceous shrubs, is the dominant ground cover.
The Big Bald M ountain association is dominated by well to
rapidly drained Orthic Humo-Ferric Podzols (Fig. 14). The
profile consists of a bleached ashy Ae horizon followed by a
dark to strong brown B horizon in which both colour value and
chroma decrease with increase in depth. The C horizon is dark
yellowish brown. Imperfectly to somewhat poorly drained sites
occur as inclusions. They consist of Gleyed Humo-Ferric
Podzols.
Figure 12. Location of mapped Big Bald Mountain soils.
of angular coarse-grained fragments resulting from the
granular disintegration of granite (and other crystalline rocks)
is referred to as "grus". The granite bedrock of the Big Bald
Mountain association is estimated to consist of 40% potassium
feldspar, 25% plagioclase, 30% quartz and 5% biotite, chloride
and hornblende. Weathered bedrock or grus is usually less than
1 m thick, except for the soils at the foot of slopes which are
deeper. Tors, peculiarly shaped isolated rock masses or
pinnacles, are present on some summits (Fig. 13). They are
deeply weathered, with rings 1 to 2 m wide, of colluvial grus
accumulating around their bases.
Figure 13. Big Bald Mountain soil association landscape
showing “tors”.
Gibbsite, considered to be the end product of the weathering
sequence of soil minerals, has been found in Big Bald
Mountain soil parent material. The presence of tors and
gibbsite coupled with a general lack of evidence of glacial
activity prompted Wang et. al. (1981) to conclude that these
soils and landforms are of pre-Wisconsin or even
pre-Pleistocene age. It is hypotheorized that the area was
frozen, protected by ice, and consequently undisturbed by the
Figure 14. Well drained Big Bald Mountain soil profile.
Precipitation is the sole source of water on well to rapidly
drained sites. The soils have a high infiltration capacity and
excess water flows downward rapidly through the porous
profile at an estimated rate of 10 cm/hr or greater. The
bedrock, which becomes m ore consolidated with depth,
impedes downward flow to some degree, causing horizontal
water flow under conditions of extrem e rainfall or rapid
snowmelt. Available water storage capacity is estimated to be
less than 0.15 cm/cm in the solum and less than 0.10 cm/cm in
the C horizon. Increased capacity to retain moisture in the
solum is attributed to its higher clay and organic matter
contents and lower coarse fragment content than the patent
material. Moisture deficits on Big Bald Mountain soils
influence forest fire patterns, encouraging repeated burnings,
thus determining the vegetative cover type. Imperfectly to
somewhat poorly drained sites occupy depressions and
drainage channels in lower site positions. They are supplied
with water by groundwater flow and seepage (along the
soil-bedrock interface) from adjacent uplands.
Soil development averages 30 to 45 cm in depth. The common
horizon sequence consists of: Om, Ae, Bf, BC, C, and R. A
weakly developed ortstein layer may occur in the Bf horizon.
Ortstein is an irreversible hardpan that is bonded by Fe, Al and
organic matter complexes. It is discontinuous, occurring in
less than 20% of the soil associations horizontal extent. Profile
40
texture is sandy loam to loamy sand. Clay content seldom
exceeds 10%. Coarse fragment content increases with depth
from 10 to 20% in the solum to in excess of 60% in the parent
material C horizon). Most coarse fragments are angular fine
gravels but the occasional cobble or stone sized fragment of
consolidated bedrock is also found in the profile. The land
surface is slightly to moderately stony where differential frost
heaving has brought bedrock fragments to the soil surface. All
coarse fragments have been derived from the underlying
granitic bedrock. Bedrock exposures and areas of very thin
soil (less than 10 cm thick) cover up to 25% of the land surface
of some map polygons. They are scattered patches on crest
and upper slope positions. Big Bald Mountain soils are very
low in natural fertility and acidic, pH (H2O) of 4.5 to 5.5,
throughout. The soil is very friable to friable, very weak, fine
to coarse, subangular blocky in the solum, and firm, pseudo
platy in the C horizon. Much of the original bedrock structure
is retained in the profile, becoming more pronounced with
depth. Where patches of ortstein occur the Bf horizon is firm
and massive.
Juniper is the soil most commonly mapped in association with
Big Bald Mountain. Juniper is coarse loamy to sandy and is
derived from primarily granitic sources. Its till mode of
deposition, however, makes it easy to separate the two soils.
Juniper soils are a heterogeneous mixture of glacial debris
ranging from silts and clays to boulders. Lithologically they
are also more diverse with diorites, granodiorites, granite
gneiss, volcanics and miscellaneous sedimentary and
metamorphic coarse fragments in addition to the feldspar rich
granites. Big Bald M ountain is also found adjacent to units of
Long Lake and McGee soils, both of which are glacial till
soils. The Long Lake and McGee associations have distinctly
different lithological origins, having been derived from
argillaceous sedimentary and metamorphic rock types such as
shale, argillite, slate, greywacke and quartzite.
Big Bald Mountain soils are shallow to bedrock and very low
in natural fertility and available moisture storage capacity.
These limitations coupled with adverse topographic conditions,
ie. excess slope, and a harsh climate, make Big Bald Mountain
soils unsuitable for agriculture. These factors also limit the
soils potential for forestry.
Summary of general characteristics of the Big Bald Mountain Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: BM
: N. B. Highlands
: 400-600 m
: 15,394 ha
: 0.55%
: Mineral
: Residual
:<1m
: Yellowish brown
: Sandy skeletal
: Granite
: Very low
: Strongly rolling to hilly (9-45%)
: Well
: Orthic Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Bedrock
Depth (cm)
0 - 35
35 - 70
> 70
Texture
Class
Sandy loam
Loamy sand
-
% Sand
70
85
-
% Silt
23
7
-
% Clay
7
8
-
% Coarse
Fragments
15 angular G
50 angular G/C
-
pH (H2 O)
4.5
5.0
-
BD (g/cm3 )
1.10
1.45
-
Ksat (cm/hr)
> 10
10
-
AWHC
(cm/cm)
< 0.15
< 0.10
-
Boston Brook Association
The Boston Brook association consists of soils that have
developed in acidic, fine loamy, noncompact morainal till
derived from argillites, slates and fine-grained sandstones.
Deposits range from less than 1 m thick (veneers) to in excess
of 3 m. Boston Brook soils occur in the Chaleur Uplands
portion of the study area (Fig. 15) at elevations between 300
and 500 m above sea level. They occupy approximately 2,877
ha, representing some 0.10% of the map area.
Boston Brook soil parent material is an ablational till, and as
such is typically noncompact, however, some firmness may
occur in the subsoil. The somewhat firm consistence of the
subsoil can be attributed to the composition of the parent
material in that it is fine loamy and acidic. The acidic nature
of the subsoil does not promote soil forming physical and
biochemical processes that favour the development and
stabilization of soil structure.
Boston Brook soils consist of fine loamy sediments with
subangular and flat to subrounded coarse fragments derived
from the underlying slate, argillite, sandstone or quartzite
bedrock. Surface stoniness ranges from moderate to very
stony, with up to 15% of the land surface occupied by coarse
fragments in some cases. Well drained Boston Brook soils
have developed under a mixed hardwood-softwood forest
cover type consisting of yellow birch, cedar, spruce, balsam
fir, sugar maple, beech, white birch, white pine, red oak and
striped maple. Poorly to very poorly drained members are
dominated by cedar, black spruce, balsam fir, white birch, red
maple, speckled alder and willows.
41
Figure 15. Location of mapped Boston Brook soils.
The Boston Brook association is dominated by well to
moderately well drained Orthic Humo-Ferric Podzols.
Imperfectly drained sites are classified as Gleyed Humo-Ferric
Podzols, indicating varying oxidizing/reducing conditions due
to periodic saturation. Poorly to very poorly drained sites are
typically Orthic Gleysols but may have some inclusions of
Fera Gleysols. Imperfect and poorly to very poorly drained
sites occur along drainage channels and in depressions in areas
dominated by moderately well drained soils, or more
extensively in areas that are level or only gently undulating.
Boston Brook soils have moderate to somewhat slow internal
drainage. The upper solum usually has moderate permeability
(approximately 5 cm/hr saturated hydraulic conductivity), but
the subsoil only has moderately slow permeability (0.5 to 2.0
cm/hr). Available moisture storage capacity exceeds 0.20
cm/cm throughout the profile with highest levels in the upper
solum. Decreased pore size in the lower solum reduces the
availability of retained moisture. In well to moderately well
drained sites precipitation is the dominant source of water.
Lateral flow or seepage is not a problem, occurring only on
very steeply sloping landscapes where bedrock restricts
vertical flow, or when water inputs due to either precipitation
or snowmelt exceed the subsoil permeability. Poorly to very
poorly drained sites occur because of high groundwater levels
and to a lesser extent because of the inflow of seepage from
adjacent uplands, or both. The underlying bedrock is acidic
and so seepage waters are not exceptionally rich in nutrients,
although still somewhat beneficial to plant growth.
Soil development is relatively thin, with solums ranging from
35 to 55 cm. The common horizon sequence on well drained
sites is LFH, Ae, Bhf, Bf, BC and C. O horizons may occur
under coniferous forests where mosses dominate the ground
vegetation. The organic layer is 3 to 10 cm thick, becoming
more humified with depth. It overlies a thin (2 to 5 cm), light
brownish gray coloured Ae horizon which breaks abruptly into
the B horizon. A thin brown to dark brown Bhf horizon varies
from 3 to 8 cm in thickness. The Bhf horizon merges with a
yellowish brown Bf horizon which gradually grades into the
oxidized light olive brown parent material. At 30 to 40 cm the
podzolic B horizon grades into a BC horizon which grades into
the unaltered parent material or C horizon. Imperfectly
drained soils have similar profile horizons but are modified by
periodic saturation. They are mottled in the B and C horizons.
Poorly to very poorly drained horizon sequences typically
consist of LFH or O, Aeg, Bg, BCg, and Cg horizons. The
forest duff layer is thicker in poorly and very poorly drained
conditions than found in well drained counterparts, varying
from 5 to 15 cm, but occasionally as thick as 30 cm. The
Boston Brook textural profile consists of a loam to clay loam,
usually increasing in clay content with depth and also as
drainage becomes poorer. Profile coarse fragment content
varies from 10 to 30%, with a preponderance of subangular to
somewhat subrounded gravels and cobbles. Boston Brook
soils are medium in inherent fertility and acidic throughout,
with pH(H 2O) values of 4.0 to 5.5. A friable to very friable,
weak to moderate, fine to medium, granular or subangular
blocky solum overlies a slightly firm weak, medium
subangular blocky subsoil.
Boston Brook soils are associated with soils of the Caribou,
Holmesville and Violette associations., and occasionally with
the Tetagouche and Tetagouche Falls associations
The
Caribou association is differentiated from Boston Brook on the
basis of subsoil reaction. Boston Brook parent materials are
acidic while Caribou parent materials are near neutral. Coarse
fragment lithologies also differ between the two soils,
however, in many other features they are similar owing to their
both having developed on fine loamy noncompact till
materials. Boston Brook is differentiated from Holmesville
and Violette on the basis of subsoil compaction. Boston Brook
soils are only somewhat compact in the subsoil while both
Holmesville and Violette soils are strongly compacted,
especially Violette soils. Holmesville soils have coarser
textured subsoils than Boston Brook soils. Violette soils have
similar fine loamy subsoils, and near identical lithologies,
making their separation from Boston Brook soils one of
subsoil compaction.
The Boston Brook association is considered marginally
suitable for agriculture in its existing state. The major
limitation to agricultural development is coarse fragment
content.
Stones and cobbles may impede agricultural
production, but when overcome, Boston Brook soils should be
moderately suitable for most crops. They have good nutrient
and water holding capacities and the subsoil is not typically a
structural limitation. From a forestry perspective these soils
are capable of supporting a wide range of commercial species
since they are moderate in natural fertility.
Summary of general characteristics of the Boston Brook Association
Map Symbol
Physiographic Region(s)
: BO
: Chaleur Uplands
42
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: 300-500 m
: 2,877 ha
: 0.10%
: Mineral
: Glacial till, noncompact
:<3m
: Olive to olive brown
: Fine loamy
: Argillite, slate and fine-grained sandstone
: Medium
: Undulating to hilly or ridged (2-70%)
: Well to moderately well
: Orthic Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Loam
Clay loam
% Sand
35
30
% Silt
40
39
% Clay
25
31
% Coarse
Fragments
15 subangular G/C
25 subangualar G/C
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.30
1.60
Ksat (cm/hr)
5
0.5 - 2
AWHC (cm/cm)
>.20
0.20
9%, but slopes of 15 to 45% may occur along stream channels
that are deeply incised into the bedrock. Landform surface
expressions are more characteristic and indicative of a basal till
mode of deposition. This is further corroborated by the
localized nature of the till debris. Most of the soil parent
material has been derived from the bedrock upon which it is
presently resting, with only minimal displacement. Similarity
to the underlying bedrock often makes it difficult to determine
if the subsoil is till or residual (weathered in situ) material.
The friable to only somew hat firm consistence of the subsoil
may be attributed to the composition of the parent material.
The presence of available bases (ie. calcium from the calcitic
bedrock debris) promotes physical and biochemical processes
in soil formation that favour the development and stabilization
of soil structure.
Figure 16. Location of mapped Caribou soils.
Caribou Association
The Caribou association consists of soils that have developed
in neutral to weakly calcareous, fine loamy, noncompact
morainal till derived from calcareous shale, argillite and slate,
and occasionally some limestone. Deposits range from less
than 1 m thick (veneers) to some deposits in excess of 3 m
thick. The transition from regolith to bedrock may be gradual,
with some in situ weathering of the underlying vertically
dipping calcitic shale (slate) bedrock. Caribou soils occur in
the Chaleur Uplands portion of the study area (Fig. 16) at
elevations between 300 and 500 m above sea level. They
occupy approximately 82,212 ha, representing some 2.95%
of the map area.
Caribou soil parent material is noncompact, and as such has
been considered to be ablational till. However, it is quite
conceivable that much of the material was in fact deposited as
basal till, laid down below the glacier as it advanced. This
hypothesis is substantiated by several conditions. Most
Caribou soils occur on the gently rolling to undulating plateau
between St. Quentin and the Restigouche River. They
commonly occupy ridges with broad tops and slopes of 3 to
Regardless of mode of deposition, the physical and chemical
attributes of Caribou soils are quite uniform. They consist of
noncompact, fine loamy sediments with sharp, angular, flat
coarse fragments derived from the underlying weakly
calcareous shale-slate. Surface stoniness ranges from slightly
to moderately stony, with less than 3% of the land surface
occupied by coarse fragments. Well drained Caribou soils have
developed under a mixed hardwood-softwood forest cover type
consisting of red and sugar maple, beech, white birch,
mountain ash, red oak, trembling aspen, white pine, balsam fir
and black and white spruce. Poorly to very poorly drained
members are dominated by black spruce, balsam fir, white
cedar, tamarack, red maple, trembling aspen, black ash, and
speckled alder.
The Caribou association is dominated by well to moderately
well drained Podzolic Gray Luvisols and Luvisolic
Humo-Ferric Podzols. This represents bisequal soil
horizonation ie. two sequences of an eluvial horizon and its
related illuvial horizon. The upper sequence of horizons is
typical of a podzol with development of a Bf horizon. The
lower sequence of horizons is typical of a luvisol, with a
distinct increase in clay content forming a Bt horizon. Depth
43
to the Bt horizon determines whether the soil is classified as
Luvisolic or Podzolic. During soil formation acid leaching
removed free carbonates from the upper solum. Wetting and
drying cycles then lead to the dispersal of the very fine clay
component which was translocated with the downward
movement of water. Carbonates in the lower profile caused the
clays to flocculate, thus accumulating into a Bt horizon. Thin
to moderately thick clay films are present in voids and root
channels and on most vertical and horizontal ped faces.
Imperfectly drained sites are classified as either Gleyed
Podzolic Gray Luvisols or Gleyed Brunisolic Gray Luvisols,
indicating weaker soil development than is found in the well to
moderately well drained sites. Poorly to very poorly drained
sites are Orthic Luvic Gleysols and Orthic Humic Gleysols.
They usually occur along drainage channels and in depressions
as predictable inclusions in areas dom inated by well to
moderately well drained soils. Caribou soils have moderate
internal drainage. Based on pore size distribution, the upper
solum is estimated to have a moderate to moderately rapid
permeability (2.5 to 10 cm/hr saturated hydraulic conductivity)
and the lower solum (Bt horizon) and subsoil moderately slow
permeability (0.5 to 2.0 cm/hr). Available moisture storage
capacity exceeds 0.20 cm/cm throughout the profile. In well
to moderately well drained sites precipitation is the dominant
source of water. Rainfall exceeds evaporation resulting in
excess water which flows downward through the profile.
Lateral flow occurs only on very steep gradients during periods
of extreme wetness (spring snowmelt, heavy rainfall, etc.).
Poorly to very poorly drained sites occur because of high
groundwater levels and to a lesser extent because of inflow of
seepage from adjacent uplands, or both. The underlying
bedrock is a vertically standing weathered shale-slate (Fig.17)
that accommodates some downward movement of water.
Soil development is quite thick, with solums ranging from 60
to in excess of 100 cm. This greater than normal thickness of
solum development can be attributed to the illuviation of clay.
Profile development is greatest in the well to moderately well
drained sites. The common horizon sequence is LFH, Ah, Ae1,
Bf, Ae2, Bt and C. The Ae1 horizon is usually thin and often
discontinuous. Faunal activity has created a moder-mull type
of forest humus form that may reach depths of 5 to 10 cm, at
the expense of the LFH and Ae horizons. However, conditions
also exist in which the Ah horizon may be almost completely
absent. The organic rich Ah is dark brown to black while the
Ae horizon is white to light grey. The Bf horizon is
characteristically strong brown to brownish yellow, becoming
paler with depth. Parent material colours range from olive to
olive brown. Imperfectly drained Caribou soils have similar
horizonation to their well drained counterparts. The major
difference morphologically is the presence of mottles and gley
features due to periodic reducing conditions. Chemically, Fe
and Al accumulation in the upper B horizon is less than in the
well drained member. The upper B horizon in imperfectly
drained soils ranges from a Bf to a Bm (or Bfj). In poorly to
very poorly drained profiles the common horizon sequence is
either LFH or O, Aeg, Btg and Cg where there is a significant
amount of clay translocation; or, LFH or O, Ah, Bg and Cg
Figure 17. Well drained Caribou soil profile, veneer phase.
where the dominant features are the thick Ah and lack of clay
migration; or some combination of the two sequences. The
Caribou textural profile consists of a silt loam to loam upper
solum that grades into a clay loam to silty clay loam in the Bt
and C horizons. The clay content peaks in the Bt horizon.
Clay mineralogy of the podzolic portion of the profile is
dominated by vermiculite. Mica dominates the Bt and C
horizons (Arno et. al ca 1964). Percent silt plus clay averages
60 to 75%. Poorly drained depression sites have heavier
textures because of inwashed fines from seepage and overland
flow. Coarse fragment content within the profile averages 10
to 30%, usually increasing with depth. Lithic or veneer phases
may have increased coarse fragment contents especially
nearing the bedrock interface. The rock fragments are flat,
angular gravels (channers) of soft weathered shale-slate
derived from the underlying calcitic bedrock. Most fragments
are completely leached of carbonates, especially in the upper
profile. The soil parent material has been derived from rock
types that weather rapidly and are moderately rich in bases.
Inherent fertility is therefore high in comparison to other soil
associations but at the same time "wanting" because of natural
leaching due to rainfall. From an agricultural perspective
nutrient retention is good. There is a gradual increase in soil
reaction down the profile. The upper solum is acidic while the
lower solum is neutral grading into a weakly calcareous parent
44
material between 1 and 2 m from the mineral soil surface.
Shallow to bedrock phases are acidic throughout. Sites that
receive seepage are often enhanced with soluble bases that
have been leached from adjacent upland soils and bedrock
formations. Impeded drainage also results in less acid
leaching. For this reason depressions are often higher in
exchangeable bases (more nutrient rich) and thus have a higher
pH. Caribou soils are characterized by their noncompactness
and well developed structures. The upper solum is usually
friable to very friable, moderate to strong, medium, granular.
The Bt is friable to slightly firm with a moderate, medium,
subangular blocky structure. The subsoil is somewhat firm in
situ but is very friable when removed.
Caribou soils are primarily associated with soils of the
Carleton and Thibault associations, and to a lesser degree with
the Boston Brook, Violette and Holmesville associations.
Caribou, Carleton and Thibault soils have all developed on
parent materials derived from calcareous to weakly calcareous
rock types. Thibault soils are coarser-textured and often
referred to as "the coarse loamy phase of the Caribou
association". However, while well drained Caribou soils have
bisequal profile development with podzolic features over
luvisolic features, Thibault association soils lack any sign of
luvisolic features. The Carleton association is similar to the
Caribou association in that both soils are fine loamy and have
developed from parent materials derived from the same
lithological rock types. They differ in subsoil compaction.
Carleton soils are compact, Caribou soils are non-compact. In
some instances where the subsoils are only weakly compact,
separation of these two associations may be difficult. The
Caribou association is differentiated from the Boston Brook,
Violette and Holmesville soils on the basis of coarse fragment
lithology, particle size class, reaction,
and/or subsoil
consistence. Caribou is derived almost completely from
calcareous shale-argillite-slate. Boston Brook, Violette and
Holmesville are derived from acidic lithological rock types
such as quartzite, sandstone, argillite and slate. Both
Holmesville and Violette have developed on lodgment tills and
as such have dense compact subsoils. Holmesville soils are
also coarse loamy in comparison to the fine loamy Caribou.
Like Caribou soils, Boston Brook soils are fine loamy and noncompact in the subsoil. But Boston Brook soils have more
angular cobble-sized coarse fragments, the coarse fragments
are of acidic metasedimentary rock types, the subsoil pH is
more acidic and the subsoil consistence is more firm (com pact)
and less structured.
The Caribou association is considered highly suitable for
agriculture where surface relief is sufficient for external
drainage, but not excessively steep. The soil has a deep (50 cm
plus) available rooting zone with excellent nutrient and water
retention capacities. The soils are easily worked and retain
most of their structural integrity. From a forestry perspective
these soils are capable of supporting a wide range of
commercial species. They are comparatively high in natural
fertility.
Summary of general characteristics of the Caribou Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: CB
: Chaleur Uplands
: 300-500 m
: 82,212 ha
: 2.95%
: Mineral
: Glacial till, noncompact
:<3m
: Olive to olive brown
: Fine loamy
: Calcareous shale, argillite, slate and some
limestone
: High
: Undulating and rolling to hilly or sloping
(3-45%)
: Well to moderately well
: Podzolic Gray Luvisol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 50
50 - 100+
Texture Class
Silt loam
Clay loam
% Sand
30
35
% Silt
45
33
% Clay
25
32
% Coarse
Fragments
10 flat/angular G
25 flat/angular G
pH (H2 O)
5.3
6.0 - 7.0+
BD (g/cm3 )
1.20
1.55
Ksat (cm/hr)
2.5 - 10
0.5 - 2
AWHC (cm/cm)
0.25
0.20
Carleton Association
The Carleton association consists of soils that have developed
in neutral to weakly calcareous, fine loamy, compact morainal
till derived from calcareous shale, argillite and slate, and
occasionally some limestone. Deposits are typically less than
2 m thick (veneers and blankets) over bedrock. In veneer
phases, the transition from regolith to bedrock may be gradual,
with some in situ weathering of the underlying calcareous
bedrock. Carleton soils occur mostly in the Chaleur Uplands
portion of the study area (Fig. 18) at elevations between 300
and 500 m above sea level. They occupy approximately
85,211 ha, representing some 3.06% of the map area.
Carleton soil parent material is compact, and as such has been
considered to be a lodgment or basal till, laid down below the
glacier as it advanced. Most of the soil parent material has
been derived from the bedrock upon which it is presently
resting, with only minimal displacement. While the subsoil is
45
considered to be firm, it is not excessively so. The firm to
somewhat friable subsoil consistence is attributed to the
composition of the parent material. It is gravelly, which tends
to reduce its compatibility and it is also higher in pH. The
presence of available bases (ie. calcium from the calcareousrich bedrock debris) promotes physical and biochemical soil
forming processes that favour the development and
stabilization of soil structure.
Figure 18. Location of mapped Carleton soils.
Carleton soils consist of compact, fine loamy sediments with
an abundance of gravel-sized subangular and subrounded to
sharp, angular, flat coarse fragments derived from the
underlying weakly calcareous bedrock. Surface stoniness
ranges from slightly to moderately stony, with less than 3% of
the land surface occupied by coarse fragments. Well drained
Carleton soils have deve loped under a mixed
hardwood-softwood forest cover type consisting of red and
sugar maple, beech, birch, mountain ash, red oak, trembling
aspen, white pine, balsam fir and black and white spruce.
Poorly to very poorly drained members are dominated by
black spruce, balsam fir, white cedar, tamarack, red maple,
trembling aspen, black ash, and speckled alder.
The Carleton association is dominated by well to moderately
well drained Podzolic Gray Luvisols (Fig. 19) and Luvisolic
Humo-Ferric Podzols, but with some Orthic Humo-Ferric
Podzols. The Podzolic Luvisols and the Luvisolic Podzols have
overlying sequences of eluvial/illuvial horizons. The upper
sequence of horizons is typical of a podzol with development
of a Bf horizon. The lower sequence of horizons is typical of
a luvisol, with a distinct increase in clay content forming a Bt
horizon. Depth to the Bt horizon determines whether the soil
is classified as a Luvisolic or Podzolic intergrade, and where
Bt horizon formation is weak (more acidic sites), the profile is
classified solely as a Podzol. During soil formation acid
leaching removed free carbonates from the upper solum.
Wetting and drying cycles then lead to the dispersal of the very
fine clay component which was translocated with the
downward movement of water. Carbonates in the lower
profile caused the clays to flocculate, thus accumulating into a
Bt horizon. Thin to moderately thick clay films are present in
voids and root channels and on most vertical and horizontal
ped faces. Imperfectly drained sites are classified as gleyed
variants of their well-drained counterparts, Gleyed Podzolic
Gray Luvisols and Gleyed Hum o-Ferric Podzols. They may
also be Gleyed Brunisolic Gray Luvisols, indicating weaker
soil development than is found in the well to moderately well
drained sites. Poorly to very poorly drained sites are Orthic
Luvic Gleysols and Orthic Gleysols. They usually occur along
drainage channels and in depressions, interspersed in areas
dominated by well to moderately well drained soils. Carleton
soils have slow internal drainage. The upper solum is
estimated to have moderate to moderately rapid permeability
(2.5 to 10 cm/hr saturated hydraulic conductivity), but the
lower solum (Bt horizon) and subsoil have slow permeability
(0.1 to 0.5 cm/hr). Available moisture storage capacity ranges
from 0.25 cm/cm in the upper solum to less than 0.15 cm/cm
in the subsoil. The subsoils are dense and compact, but not
excessively so. Bulk densities of 1.70 to 1.80 g/cm3 are
common. In well to moderately well drained sites precipitation
is the dominant source of water. Downward movement of
excess moisture through the profile is impeded by the subsoil.
Lateral flow or seepage is common, especially on sloping
topography after heavy rains or follow ing snow melt.
Imperfectly and poorly to very poorly drained areas have
developed because of a combination of topographic position,
lack of gradient, subsoil compaction, seepage and high
groundwater table.
Soil development is quite thick, with solums ranging from 60
to in excess of 80 cm. This greater than normal thickness of
solum development can be attributed to the illuviation of clay.
Profile development is greatest in the well to moderately well
drained sites. The common horizon sequence is LFH, Ah, Ae1,
Bf, Ae2, Bt and C. The Ae1 horizon is usually thin and often
discontinuous. Faunal activity has created a moder-mull type
of forest humus form that may reach depths of 5 to 10 cm, at
the expense of the LFH and Ae horizons. However, conditions
also exist in which the Ah horizon may be almost completely
absent. The organic rich Ah is dark brown to black while the
Ae horizon is white to light grey. The Bf horizon is
characteristically strong brown to brownish yellow, becoming
paler with depth. Where clay translocation is weakly
expressed, the Bt horizon may not be present. The transition
to parent material is then designated as a BC horizon. Parent
material colours range from olive to olive brown. Imperfectly
drained Carleton soils have similar horizonation to their well
drained counterparts. The major differences morphologically
are the presence of mottles and gley features due to periodic
reducing conditions. Chemically, Fe and Al accumulation in
the upper B horizon is less than in the well drained member.
The upper B horizon in imperfectly drained soils ranges from
a Bf to a Bm (or Bfj). In poorly to very poorly drained profiles
the common horizon sequence is either LFH or O, Aeg, Btg
and Cg where there is a significant amount of clay
46
translocation; or, LFH or O, Ah, Aeg, Bg and Cg where clay
migration is less pronounced. The Carleton textural profile
consists of a loam to silt loam upper solum that grades into a
loam to clay loam or silty clay loam in the Bt and C horizons.
The clay content peaks in the Bt horizon. Poorly drained
depressional sites have heavier textures because of inwashed
fines from seepage and overland flow. Coarse fragment
content within the profile averages 10 to 30%, usually
increasing in abundance with depth. Lithic or veneer phases
may have increased coarse fragment contents especially
nearing the bedrock interface. Most fragments are completely
leached of carbonates, especially in the upper profile. The soil
parent material has been derived from rock types that weather
rapidly and are moderately rich in bases. Inherent fertility is
therefore high in comparison to other soil associations but at
the same time subjected to natural leaching due to rainfall.
From an agricultural perspective nutrient retention is good.
There is a gradual increase in soil reaction with depth. The
upper solum is acidic while the lower solum is neutral grading
into a weakly calcareous parent material between 1 and 2 m
from the mineral soil surface. Shallow to bedrock phases are
acidic throughout. “There are slight variations in texture, pH
and degree of leaching in the Carleton association. The degree
of leaching usually increases and the pH decreases as the
texture becomes lighter. It is also generally found that a welldrained porous soil on top of ridges and knolls is more acidic
and more leached then the average Carleton soil. Down the
slope the reaction of the soil gradually increases and the degree
of leaching decreases. This gradual change down the slope is
partly connected with the parent material of the soil. The
parent material of the Carleton series contains considerable
lime, which on weathering, is liberated into the soil and
subsequently washed down to the lower levels. This raises the
pH of the lower lying soils and consequently restricts the
leaching process.” (Stobbe 1940). Sites that receive seepage
are thus enhanced with soluble bases that have been leached
from adjacent upland soils and bedrock formations, resulting
in increased fertility. The upper solum is usually friable to
very friable, moderate to strong, medium, granular. The Bt is
firm, but with a moderate, medium, subangular blocky
structure. The subsoil increases in density with depth.
and slate while the Carleton association soils have been
derived from calcareous-rich rock types. Holmesville is coarse
loamy in comparison to the fine loamy Carleton, but Violette
is similarly fine loamy in composition and as such very similar
to the Carleton soil. In addition to different lithologies, subsoil
reaction and density are also used to separate the two
associations. Violette is acidic and more compact in the
subsoil than Carleton. Violette also has more cobble-sized
subangular coarse fragments throughout the profile.
Figure 19. Well drained Carleton soil profile.
Carleton soils are associated w ith other soils that have
developed on parent materials derived from calcareous to
weakly calcareous rock types - the Thibault and Caribou
associations.
Both of these soils have developed on
noncompact ablational tills and as such lack the compact
subsoil found in the Carleton soils. The Thibault soils are also
coarser textured than the Carleton soil. The Caribou
association is similar to the Carleton association in that both
soils are fine loamy and have developed from parent materials
derived from the same lithological rock types. They differ in
subsoil compaction. Carleton soils are compact, Caribou soils
are noncompact. In some instances where the subsoils are only
weakly compact, separation of these two associations may be
difficult. Carleton soils have also been mapped with Violette
and Holmesville soils. Both Violette and Holmesville soils
have been derived from acidic quartzite, sandstone, argillite
The Carleton association is considered highly suitable for
agriculture where surface relief is sufficient for external
drainage but not excessively steep. The soil has a relatively
deep (50 cm plus) available rooting zone with excellent
nutrient and water retention capacities. The soils are easily
worked and retain most of their structural integrity. From a
forestry perspective these soils are capable of supporting a
wide range of commercial species. They are comparatively
high in natural fertility.
Summary of general characteristics of the Carleton Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
: CR
: Chaleur Uplands
: 300-500 m
: 85,211 ha
47
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: 3.06%
: Mineral
: Glacial till, compact
:<2m
: Olive to yellowish brown
: Fine loamy
: Calcareous shale, argillite, slate and some
calcite
: High
: Rolling and undulating to hilly or sloping
(2-100%)
: Well to moderately well
: Podzolic Gray Luvisol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 50
50 - 100+
Texture Class
Loam
Loam - clay loam
% Sand
40
40
% Silt
40
29
% Clay
20
31
% Coarse
Fragments
15 subangular G/C
25 subangular G/C
pH (H2 O)
5.0 - 5.5
6.0+
BD (g/cm3 )
1.20
1.75
Ksat (cm/hr)
2.5 - 10
0.1 - 0.5
AWHC (cm/cm)
0.25
< 0.15
Figure 20. Location of mapped Catamaran soils.
Catamaran Association
The Catamaran association consists of soils that have
developed in moderately thin (most less than 2 m thick)
deposits of acidic, coarse loamy compact morainal till. This
association has been used to describe soils that occur mostly in
an area along the eastern boundary of the New Brunswick
Central Highlands physiographic region (Fig. 20), where the
glacial till has been derived from a mixture of Devonian
granites and Ordovician and Silurian greywacke, schists,
quartzite, slates and sandstones. Elevations range from 120 to
400 m above sea level. Other occurrences of Catamaran soils
are found north of Fredericton and west of Bathurst. In total
these soils occupy approximately 133,044 ha or 4.77% of the
total map area.
Catamaran parent material has been deposited as ground
moraine, basal till plastered in place during glacial advance and
subsequently covered w ith a thin discontinuous mantle of
ablational till upon glacial retreat. Both materials are of
similar composition. Mixing actions of soil formation have
obliterated most evidence of the ablational capping. Only in
areas where the noncompact ablational material is significantly
thicker than the average depth of soil development can the two
materials be positively identified. These represent very small
areas, being the exception rather than the rule. In most profiles
the solum is underlain by a dense compact lodgment till
subsoil (Fig. 21). Because of the relatively thin nature of these
deposits, the surface expression generally reflects the
topography of the underlying bedrock. Landforms consist
largely of blankets and to a lesser extent veneers over an
undulating to rolling (2 to 15% slope) and sometimes hilly,
inclined or sloping (9 to 45% slope) bedrock. Relief is a
function of distance from the Maritime Plain, with more
strongly expressed topographic conditions occurring in the
central portions of the Highlands. Although the regolith is
thin, the material is uniform in thickness. Seldom are there
significant bedrock outcrops (ie. exposures covering more than
2% of the surface) to warrant consideration. Well drained
Catamaran soils support mixed softwood-hardwood stands of
balsam fir, black spruce, red spruce, white birch, yellow birch,
red oak and sugar and red maple. Forest cover on poorly
drained sites is comprised of balsam fir, black spruce, cedar,
red maple, tamarack and some yellow birch.
Drainage of Catamaran soils ranges from good to poor, but
well and imperfectly drained associates dominate. They are
classified as Orthic Humo-Ferric Podzols (Fig. 21) and Gleyed
Humo-Ferric Podzols, respectively. Most profiles show some
tendency of intergrading towards soils of the Ferro-Humic
Podzol great group, with a thin (less than 10 cm thick) Bhf in
the upper B horizon. Higher effective precipitation due to
cooler temperatures results in environmental conditions in
central New Brunsw ick that are conducive to organic matter
accumulation in the B horizon and thus the formation of a Bhf.
Poorly drained Catamaran soils are classified mainly as Orthic
or Fera Gleysols, and occasionally as Orthic Humic Podzols.
Internal drainage is somewhat impeded by the subsoil which
has an estimated slow permeability rate of 0.1 to 0.5 cm/hr.
Available water storage capacity is estimated at 0.15 to 0.25
48
are slow. The F horizon dominates over the H horizon. The
light grayish coloured Ae overlies the dark reddish brown
coloured Bhf which in turn changes abruptly to a 10 to 25 cm
thick, yellowish brown coloured Bf horizon. The Bf horizon
grades through a transitional BC horizon into a compact C
horizon. The C horizon often has fragipan formation, which
when moist, is difficult to differentiate from the compact
parent material. When dry, the fragic material is brittle and
slakes in water.
Well drained profiles with fragipan
development are classified as Fragic Humo-Ferric Podzols.
However, most of the fragipan in Catamaran soils is weakly
expressed and limited in areal extent. Imperfectly drained
members of the Catamaran association have a similar sequence
of horizons, but display distinct or prominent mottling,
especially along the contact of the dense, compact subsoil.
Gleying becomes more prominent in lower site positions.
Poorly to very poorly drained Catamaran soils have profiles
consisting of LFH or O, Aeg, Bg or Bgf, and Cg. The
predominance of coniferous forest vegetation on these sites
encourages mosses and the accumulation of thicker organic
layers. Lithic phases of Catamaran occur randomly in well,
imperfectly and even some poorly drained locations, wherever
bedrock is near the surface. With the exception of being
somewhat abbreviated, profile characteristics are similar to the
aforementioned.
Figure 21. Moderately well drained Catamaran soil profile.
cm/cm in the solum and less than 0.15 cm/cm in the subsoil.
Well to moderately well drained Catamaran soils have
developed in areas where steeper topography permits adequate
site drainage. They occupy crest to mid-slope positions in
rolling landscapes, but may also occupy lower slope positions
in hilly, inclined and strongly sloping areas. Precipitation is
the dominant water source but additions by subsurface flow are
also significant in moderately well drained sites. Excess water
flows both downward through the underlying parent material
and laterally as subsurface flow. Seepage along the subsoil
contact is common during periods of excess moisture. ie. after
heavy rainfalls and following snowmelt. Poorly drained
Catamaran soils occur on level to gently undulating terrain
characterized by slow runoff, or in depressions and along
drainage ways in areas with more relief (rolling, hilly and
sloping topography). Groundwater flow and subsurface flow
are the major water sources. Imperfectly drained sites are
frequently the result of a temporarily perched water table
where precipitation and lateral flow exceed downward
permeability and evapotranspiration.
Solum thickness ranges from 40 to 50 cm. On well drained
sites the common horizon sequence is LFH, Ae, Bhf, Bf, BC
and C or Cx. The upper horizons, LFH, Ae, and Bhf are all
relatively thin (3 to 10 cm) but distinct in appearance.
Mineralization and humification processes in the organic layer
The Catamaran texture profile consists of a loam to sandy loam
throughout, with 8 to 18% clay content. Weathering within the
solum may result in a slightly finer texture in the upper profile
than in the subsoil, however, this variation is still within the
loam-sandy loam grouping. Profile coarse fragment content
ranges from 10 to 25% with subangular cobbles and gravels
the dominant size class. Most Catamaran land surfaces are
moderately to very stony with stone-sized clasts occupying 2
to 15% of the area. Usually these soils are also moderately to
very cobbly with surface coverage similar to that of the stones.
Surface boulders are present but not in significant quantities to
warrant designation. Catamaran soils are low to medium in
natural fertility. The granitic parent rocks weather slowly and
yield relatively infertile soil material. The non-granitic
component tends to weather more rapidly and yield more
nutrient-rich soil. Soil reaction increases with depth but both
the solum and subsoil are acidic, falling within a pH(H 2O)
range of 4.0 to 5.5. The solum is weak to moderate, fine to
medium, granular to subangular blocky structured and very
friable. It provides a 40 to 50 cm potential rooting zone. The
parent material is firm to very firm, compact, and slightly
cemented in the upper C horizon. The C horizon is usually
pseudoplaty in situ but breaks to medium subangular blocky
when extracted.
Catamaran soils found along the Plaster Rock-Renous highway
occupy a bedrock zone that separates the Long Lake-McGee
association parent materials to the northwest, the Juniper
association parent material to the west and the Reece
association parent material to the east. Juniper soils are readily
differentiated from Catamaran soils on the basis of a number
of properties, the most obvious being subsoil consistence,
49
coarse fragment content and lithology. Juniper soils have a
noncompact subsoil, 20 to 50% coarse fragment content and
granitic lithology. Catamaran soils have a compact subsoil, 10
to 2 5 % c o a r se fragm ent co n t e n t an d m i x ed
granitic-metamorphic lithology. Reece soils are similar in
morphology but are fine loamy (greater than 18% clay content)
whereas Catamaran soils are coarse loamy (less than 18% clay
content). Reece soils are also derived from sandstone and
shale bedrock types. Long Lake soils are closest to the
Catamaran association in terms of physical, chemical and
morphological properties. Long Lake soils are coarse-loamy
with compact subsoils, but they are derived from slate,
siltstone, argillite, schist and miscellaneous quartzite and
greywacke.
Biological production on Catamaran soils is affected by low to
medium inherent fertility, surface stoniness, depth to a
root/water restricting layer, climate, and to a lesser degree
wetness and topography. These limitations more severely
handicap agriculture than forestry. Agricultural potential is
marginal. Catamaran soils should prove adequate to support
moderately productive stands of forest tree species climatically
suited to the region.
Ksat (cm/hr)
2.5 - 10
0.1 - 0.5
AWHC (cm/cm)
0.15 - 0.25
< 0.15
Gagetown Association
The Gagetow n Association consists of soils developed in thick
deposits (some in excess of 20 m) of noncalcareous, sandy
skeletal, glaciofluvial material with mixed igneous and
metamorphic coarse fragment rock types. There soils occur in
small tracts scattered throughout the central New Brunswick
Highlands and coastal Maritime Plain regions of the survey
area (Fig. 22).
Gagetown association soils cover
approximately 44,150 ha or 1.58% of the map area.
Summary of general characteristics of the Catamaran Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: CT
: N. B. Highlands
: 120-400 m
: 133,044 ha
: 4.77%
: Mineral
: Glacial till, compact
:<2m
: Yellowish brown to olive brown
: Coarse loamy
: Granite, schist, quartzite, slate and
sandstone
: Medium
: Rolling and undulating to hilly or sloping
(2-45%)
: Well to moderately well
: Orthic Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Loam - sandy loam
Sandy loam
% Sand
50
60
% Silt
35
30
% Clay
15
10
% Coarse
Fragments
15 subangular C/G
20 subangular C/G
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.20
1.80
Figure 22. Location of mapped Gagetown soils.
Gagetow n soils are found on eskers, kames, kame terraces and
deltas, kame and kettle complexes, outwash plains and fans
and valley trains. Surface expressions vary from gently
undulating plains with less than 5% slopes to hummocky,
terraced or sloping landscapes with slopes ranging from 2 or
3% to in excess of 45%. Steep complex slopes are the rule
rather than the exception. Many of these depositions are
associated with present day river valleys along the Nepisiguit,
Tetagouche, Miramichi and Nackawic Rivers and their
tributaries. Other deposits traverse the landscape, showing
little or no conformity to existing relief or topography. These
were englacial stream flow sediments which were left
behind upon glacial retreat. Most sediments consist of well
stratified sands and gravels with some cobbles. Bedding is
commonly skewed from the horizontal and particle size
distribution may vary abruptly and significantly from one layer
to the next. Most of the finer materials (silts and clays) have
been washed out during deposition. Boulders and stones
occasionally occur, both on the surface and within the soil
profile, the result of ice-rafted debris. However, most units are
nonstony. Gagetown soils usually support forest stands of
50
predominantly softwoods, jack pine and black spruce, with
some grey birch on the drier sites. Wetter sites along river
bottoms encourage stands of black spruce, red maple and white
birch.
The Gagetown Association is dominated by well to rapidly
drained Orthic Humo-Ferric Podzols (Fig. 23) and Eluviated
Dystric Brunisols. Significant areas of gleyed phases of the
aforementioned subgroups occupy imperfectly and poorly
drained sites, with some Orthic Gleysols on very poorly
drained locations. On well to rapidly drained sites the sole
source of water is precipitation. Excess rainfall quickly
dissipates since the underlying material is very rapidly
permeable (usually greater than 25 cm/hr). These soils have a
low to very low available water storage capacity, 0.10 cm/cm
or less. In imperfectly and poorly drained sites excess water is
the result of a high ground water table. Off drainage occurs in
depressions and lower terrace site positions along some stream
and river valleys.
Figure 23. Rapidly drained Gagetown soil profile.
The solum of Gagetown Association soils varies from 35 to 45
cm in thickness. Solum thickness is related to the prevailing
moisture regime. Well to somewhat imperfectly drained soils
have the thickest development, followed by rapidly
(excessively) and then poorly to very poorly drained soils. The
common horizon sequence in well to rapidly drained soils is:
LFH, Ae, Bf or Bm, BC and C. Imperfectly to poorly drained
profiles have: LFH or O, Ae, Bfgj or Bmgj, BCgj or BCg and
Cg ; and very poorly drained profiles: LFH or O, Aeg, Bg and
Cg. The surface horizons of Gagetown soils are relatively
devoid of the stratification or layering so prevalent and
characteristic of the parent material. The non-stratified nature
of these upper horizons can be attributed to pedogenic
activities of soil mixing by microorganisms, frost action and
tree windthrow. Pedogenic weathering has also resulted in
increased levels of silt and clay (fines) in the solum. The
Gagetown texture profile usually grades from a gravelly loamy
sand to sandy loam solum into a gravelly to very gravelly
loamy sand to sand subsoil. Coarse fragment content varies
from occasionally less than 20% in the solum to more than
70% in the C horizon or parent material, usually increasing
with depth. Most coarse fragments are rounded or subrounded
gravels, 0.2 to 7.5 cm in diameter, however some larger
cobbles may occur. The coarse fragments are derived from
granites, granite gneiss, schists, quartzite, basalt and related
lithologies. Gagetown soils are very low in natural fertility.
They are also acidic throughout the profile, with pH(H 2O)
ranging from 4.0 to 5.5. In well drained soils the parent
material colour is yellow ish brown to brown. The solum
consists of a light gray Ae horizon and a yellowish brown to
strong brown and occasionally even reddish brown Bf or Bm
horizon. Imperfectly and poorly drained members have either
distinct or prominent mottling. Poorly and very poorly drained
members are gleyed with gray to olive gray colours of low
chroma. The subsoils are loose and single grain, while the sola
are for the most part very friable, very weak, fine to medium
granular. In exception to this is the presence of ortstein, a
hardpan that occurs sporadically throughout Gagetown soils.
Iron, aluminum and organic complexes are the cementing
agents that result in massive to slightly platy, irreversible Bfc
horizons. Ortsteins usually form 10 to 15 cm below the
mineral soil surface. The upper boundary of the ortstein is
abrupt and cementation decreases near the lower boundary
some 10 to 45 cm below. Ortstein is most strongly expressed
under poorly drained conditions, however, even here it is
discontinuous. Massive blocks of cemented ortstein materials
are frequently observed in gravel pits where G agetown soil
parent materials are being extracted.
The Gagetown catena has formed in glaciofluvial material
derived primarily from igneous and highly metamorphosed
rocks. It is found in areas dominated by soils formed from
similar rock types, such as the Juniper, Catamaran, Popple
Depot and Tuadook Associations. However, these are till soils
and readily distinguished from Gagetown. Catamaran, Popple
Depot and Tuadook are nonstratified deposits with angular
coarse fragments, finer textures and have compacted subsoils.
Juniper, an ablational till, is similar to Gagetown owing to its
mode of deposition. Depending upon the degree of waterworking during deposition, some Juniper soils may closely
resemble Gagetown soils. The modal Juniper soil is readily
differentiated from Gagetown on the basis of its non-stratified,
heterogeneous nature and the presence of more angular coarse
fragment shapes. Gagetown soils also occupy the same type of
51
landforms as a number of other associations formed in fluvial
sediments - Grand Falls, Riverbank, Interval and Maliseet.
Geographically, the Gagetown association is most closely
associated with the Riverbank and Interval associations.
Differentiation among associations formed in fluvial
sediments is made on the basis of particle size or coarse
fragment lithology. The Interval and Maliseet associations are
coarse loamy; the Riverbank association is sandy; and the
Grand Falls association is sandy skeletal but with noncalreous
shale, quartzite, slate and sandstone coarse fragments. In
comparison, the Gagetown association is sandy skeletal and
has granite, granite gneiss, basalt and some quartzite coarse
fragments.
All uses of Gagetown soils for biological production, be it
agriculture or forestry, are limited by the soils low water
holding capacity and fertility related problems - low inherent
fertility and low fertility retention. Forest tree species selection
must be done with these limitations in mind. Imperfect to very
poorly drained members also have added problems of
excessive wetness, typically due to topographic position.
However, Gagetow n soils are readily drained by tile drainage
systems. Gagetown soil parent material is an excellent source
of aggregate for road building, construction and related uses.
It is extracted for local use from numerous sites.
BD (g/cm3 )
1.20
1.55
Ksat (cm/hr)
> 25
> 25
AWHC (cm/cm)
< 0.10
< 0.05
Grand Falls Association
The Grand Falls Association consists of soils developed in
thick deposits (often in excess of 20 m) of acidic, sandy
skeletal, glaciofluvial material with noncalcareous slate, shale,
quartzite and sandstone coarse fragments. The glaciofluvial
material is underlain by glacial till or bedrock. These soils
occur in small tracts scattered throughout the Chaleur Uplands
and New Brunswick Highlands regions of the survey area (Fig.
24). Grand Falls association soils cover approximately 24,264
ha or 0.87% of the map area.
Summary of general characteristics of the Gagetown Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: GG
: N. B. Highlands, Maritime Plain
: up to 300 m
: 44,150 ha
: 1.58%
: Mineral
: Fluvial (glaciofluvial)
: Up to 20 m
: Yellowish brown to brown
: Sandy skeletal
: Mixed igneous and metamorphic and
some sedimentary
: Low
: Terraced, undulating and hummocky (245%)
: Rapid
: Orthic Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 40
40 - 100+
Texture Class
Loamy sand
Loamy sand - sand
% Sand
80
85
% Silt
10
10
% Clay
10
5
% Coarse
Fragments
25 rounded G
60 rounded G
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
Figure 24. Location of mapped Grand Falls soils.
Grand Falls soils were deposited as river terraces, outwash
plains or kames or eskers. The topography is either
hummocky ie, knob-and-kettle; terraced, with horizontal or
gently inclined terraces separated by steeply sloping scarp
faces; or undulating. The knob-and-kettle topography consists
of a disordered assemblage of knolls or "knobs" interspersed
with irregular depressions or "kettles" that are commonly
poorly drained or even swamps or ponds. The terraces are
long, narrow surfaces running parallel to streams and rivers,
marking a former water level. The esker deposits are long,
narrow, low, sinuous, steep-sided ridges or mounds. Most of
the Grand Falls soils mapped are located along present day
drainage systems, however, some minor deposits are known to
occur in isolated areas far removed from any existing
waterways. These have been deposited by streams within
glacial ice and then subsequently laid down upon glacial
retreat, thus show ing little or no conformance to local relief.
Most sediments consists of well stratified sands and gravels
52
with some cobbles. The soil and rock fragments are smooth
and rounded. The layers or strata vary in thickness and
composition, a reflection of the changing environmental
conditions during which they were deposited. Although some
erratic surface boulders and stones may be found, Grand Falls
soils are considered to be nonstony. The major forest species
on well to rapidly drained sites are black spruce, balsam fir and
white and yellow birch. Poorly to very poorly drained lower
slopes and depressions support communities of black spruce,
balsam fir, red maple and white birch.
The Grand Falls Association is dominated by well to rapidly
drained Orthic Humo-Ferric Podzols (Fig. 25). Gleyed
Humo-Ferric Podzols occupy imperfectly drained sites, and
Gleyed Humo-Ferric Podzols, Gleyed Eluviated Dystric
Brunisols, Orthic Gleysols and Rego Gleysols occur on poorly
to very poorly drained sites. The subsoil parent material is
very rapidly permeable (usually greater than 25 cm/hr) and so
on elevated, rapidly to well drained sites, excess precipitation
readily flows downward through the profile. These soils have
low available water storage capacity within the control section,
averaging 0.10 cm/cm or less. The available water storage
capacity decreases with depth, a reflection of coarser soil
materials and increased gravel content. Upper solum water
holding capacities are enhanced by their finer textures and the
presence of organic matter. Precipitation is the sole source of
water on these sites. Off-drainage (imperfect, poor and very
poor drainage) is the result of high ground water tables and
groundwater flow. Most Grand Falls soils are either dry (well
to excessively drained) or wet (poorly to very poorly drained).
Areas of imperfect drainage are restricted to subdominant
components of map units of the above mentioned drainage
categories.
The depth of the solum of Grand Falls Association soils varies
from 35 to 55 cm. Thickest solum development is found on
well to imperfectly drained sites. Sites with moisture regimes
at the extremes, either excessively dry or excessively wet, tend
to have shallow er solum development. The common horizon
sequence in well to rapidly drained soils is: LFH, Ae, Bf, BC
and C. At higher elevations where there is greater effective
precipitation, increased accumulation of organic matter in the
upper podzolic B horizon leads to the formation of a thin Bhf
horizon. Imperfectly drained profiles have: LFH, Ae, Bfgj,
BCgj and Cg horizons, indicating the presence of distinct or
prominent mottles. Poorly to very poorly drained soils have
horizons sequences of: LFH, Ae, Bmgj or Bfjgj and Cg; LFH
or O, Aeg, Bg and Cg; or LFH or O and Cg as drainage gets
progressively worse. The stratification so characteristic of the
soil parent material is not present in the solum. Mixing actions
of soil organisms, frost churning and tree uprooting
(windthrow) have altered the upper soil profile, obliterating
any of its original stratification. The Grand Falls texture
profile usually grades from a gravelly sandy loam to loamy
sand, and occasionally even loam, solum into a gravelly to
very gravelly loamy sand to sand subsoil. In poorly drained
sites inwashed fines (siltation) may make the surface material
slightly heavier. Coarse fragment content increases with depth
to in excess of 70% in some strata (layers) in the parent
material. Percentage coarse fragment content varies from one
stratum to another. Most coarse fragments are round-edged,
flat, elongated gravels or channers, 0.2 to 15 cm long. These
channers are derived from slate, shale, quartzite, sandstone and
related lithologies. The characteristic channer shape is an
inherited feature from these rock types. Grand Falls soils are
low in natural fertility. Profiles are acidic throughout, with
pH(H 2O) values ranging from 4.0 to 5.5. In well drained soils
the parent material colour is olive brown. The solum consists
of a relatively thin (1-5 cm) LFH horizon over a light to
pinkish gray Ae which is underlain by a brownish or reddish
yellow to strong brown coloured Bf. Imperfectly drained soils
have iron mottling of high chroma and value in the lower B
and C horizons. Poorly drained soils are characterized by gray
colours and prominent mottling indicative of intense reducing
conditions. Matrix chromas are generally 2 or less. The
subsoils are loose and single grain, while the sola are very
friable to friable, with weak, fine to medium, granular structure
in the B horizon and weak, fine, platy structure in the A
horizon. Cementation of the B horizon occurs in some profiles.
This is the result of ortstein or hardpan formation. It is
discontinuous and very sporadic in its occurrence.
Figure 25. Rapidly drained Grand Falls soil profile.
Grand Falls soils are found in areas dominated by soils formed
53
from shale, slate, quartzite and sandstone, such as the
Holmesville, Long Lake and McGee associations. However,
these are till soils and readily distinguished from Grand Falls
soils. These till soils are nonstratified deposits with angular
coarse fragments (cobbles, gravels, and stones), finer textures
and have friable to very firm subsoils. Grand Falls soils
occupy the same type of landscapes as do a number of other
soils formed on fluvial sediments: Gagetown, Interval and
Maliseet. They are differentiated on the basis of soil particle
size class and coarse fragment lithology. Interval and Maliseet
are coarse loamy nonskeletal materials. Gagetown is sandy
skeletal, but dominated by igneous coarse fragments.
Biological production on Grand Falls soils is limited because
of low fertility retention and low water holding capacity. Finertextured surface soil in some deposits helps but does not
completely alleviate this problem. Retention characteristics of
the subsoil are still problematic. Excessive wetness is an
additional problem on poorly drained sites. Grand Falls soil
parent material is an excellent source of aggregate for road
building, construction and related uses. It is extracted for local
use from numerous sites.
Ksat (cm/hr)
> 25
> 25
AWHC (cm/cm)
< 0.10
< 0.05
Guimond River Association
The Guimond River Association consists of soils developed in
relatively thick deposits (sometimes in excess of 10 m) of
acidic, sandy skeletal, glaciofluvial material with coarse
fragments of soft sandstone. The glaciofluvial sediments are
underlain by either bedrock, or a thin mantle of glacial till over
the bedrock. Guimond River soils are found only on the
lowlands or Maritime Plain (Fig. 26). All deposits occur at low
altitude, less than 100 m above sea level, and so were subjected
to a short (approximately 2000 years) period of post glacial
marine submergence. They occupy approximately 2169 ha or
0.08% of the map area. Occurrences are scattered and small
in size.
Summary of general characteristics of the Grand Falls Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: GF
: N. B. Highlands, Chaleur Uplands, Notre
Dame Mountains
: 300-600 m
: 24,264 ha
: 0.87%
: Mineral
: Fluvial (glaciofluvial)
: Up to 20 m
: Olive to olive brown
: Sandy skeletal
: Noncalcareous slate, shale, quartzites and
sandstones
: Low
: Terraced and hummocky to undulating
and rolling (0.5-15%)
: Rapid
: Orthic Humo-Ferric Podzol
Figure 26. Location of mapped Guimond River soils.
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Sandy loam - loamy
sand
Loamy sand - sand
% Sand
75
90
% Silt
15
5
% Clay
10
5
% Coarse
Fragments
35 rounded, flat,
elongated G
60 rounded, flat,
elongated G
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
1.20
1.50
3
BD (g/cm )
Guimond River soils were deposited as river terraces, outwash
plains, eskers, beach ridges and related landscapes. Typically
they are found close to flowing water, but not necessarily.
Englacial sediments deposited during glacial retreat do not
always conform to present day relief. Landform surface
expressions vary from gently undulating with slopes of less
than 5%, to sloping terraced configurations with complex,
irregular slopes of up to 30%. Valley fills of Guimond River
materials are common. The sediments consist of well stratified
sands and gravels with some cobbles. Water working has
resulted in most soil and gravel fragments being smoothed and
well rounded. Changing conditions during the time of
deposition is reflected in an alternation of sediment beds that
show no regular sequence and considerable variation in
thickness and texture. Guimond River soils are nonstony, with
the exception of the occasional ice rafted erratic stone or
54
boulder. Well to rapidly drained sites support stands dominated
by jack pine and black spruce, with minor inclusions of red
pine and stunted white birch. Ill-drained sites in depressions
or along drainage channels have forest stands of black spruce,
balsam fir, red maple and some birch and alder.
The Guimond River association is dominated by well to
rapidly drained Orthic Humo-Ferric Podzols and Eluviated
Dystric Brunisols. Imperfectly to poorly drained sites are
classified as gleyed phases of the aforementioned subgroups.
Very poorly drained soils are frequently classified as Orthic
Gleysols. The entire depth of the soil (greater than 100 cm)
consists of a very rapidly permeable material with saturated
hydraulic conductivities of 25 cm/hr and faster. Coarse texture
results in a low available water storage capacity of 0.10 cm/cm
or less. The available water storage capacity is highest in the
solum where textures are slightly finer and less gravelly, and
organic matter is present in significant quantities. Precipitation
is the sole source of water on well to rapidly drained sites. In
poorly drained sites precipitation supplements groundwater
flow, which is the dominant factor determining drainage. In
the catenary sequence the transition from rapidly drained to
poorly drained soils is abrupt, occurring over a relatively short
horizontal distance. Imperfectly drained soils are usually only
subdominant components of map units dominated by either
well to rapidly drained soils or poorly to very poorly drained
soils.
Solum development in Guimond River soils varies from 30 to
50 cm in depth, where it gradually merges into the
unweathered regolith or subsoil. Well-aerated conditions
promote thicker sola than in poorly drained sites. This may be
somewhat negated on rapidly drained sites that are excessively
droughty. Moisture deficiencies lead to reduced rates of soil
genesis. Poorly drained soils may have more than 20 cm of
organic debris accumulation on the surface. The common
horizon sequence is: in well to rapidly drained soils, LFH, Ae,
Bf or Bm, BC and C; in imperfectly to poorly drained soils,
LFH or O, Ae, Bfgj or Bmgj, BCg and Cg; and in very poorly
drained soils, LFH or O, Aeg, Bg and Cg.
Postglacial marine submergence (wave washing, sediment
deposition and erosion) and soil forming processes have
created solum conditions that vary from the subsoil. The
solum is nonstratified and finer textured and less gravelly than
the subsoil. Marine submergence was brief and consisted more
of an estuarial environment of brackish water rather than salt
water. Some sediments may have been deposited
subaqueously. However, chemical alterations as a result of this
marine inundation have long since been leached out. The
Guimond River texture profile consists of gravelly to
nongravelly sandy loam to loamy sand A and B horizons over
a gravelly to very gravelly loamy sand to sand subsoil. Coarse
fragment content increases with depth. It ranges from 35 to
70%. Most coarse fragments are rounded gravels, 0.2 to 7.5
cm in diameter. They are derived from the gray-green
Pennsylvanian sandstone that underlies the coastal plain.
Minor inclusions of red Pennsylvanian sandstone and some
non-sandstone components from the highlands may be present.
The gray-green sandstone is relatively soft ( less than 4 Mohs
scale), medium to fine-grained, and contains 60 to 85%
feldspars and 5 to 10% biotite and muscovite. Guimond River
soils are very low in natural fertility and acidic throughout the
profile, with pH(H 2O) values of 4.0 to 5.5. In well to rapidly
drained soils the parent material is olive to yellowish brown.
The solum consists of a light grayish coloured eluvial Ae
horizon with an abrupt boundary to a reddish brown to
yellowish brown B horizon that becomes progressively
yellower in hue as it grades into the BC and C horizons.
Mottles and grayish gley colours are found in imperfectly and
poorly drained conditions, but for the most part the general
podzolic or brunisolic horizon sequence is maintained. The
subsoil is loose and single grain while the solum is usually
very friable, very weak, fine to medium granular. Ortstein, an
irreversible hardpan, occurs sporadically in the B horizon of
Guimond River soils. Iron, aluminum and organic matter
complexes cement the sand grains together into a very firm,
compact, massive but discontinuous layer. Ortstein is most
strongly expressed under poorly drained conditions.
The Guimond River association is found on the eastern coastal
plain portion of the study area, interspersed between units of
Reece, Stony Brook and Sunbury till soils. The Reece and
Stony Brook soils are compact lodgment tills and readily
distinguished from the Guimond River association. Sunbury
soils are similar lithologically in that their coarse fragments are
derived from soft sandstone. But Sunbury soils are finer
textured in the parent material and consist of nonstratified
glacial drift with angular and flaggy coarse fragments.
Guimond River soils are most closely associated with
Richibucto soils. Both were deposited by water and they
occupy similar landscapes positions. However, Richibucto
soils are non-skeletal; they are relatively coarse fragment-free
sandy materials.
Very low water holding and nutrient retention capacities effect
all uses of Guimond River soils for biological production of
forest and agricultural crops. Forest tree species selection in
particular must be made with these limitations in mind.
Guimond River parent material is a source of aggregate used
for buildings, road construction and related activities. Quality
is a problem with these materials. The sandstone clasts are
considered to be unsound. The gravels are soft and rapidly
break down into their initial components, ie. sand, making
them lower quality gravel sources.
Summary of general characteristics of the Guimond River Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
: GM
: Maritime Plain
: < 100 m
: 2169 ha
: 0.08%
: Mineral
: Fluvial (glaciofluvial), possibly marinemodified
: Up to 10 m
: Olive to yellowish brown
55
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: Sandy skeletal
: Soft gray-green sandstone
: Very low
: Undulating (0.5-5%)
: Rapid
: Orthic Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 40
40 - 100+
Texture Class
Sandy loam - loamy
sand
Loamy sand - sand
% Sand
80
90
% Silt
10
5
% Clay
10
5
% Coarse
Fragments
30 rounded G
60 rounded G
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.20
1.50
Ksat (cm/hr)
> 25
> 25
AWHC (cm/cm)
< 0.10
< 0.05
Holmesville Association
The Holmesville association consists of soils that have
developed in relatively thin (1 to 3 m thick) deposits of acidic,
coarse loamy, compact morainal till sediments derived from
quartzite and sand stones with miscellaneous argillite, slate
and schists. They occur in the Chaleur Uplands, Central
Highlands and Notre Dame Mountains physiographic regions
of the study area (Fig. 27) at elevations of 300 to 600 m above
sea level. Holmesville soils occupy approximately 72,592 ha,
or 2.60% of the map sheet.
The soil parent material has been deposited as ground moraine,
plastered in place under the weight of advancing glacial ice.
However, it is possible that the loose material in which the
solum formed is a thin layer of ablational till, derived from the
same bedrock sources, deposited on top of the ground moraine
by melting ice during glacial retreat. As a result, there are
varying depths of the loose material overlying the compact till.
Composition strongly reflects the incorporation of local
bedrock formations. The till is a heterogeneous mixture of
angular to subrounded shaped particle sizes ranging from silts
and clays to cobbles and stones. Coarse fragment shapes are a
function of the parent bedrock but have been somewhat
rounded by basal till grinding actions. Contents typically vary
from 10 to 30% with a high percentage of gravels and cobbles.
Holmesville soils are generally not too stony to prevent their
use for agriculture, with usually less than 3% of the land
Figure 27. Location of mapped Holmesville soils.
surface area occupied by coarse fragments. Frost action may
concentrate profile cobbles on the mineral soil surface under
the forest floor in imperfectly and poorly drained sites.
Boulders are not common. Holmesville landforms are
dominated by undulating, rolling and occasionally hilly surface
expressions with slopes varying from 2 to 45%, but mostly in
the 2 to 15% range. Holmesville soils occur on bedrock
controlled topography with most map units averaging only 1
to 2 m of soil material. Veneer phases are associated with
areas of steeper topography and bedrock outcrops that occur
are usually associated with these areas. Well drained soils of
the Holmesville association support forest communities of
sugar maple, beech, yellow birch, red oak, red and white
spruce, balsam fir, red maple, white pine, trembling aspen, pin
cherry, striped maple and mountain maple. On poorly to very
poorly drained sites the tree vegetation consists of black
spruce, cedar, speckled alder and balsam fir, with some red
maple and tamarack.
Holmesville soils are dominated by well drained Orthic
Humo-Ferric Podzols (Fig. 28). Well drained conditions
dominate where more steeply sloping hilly and rolling
landscapes occur. In these landforms poorly and imperfectly
drained conditions are confined to relatively narrow drainage
channels. More significant hectarages of imperfectly and
poorly drained Holmesville soils occur as Gleyed Humo-Ferric
Podzols and Orthic Gleysols, respectively, in areas of
undulating to gently rolling topography. Internal drainage is
restricted by a slowly to moderately slowly permeable subsoil
with an estimated saturated hydraulic conductivity value of 0.1
to 1.0 cm/hr. Available water storage capacity ranges from
0.25 to less than 0.15 cm/cm, decreasing with depth because of
reduced total porosity in the compact subsoil. Well drained
sites are supplied with water solely via precipitation.
Downward movement of excess moisture through the profile
is impeded by the subsoil, resulting in lateral flow or seepage,
particularly in the spring after snowmelt. Imperfectly and
poorly to very poorly drained areas have developed because of
a combination of topographic position, lack of gradient, subsoil
56
compaction, seepage and high groundwater table.
lack a podzolic B horizon. They consist of LFH or O, Aeg,
Bg, BCg, and Cg horizons. The forest duff layer is thicker in
the poorly and very poorly drained conditions than found in
well drained counterparts, varying from 5 to 15 cm, but is
occasionally as thick as 30 cm. The Holmesville textural
profile consists of a loam to sandy loam (8 to 18% clay)
throughout. Profile coarse fragment content varies from 10 to
30%, with a preponderance of subangular to somewhat
subrounded gravels and cobbles. Holmesville soils are
medium in inherent fertility and acidic throughout, with
pH(H 2O) values of 4.0 to 5.5. The friable to very friable, weak
to moderate, fine to medium, granular or subangular blocky
solum overlies a firm to very firm, massive to medium platy
subsoil. The subsoil shatters readily upon extraction.
The Holmesville association is most comm only found with
members of the Long Lake and McGee associations. The three
soils have been derived from materials of similar lithological
origin, mostly metasedimentary rock types. Holmesville and
Long Lake are also alike in many other physical, chemical and
morphological features, both having developed in coarse
loamy basal till materials. Differentiation is primarily based on
lithology. Long Lake soil parent materials have been derived
from strongly metamorphosed quartzite, slates and some
volcanics. Subsoil consistence is the primary differentiating
criteria between McGee and Holmesville. Holmesville
subsoils have firm to very firm consistence, high bulk density
(greater than 1.75 gm/cm 3) and voids consisting predominantly
of micro pores. McGee subsoils are friable (to slightly firm),
lower in bulk density (usually less than 1.60 gm/cm 3) and have
a higher proportion of macro pores. Holmesville soils have
also been mapped in association with Boston Brook, Caribou,
Carleton, Jacquet River and Thibault soils.
Figure 28. Well drained Holmesville soil profile, cultivated.
Soil development varies from 35 to 65 cm in thickness. The
common horizon sequence on well drained sites is LFH, Ae,
Bhf, Bf, BC and C. O horizons may occur under coniferous
forests where mosses dominate the ground vegetation. The
organic layer is 2 to 10 cm thick, becoming more
humified with depth. It overlies a thin (5 to 10 cm), white,
ashy coloured Ae horizon which breaks abruptly into the B
horizon. The upper strong brown to dark reddish brown Bhf
horizon varies from 2 to 5 cm in thickness. It merges with the
brown to yellowish brown Bf horizon which gradually grades
into the oxidized olive to grayish brown parent material.
Morphological appearance may be deceptive. Significant
amounts of translocated iron and aluminum are often present
in horizons that display little colour change from the parent
material. At 35 to 45 cm the podzolic B horizon grades into a
BC horizon which grades into the unaltered parent material or
C horizon between 35 and 65 cm from the mineral soil surface.
Imperfectly drained soils have similar profile horizons but are
modified by periodic saturation. They are mottled in the B and
C horizons, especially a thin zone immediately above the
compact subsoil where water is perched. The Ae horizon is
often irregular or broken because of tree uprooting due to
windthrow. Poorly to very poorly drained horizon sequences
Excluding problems due to wetness in imperfectly and poorly
drained locations, the dominant features affecting agricultural
land use are related to topography (excessive slope), coarse
fragment content (both surface and profile) and the presence of
a subsoil restricting layer which impedes root penetration and
water percolation. Medium inherent fertility means that
Holmesville are productive forest soils suited to a wide range
of tree species. Holmesville are typical of soil development in
New Brunswick and have been selected as the provincial soil
(Fig. 29).
Figure 29. P rovincial soil
badge. The Holme sville soil
was proclaimed the New
Brunswick provincial soil on
February 13, 1997.
57
Summary of general characteristics of the Holmesville Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: HM
: Chaleur Uplands, Notre Dame Mountains,
N. B. Highlands
: 300-600 m
: 72,592 ha
: 2.60%
: Mineral
: Glacial till, compact
: 1-3 m
: Olive to olive brown
: Coarse loamy
: Quartz and sandstone with miscellaneous
argillite, slate and schist
: Medium
: Rolling and undulating to hilly or sloping
(2-100%)
: Well to moderately well
: Orthic Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 50
50 - 100+
Texture Class
Loam - sandy loam
Loam - sandy loam
% Sand
50
50
% Silt
35
35
% Clay
15
15
% Coarse
Fragments
15 subangular G/C
25 subangular G/C
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.10
1.75
Ksat (cm/hr)
2.5 - 10
0.1 - 1.0
AWHC (cm/cm)
0.20 - 0.25
< 0.15
Interval Association
The Interval association consists of soils that have developed
in acid to neutral, coarse loamy to sandy alluvial sediments of
variable thickness. Alluvium is deposited during relatively
recent geologic time by running water (rivers, streams, etc.) as
sorted or semi-sorted clays, silts, sands and gravels in stream
beds and flood plains. It is derived from the till and bedrock
that underlies its upstream area of origin. The size of particles
carried by the water is among other factors determined by
stream flow velocities and currents. Settling occurs where
stream velocity is decreased. Depositions are thus varied
within the profile (layered) as well as from site to site. Interval
sediments are mostly silts and fine sands, although some
coarser-textured materials are found immediately adjacent to
the channel. They occur as narrow flood plains and terraces
along most stream courses. Small tracts of Interval soil are
scattered throughout the study area at elevations ranging from
sea level to 700 m. However, at the exploratory level of
mapping it is not possible to identify these as individual units.
They are considered as predictable inclusions within other
related map units. The only areas of significant size are found
along the Nashwaak, Keswick and Southwest Miramichi
Rivers where river channel meandering has resulted in flood
plains of up to 1 km in width (Fig. 30). These are within the
Lowlands and Central Highlands physiographic regions. In
total, Interval soils account for 4,871 ha, or 0.17% of the map
area.
Figure 30. Location of mapped Interval soils.
Interval alluvial terraces, flood plains and stream bottoms have
flat to very gently undulating surface expressions with
generally less than 2% slope (Fig. 31). They are located only
slightly above mean annual river elevation. Alluviation is an
ongoing process. Increments of soil are added during flooding.
Depending upon site location this may be an annual event or
may only occur under extreme conditions (ie. once in every 10
or 20 year flood). Because of this gradual buildup or
accumulation of sediments, most Interval soils are rich in
organic matter. Plant roots and surface litter are constantly
being buried by the addition of new sediments (Fig. 32).
Floodwaters are also rich in organic matter. The natural
vegetation on these valley floor locations is distinctly different
from that associated with adjacent uplands. They are
dominated by nutrient demanding and/or water tolerant
deciduous tree species such as elm, ash, red maple, willow and
alder and various native grasses and herbaceous plants.
The Interval association is dominated by imperfectly drained
Gleyed Regosols and Gleyed Cumulic Regosols. Soil
horizonation is too weakly expressed to meet the requirements
of any order other than the Regosolic Order because of the
youthfulness of the material. These are immature soils. They
have little or no soil horizon development. The common
horizon sequence consists of an LF and thin (less than 10 cm
58
thick) Ah over a Cgj. A B horizon less than 5 cm thick may
underlie the Ah. Sites with only intermittent flooding and
deposition of material have buried Ah horizons resulting in
profile horizon sequences of LF, Ah, Cgj, Ahb, Cgj, Ahb, Cgj
etc. Well to moderately well drained Interval soils are
classified as orthic subgroups of their imperfectly drained
counterparts. Most of these profiles still have some faint
orange mottling. Poorly and very poorly drained associates are
Rego Gleysols and Rego Humic Gleysols with common
horizon sequences of LFH or O, Cg; and LFH or O, Ah, Cg;
respectively. Buried horizons may also occur. All catena
members are subjected to flooding. The severity of flooding
varies with site position. During the spring floods the soils are
usually saturated with water or entirely submerged. As river
levels recede, surplus moisture seeps through the profile.
Where water is trapped in enclosed depressional areas the
drying out period is extended to several weeks. Interval soils
are usually readily permeable within the profile (saturated
hydraulic conductivity of greater than 2.5 cm/hr). Underlying
substrata of both coarse (sand and gravel) and fine (clay)
materials may impede water movement. The available water
holding capacity averages 0.20 to 0.30 cm/cm for the entire
depth of the profile. Imperfectly drained soils are supplied
with water from numerous sources: precipitation, seepage from
adjacent uplands, and groundwater flow. W ell to moderately
well drained sites occupy slightly elevated positions and are
not effected by subsurface and groundwater flow to the same
extent as imperfectly drained sites. Poorly to very poorly
drained sites are the result of high groundwater tables and
inflow of seepage waters. They are found in low-lying
depressions and are subjected to ponding after heavy rainfall
or whenever river levels rise.
with each successive deposition during flooding. Many of the
sediments consist of nutrient rich materials eroded from upland
soils. Texture and organic matter contents are also conducive
to nutrient retention. Soil reaction ranges from pH(H 2O) 5.0
to 6.5. Most variation is between profiles. The parent material
colour is olive to yellowish brown in well to moderately well
drained soils. Thin, irregularly spaced layers of dark coloured,
buried Ah horizon may occur. The surface Ah is dark gray to
dark brown. Gray shades dominate poorly to very poorly
drained sites. The soil profile is weak to moderate, medium
granular to fine subangular blocky and friable to very friable
throughout. No compacted or otherwise root restricting layers
exist.
Figure 32. Imperfectly drained Interval soil profile.
Figure 31. Interval soil association landscape.
The Interval textural profile consists of a relatively uniform silt
loam to fine sandy loam or fine loamy sand throughout (Fig.
32). The majority of soil particles fall within the silt to fine
sand diameter range, 0.002 to 0.25 mm. Stratification is
common in the lower profile. Substrate may be quite variable
(clays to gravels) depending upon past stream conditions.
Interval sediments are free of coarse fragments and surface
stones. They are high in natural fertility, probably the most
fertile soils of the region. The fertility is renewed or enhanced
Interval soils are associated with other fluvial soils that occupy
similar geographic positions. They have been mapped with
Gagetown, Grand Falls and Riverbank soils. The Gagetown
and Grand Falls associations are sandy skeletal (ie. gravels)
and the Riverbank association is sandy. All three have well
developed horizonation.
Interval soils are readily
distinguished by their lack of soil development and silty
texture.
Well to moderately well drained Interval soils are particularly
suited to agriculture. They are stone free and friable
throughout, making them easy to work. Available moisture
59
storage capacity is high and they retain nutrients well. Surface
conditions are level to gently undulating. Their chief
limitations are that they are subject to flooding and that their
scattered distribution and small extent make them
economically unimportant from a regional perspective.
Flooding and subsequent saturation delays planting until late
in the spring. Poorly drained areas are difficult to drain
because of their low-lying locations with groundwater levels
near the surface. Development of many Interval soils is
possible on a field by field basis, but under other circumstances
they require community efforts for such projects as dykes and
main drains. From a wood production point of view, Interval
soils are really of little significance, other than that they
occupy riparian zones that are protected. However, it is this
riparian zone nature that makes Interval soils extremely
important in terms of surface water quality protection and
wildlife habitat. Interval soil material is often treated as an
extractable commodity. It is "mined" and sold as topsoil for
lawns, gardens and other uses.
Jacquet River Association
The Jacquet River association consists of soils that have
developed in moderately thin (mostly less than 2 m) deposits
of acidic, coarse loamy non-compact morainal till derived from
mixed rhyolite and trachytes with some basalt and
miscellaneous slates and greywackes. It occurs scattered
across the New Brunsw ick Central Highlands physiographic
region. Some Jacquet River soils are also mapped in the
Chaleur Uplands (Fig. 33). Elevations range from 120 to 700
m above sea level. In total these soils occupy approxim ately
69,047 ha or 2.48% of the total map area.
Summary of general characteristics of the Interval Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: IN
: Maritime Plain, N. B. Highlands
: up to 700 m
: 4871 ha
: 0.17%
: Mineral
: Fluvial (alluvium)
: 1-4 m
: Olive to yellowish brown
: Coarse loamy
: Undifferentiated
: High
: Undulating or terraced (0.5-5%)
: Imperfect
: Gleyed Regosols
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 30
30 - 100+
Texture Class
Silt loam - fine
sandy loam
Silt loam - fine sandy
loam
% Sand
30
25
% Silt
55
60
% Clay
15
15
% Coarse
Fragments
0
0
pH (H2 O)
5.5 - 6.0
6.0 - 6.5
BD (g/cm3 )
1.10
1.20
Ksat (cm/hr)
> 2.5
> 2.5
AWHC (cm/cm)
0.20 - 0.30
0.20 - 0.25
Figure 33. Location of mapped Jacquet River soils.
Jacquet River parent material is a non-compact till and as such
has been deposited either as an ablational till or possibly as a
lodgment till that has been reworked by water. Regardless of
origin, it is friable throughout both solum and subsoil.
However, as a result of the overburden, the subsoil does tend
to be somewhat more dense. Because of the relatively thin
nature of these deposits, surface topography is generally a
reflection of the topography of the underlying bedrock. The
exception to this is where Jacquet River is mapped as
hummocky. Here the till is often slightly thicker and tends to
mask the underlying bedrock configuration. Most Jacquet
River landforms consist of a mixture of veneers and blankets
on either undulating and rolling or hilly, ridged and sloping
bedrock formations. Slopes range from 0.5 to 100%. Bedrock
outcrops are common on the more rugged landscapes (hilly,
sloping) that have steeper slopes. Here exposures occupy
anywhere from 2 to 50% of the map unit area. Well drained
Jacquet River soils support mixed softwood-hardwood stands
of balsam fir, black spruce, red spruce, white birch, yellow
birch, and sugar and red maple. Forest cover on poorly drained
sites is comprised of balsam fir, black spruce, cedar, red maple,
tamarack and some yellow birch.
Jacquet River soils are dominated by well drained Orthic
Ferro-Humic Podzols with some Orthic Humo-Ferric Podzols.
60
Climatic conditions in central New Brunswick are conducive
to the development of Ferro-Humic Podzols. Ferro-humic
podzolization is more strongly expressed under the harsher
climates of the central portion of the Highlands.
Mesoenvironmental differences due to the type of vegetation
and thus the type of litter are also important in determining
variation in solum formation within a map unit. Well drained
conditions dominate steeply sloping hilly, ridged and sloping
landscapes. In these landforms poorly and imperfectly drained
conditions are confined to relatively narrow drainage channels.
Most of the hectarage of imperfectly drained Gleyed
Humo-Ferric Podzols and poorly to very poorly drained Orthic
Gleysols and Fera Gleysols occur in areas of undulating
topography. Internal drainage is moderate to rapid (saturated
hydraulic conductivity of 5 to 15 cm/hr) in the solum but
becomes moderate (2 to 3 cm/hr) in the subsoil. Available
water storage capacity ranges from 0.25 to less than 0.15
cm/cm, decreasing with depth from surface to subsoil. Well
drained sites are supplied with water solely via precipitation.
Imperfectly and poorly to very poorly drained areas have
developed because of a combination of topographic position,
lack of gradient, and high groundwater table.
Solum thickness ranges from 35 to 55 cm. On well drained
sites the common horizon sequence is LFH, Ae, Bhf, Bf, BC
and C. The upper horizons, LFH, Ae, and Bhf are all relatively
thin (3 to 12 cm or slightly thicker) but distinct in appearance.
Mineralization and humification processes in the organic layer
are slow. The F horizon dominates over the H horizon. The
light grayish coloured Ae overlies the dark reddish brown
coloured Bhf which in turn changes abruptly to a 10 to 25 cm
thick, yellowish brown coloured Bf horizon. The Bf horizon
grades through a transitional BC horizon into the C horizon.
Bedrock exposures occur in better drained more steeply
sloping sites with truncated profiles. Imperfectly drained
members of the Jacquet River association have a similar
sequence of horizons, but display distinct or prominent
mottling in the subsoil. Gleying becomes more prominent in
level to depressional site positions. Poorly to very poorly
drained Jacquet River soils have profiles consisting of LFH or
O, Aeg, Bg or Bgf, and Cg horizons. The predominance of
coniferous forest vegetation on these sites encourages mosses
and the accumulation of thicker organic layers.
The Jacquet River texture profile consists of a sandy loam to
loam throughout, with 8 to 18% clay content. Weathering
within the solum may result in a slightly finer texture in the
upper profile than in the subsoil , however, this variation is still
within the sandy loam-loam grouping. Profile coarse fragment
content ranges from 20 to 40%, with subangular stones,
cobbles and gravels and even some boulders. Most Jacquet
River land surfaces are moderately to very stony with stones
occupying 2 to 15% of the surface area. Usually these soils are
also moderately to very cobbly with surface coverage similar
to that of the stones. Surface boulders are present but not in
significant quantities. Jacquet River soils are low in natural
fertility. The parent rocks weather slowly and yield relatively
infertile soil material. Both the solum and subsoil are acidic
falling within a pH(H 2O) range of 4.0 to 5.0. The solum is
moderate, fine to medium, granular to subangular blocky
structured and very friable. The parent material is friable to
slightly firm.
Jacquet River soils have been mapped with other till soils Popple Depot, Catamaran, Tetagouche Falls, Thibault and
McGee. Of these, Popple Depot is the most frequent associate.
Popple Depot soils have developed in parent materials of
similar lithology to Jacquet River soils. However, Popple
Depot soils have a compact subsoil. Catamaran soils also have
compact subsoils. Tetagouche Falls, Thibault and McG ee soils
have developed in non-compact ablational till materials as have
Jacquet River soils. They are differentiated on the basis of
coarse fragment lithologies. Tetagouche Falls is most similar,
having igneous rock types, but they are richer-yielding mafic
volcanic rocks. Thibault and McGee soils are derived from
sedimentary and metasedimentary lithologies. Jacquet River
soils are also occasionally mapped with Big Bald Mountain,
Holmesville, Juniper, Nigadoo River and Long Lake soils.
Biological production on Jacquet River soils is affected by low
inherent fertility, surface stoniness, climate, topography and to
a lesser degree wetness. These limitations more severely
handicap agriculture than forestry. Agricultural potential is
marginal. Jacquet River soils should prove adequate to support
moderately productive stands of forest tree species climatically
suited to the region.
Summary of general characteristics of the Jacquet River Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: JR
: N.B. Highlands, Chaleur Uplands
: 120-700 m
: 69,047 ha
: 2.48%
: Mineral
: Glacial till, noncompact
: <2 m
: Yellowish brown
: Coarse loamy
: Rhyolite and trachyte with some basalt,
slate and greywacke
: Low
: Undulating, rolling and hummocky to
ridged, sloping and hilly (2-100%)
: Well
: Orthic Ferro-Humic Podzol and Orthic
Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Loam - sandy loam
Loam - sandy loam
% Sand
45
60
% Silt
40
25
% Clay
15
15
61
% Coarse
Fragments
20 subangular
S/C/G
30 subangular S/C/G
pH (H2 O)
4.5 - 5.0
4.5 - 5.0
BD (g/cm3 )
1.10
1.55
Ksat (cm/hr)
5 - 15
2-3
AWHC (cm/cm)
0.20
< 0.15
Juniper Association
The Juniper association consists of soils that have developed
in thin (less than 1 m) to relatively thick (greater than 5 m)
deposits of acidic, coarse loamy to sandy, frequently skeletal,
noncompact morainal till derived from granite, granodiorite,
diorite, granite gneiss and miscellaneous volcanics. These
soils occur over large blocks of land in the Central Highlands
along the western boundary of the map area from Coldstream
north to Serpentine Lake (Fig.34). Elevations range from 300
to 700 m above sea level. Juniper soils cover approximately
219,273 ha, or 7.87% of the survey area.
different landforms. Thin layers of Juniper till cover broad
expanses. Rampton et. al. (1984) attributed these deposits to
the down wasting of dead ice which was isolated from the
main glacier as it thinned out over areas of high relief.
Associated landforms generally consist of sloping or hilly
veneers or undulating to strongly rolling blankets over
similarly configured bedrock. Slopes range from 3 to 45%.
Rock outcrops are common in elevated crest, upper slope or
summit positions or along incised stream channels. Lithic
phases (less than 1 m to bedrock) may have a component of
residual material. The underlying bedrock is usually Devonian
granite, which is also the main constituent of the Juniper till
parent material. Glacial ice has also displaced some of these
sediments to the southeast where the underlying bedrocks are
Silurian or Ordovician argillaceous sedimentary rock types.
Thicker deposits of Juniper soil (some exceeding 10 m) occur
in valley bottoms where glacial ice was thicker and supplied
more debris during melting. Associated landforms are usually
hummocky with short irregular slopes of 5 to 15%, but some
areas may be undulating to rolling in surface expression. These
units are characterized by numerous randomly oriented
drainage channels, streams, ponds and lakes. All Juniper soils
are stony and usually bouldery (Fig. 35). The valley bottom
deposits are particularly bouldery on the surface with some
units mapped as having boulder pavement where more than
50% of the surface area is occupied by boulders. Well drained
sites support stands of red and black spruce, balsam fir, sugar
and red maple, beech, yellow and white birch and some white
pine. Species segregation occurs on the basis of aspect and
slope position with the more tolerant species occupying the
cooler lower slope and north-facing slope positions. Imperfect
to poorly drained soils have forest vegetation consisting of
balsam fir, black spruce, red maple, cedar, tamarack and alder.
Figure 34. Location of mapped Juniper soils.
The soils of the Juniper association have developed on
ablational till materials. These ablational tills have resulted
from the down wasting of glacial ice that was rich in debris.
Juniper sediments are usually more stony, less compact and
coarser textured than surrounding lodgment till. The materials
accumulated in place as the ice melted. No compacting forces
were involved in their deposition. Interstitial fines were
flushed from the matrix by running water resulting in coarser
textures and accentuating the stone content. Periglacial frost
action also concentrated stones on the surface. Ice-contact well
to poorly sorted deposits such as kames and eskers are
common inclusions. Juniper soils occupy a number of
Figure 35. Juniper soil association landscape and surface
stones/boulders.
Juniper soils have excellent internal drainage. The parent
material is open and porous with 30 to 40% total pore space,
of which approximately one third are macro pores that permit
a moderate to moderately rapid (2.5 to 10 cm/hr) saturated
hydraulic conductivity. Available water storage capacity is
62
0.10 to 0.20 cm/cm in the solum but is always less than 0.15
cm/cm and commonly less than 0.10 cm/cm in the subsoil.
Better water retention capabilities in the solum are due to
increased content of colloidal materials, ie. clays and fine silts
due to weathering, and humus as a result of decaying plant
debris. Upland Juniper soils are dominated by well drained
Orthic Humo-Ferric Podzols. A thin Bhf horizon is usually
present and in some cases is sufficiently developed (greater
than 10 cm thick) to classify the profile as an Orthic
Ferro-Humic Podzol. On well drained sites precipitation is the
sole source of water. Excess water flows downward through
the underlying pervious subsoil and out of the control section.
In lithic phases lateral subsurface flow may occur for short
durations as water moves down slope along the bedrock
contact. Imperfectly and poorly to very poorly drained sites
are usually found in valley bottom deposits. Imperfectly
drained associates are Gleyed H umo-Ferric Podzols. Poorly to
very poorly drained associates are Orthic Gleysols, Fera
Gleysols or Othic Humic Gleysols. Groundwater flow is the
major water source. Precipitation and subsurface flow are less
important. Poorly to very poorly drained sites are confined to
depressions, drainage channels and other low-lying areas. In
hummocky topography there is often a sequence of well
drained knolls and poorly drained depressions. Imperfectly
drained conditions occur on the periphery of depressions, in
lower slope positions and locally where hillslope seepage is fed
by springs.
Profile development averages 40 to 55 cm in depth (Fig.36).
The common horizon sequence in well drained profiles is LFH
or O, Ae, Bhf, Bf, BC and C. Moss dominated O horizons
usually occur in sites under coniferous forest cover. Mixed
wood conditions promote development of a thinner LFH
horizon sequence. The organic layer varies from 5 to 10 cm in
thickness but may exceed 15 cm in localized areas, especially
where the organic debris is acidic softwood and moss litter.
The mineral soil profile consists of a leached ashy coloured Ae
horizon of 5 to 15 cm over a thin (less than 5 cm thick) dark
reddish brown coloured Bhf. The underlying Bf horizon is
strong brown to yellowish brown. It becomes progressively
paler with depth grading through the BC into the light olive
brown C horizon. Imperfectly drained soils have a similar
horizon sequence but are less pronounced in appearance and
distinctly mottled. As drainage conditions worsen the Bfgj
horizon becomes less distinct and the total solum thickness is
reduced. Poorly to very poorly drained sites often have peaty
phases with 15 to 40 cm of organic debris, usually from
mosses, on the mineral soil surface. Horizon sequences consist
of LFH or O, Ah and/or Aeg, Bg or Bgf, and Cg. The very
dark brown or black coloured Ah horizon is usually thin but
under some conditions may exceed 10 cm in thickness. A dull
grayish leached Aeg horizon 5 to 15 cm thick overlies the B
horizon, which is commonly highly mottled with more than
half of the soil material occurring as prominent iron mottles of
high chroma. Beneath this is the drab coloured parent
material. The Juniper textural profile consists of a sandy loam
to loam over a sandy loam to loamy sand subsoil. The acidic
granitic rock fragments weather to a coarse textured material.
Figure 36. Well drained Juniper soil profile.
However, silt plus clay content in the upper profile is
considerably greater than in the subsoil because of ongoing
physical and chemical weathering processes. Poorly drained
depressional sites also have inwashed silts and clays from
adjacent uplands and so their surface soil textures are often
significantly finer than their subsoil texture. Clay content
averages less than 15% throughout most profiles. The silt:sand
ratio decreases with depth. Rampton et. al. (1984) considered
that much of the weathering of these granites, which make up
the Juniper Association parent material, was initiated before
the last glaciation, as found in the Big Bald Mountain soils.
The profile coarse fragment content ranges from 20 to in
excess of 50%. Angular to subrounded cobbles and stones
dominate but coarse fragments of all sizes, gravels to boulders,
are present. The Juniper association is very stony to
excessively stony with 10 to 50% of the surface being
occupied by stone-sized coarse fragments. As previously
mentioned, some areas also have boulder concentrations on the
surface, with fragments ranging from 1 m to more than 4 m in
size. Juniper soils are low in natural fertility and acidic, with
pH(H 2O) of 5.5 or less throughout the profile. The parent
rocks are slow to weather and yield infertile soils. The solum
is usually weak to moderate, medium to fine, granular or
subangular blocky and very friable to friable while the subsoil
is weak, fine to medium subangular blocky to structureless and
63
friable. No significant root or water restricting soil layers
occur within the profile. Ortstein, a cemented hardpan
formation, may be present in the B horizon but it is
discontinuous and sporadic in occurrence.
Juniper soils have been mapped in proximity to several soil
associations, but are most closely associated with the
Catamaran and Tuadook soils, which are lithologically similar.
However, both the Catamaran and Tuadook soils have
developed in lodgment till and as such have dense compact
subsoils whereas the Juniper subsoil is friable. The differing
modes of deposition have also resulted in Juniper being coarser
textured and somewhat stonier than the other two. Soils such
as Gagetown, which have developed on glaciofluvial
sediments, are also common in some of the undulating to
hummocky Juniper deposits found in valleys bottoms. In more
steeply sloping landscapes with veneer-thick soil materials,
Juniper is commonly mapped with Big Bald Mountain. Big
Bald Mountain is a residual soil, having developed directly as
a result of the in situ weathering of the granitic bedrock.
Juniper, as a till soil, is a heterogenous mixture of glacial
debris ranging from silts and clays to boulders. Lithologically,
Juniper is are also more diverse with diorites, granodiorites,
granite gneiss, volcanics and miscellaneous sedimentary and
metamorphic coarse fragments in addition to the feldspar rich
granites. Juniper soils are also mapped with Long Lake and
McGee soils along some sedimentary and metasedimentarygranitic bedrock boundaries.
Juniper soils suffer from excessive stoniness and boulderiness,
droughtiness and to some degree rockiness. In many situations
topographic conditions are also detrimental to potential land
uses. While some localized areas may be the exception to the
rule, Juniper soils as a whole have little or no potential for
agricultural use. There soils should remain under forest. Forest
management of these soils should take into account the
droughty nature and low to very low inherent fertility on these
materials, and where soils are shallow to bedrock or
excessively stony on the surface, must consider the rather
delicate nature of the ecosystem.
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Sandy loam - loam
Sandy loam - loamy
sand
% Sand
55
70
% Silt
33
20
% Clay
12
10
% Coarse
Fragments
25 subangular
C/S/G
35 subangular C/S/G
pH (H2 O)
4.5 - 5.0
5.0
BD (g/cm3 )
1.00
1.60
Ksat (cm/hr)
5 - 15
2-3
AWHC (cm/cm)
0.10 - 0.20
< 0.10
Lavillette Association
The Lavillette Association consists of organic soils that have
developed on deep (average thickness greater than 1.6 m),
ombrotrophic domed bogs (Tarnocai 1981). They are mapped
only in the Maritime Plain portion of the survey area (Fig. 37).
Landform conditions vary from nearly level to very gently
rolling, slopes of 2% or less being dominant. Lavillette soils
occupy 26,811 ha or 0.96% of the area.
Summary of general characteristics of the Juniper Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: JU
: N.B. Highlands
: 300-700 m
: 219,273 ha
: 7.87%
: Mineral
: Glacial till, noncompact
: <1 - >5 m
: Yellowish brown to brown
: Coarse loamy to sandy skeletal
: Granite, granodiorite, diorite, granite
gneiss and some volcanics
: Low
: Undulating, rolling and hummocky to
sloping and hilly (2-70%)
: Well
: Orthic Humo-Ferric Podzol
Figure 37. Location of mapped Lavillette soils.
As the name implies, domed bogs are typified by convex
surfaces or domes. As most of the bog surface is raised above
the level of the surrounding terrain it is virtually unaffected by
any nutrients in ground waters from adjacent mineral soils.
Most deposits consist of the following zones: a central dome
zone (also referred to as core); a slope zone with a flark
64
subzone; and a marginal zone (Airphoto Analysis Associates
Consultants Ltd. 1975). The dome or core zone is characterized by depths of as great as 5 to 10 m. The slope zone
borders the dome and extends to the almost-level marginal
zone. A flark subzone occurs within the slope zone,
immediately adjacent to the dome. It is characterized by a
distinctive arrangement of ridges with interspaced flashets that
forms a circular pattern, oriented perpendicular to the direction
of slope. The marginal zone or lagg, composed of relatively
shallow peat materials (usually less than 1 m in thickness),
borders the bog, forming a transition from organic deposit to
mineral soil. Wide lagg areas dissected by small streams are
common. The marginal zones vary from the core and slope
zones in that they are generally influenced to some degree by
the nutrients in seepage waters from the surrounding mineral
soils.
Lavillette deposits are usually void of significant tree cover.
Bog domes and slopes are covered with sphagnum and feather
mosses and ericaceous shrubs, but scattered dwarf black spruce
and larch are common. Lagg areas are generally open and
support sedge species in addition to mosses and shrubs. Dense
stands of stunted black spruce and larch occupy the lagg to
mineral soil transition zones.
Peat stratigraphy usually consists of a surface layer 0.5 to
greater than 4.0 m thick of fibric (weakly decomposed) sphagnum peats overlying a layer 0.3 to 2.0 m thick of mostly mesic
(moderately decomposed) and some humic (well-decomposed)
sedge-sphagnum peats which grade into pure sedge peats. This
material in turn is underlain by a relatively thin, confined,
basal layer of sedimentary peat.
The surface fibric layer is dominated by sphagnum mosses,
readily identifiable as to origin because they are only slightly
decomposed. The remains of shrubby plants are also
commonly found in this layer and may account for as much as
20% by volume. In general this surface layer is composed of
materials that have a brown to dark reddish brown colour, an
extremely acid reaction (pH in H 2O of less than 4.0), low bulk
densities (less than 0.075 g/cm3), moderately rapid to rapid
permeabilities (saturated hydraulic conductivity of greater than
10 cm/hr), and high contents of rubbed fibre with class 1 to
class 4 ratings on the von Post scale of decomposition. The
middle layer is dominated by sedges (Carex spp.) with lesser
amounts of sphagnum mosses. These materials are at an intermediate to advanced stage of decomposition. They have a
brown to dark brown colour, an extremely acid to acid reaction
(pH in H2O of less than 4.0), moderate to high bulk densities
(greater than 0.15 g/cm 3), moderate to very slow permeabilities
(saturated hydraulic conductivity of less than 2 cm/hr), and
moderate to low contents of rubbed fibre with von Post scale
of decomposition class 5 to class 8.
The basal layer of sedimentary peat or ooze is composed of
coprogenous earth, which is aquatic plant debris modified by
aquatic animals. Very few or no plant remains are
recognizable to the naked eye. It usually has a dark brown to
very dark grayish brown colour, an acid reaction (pH in H2O
of 4.5), high bulk density (greater than 0.3 g/cm 3) and ash
content (30%) values, and very slow permeabilities (saturated
hydraulic conductivity of less than 0.1 cm/hr).
Natural drainage varies little with site position on the bog. The
dome, slope and marginal zones are all very poorly drained
(Fig. 38). The water table is at or near the surface throughout
the year. Groundwater in bogs is extremely acid and low in
nutrients, even in lagg areas.
Figure 38. Lavillette soil association landscape.
Lavillette soils are mainly Typic, and some Mesic, Fibrisols on
the dome and slope zones with Terric Mesic or Humic
Fibrisols on the marginal zone. Typic Fibrisols have
dominantly fibric middle and bottom tiers. Some minor layers
of mesic material occur, usually in the deeper portions of the
profile. Where subdominant mesic layers have a total
thickness greater than 25 cm in the m iddle and bottom tiers the
soils are classified as Mesic Fibrisols. Bog margin or lagg
zones have shallow (usually less than 160 cm) thickness of
organic material, consisting of fibric sphagnum peats over
mesic or humic sedge-sphagnum peats. They are classified as
Terric Mesic or Humic Fibrisols.
Lavillette soils are associated with other organic soils as well
as with poorly and very poorly drained members of some
mineral soils. Acadie Siding is an organic associate which
differs from Lavillette soils in that it consists of soils on
less-developed peatland deposits--mostly shallow (less than 1.6
m of organic material) Terric Mesisols (moderately
decomposed) or Humisols (well decomposed). Acadie Siding
soils lack the pronounced circular surface pattern of Lavillette
soils. Very poorly or poorly drained Barrieau-Buctouche, Reece, Richibucto, Stony Brook and Tracadie soils are also
commonly found with Lavillette soils. Mineral soils may have
surface layers of fibric organic material up to 60 cm thick and
still be considered mineral soils. The boundary between
Lavillette organic soils and adjacent mineral soils is, in most
places, abrupt and obvious.
Lavillette soils are considered non-productive woodland. They
have potential agricultural uses for vegetable crop production
but require specialized management practices and equipment.
65
Lavillette soils are often used as sources for peat moss and
related products.
Summary of general characteristics of the Lavillette Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Degree of Decomposition
Botanical Composition
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: LV
: Maritime Plain
: < 150 m
: 26,811 ha
: 0.96%
: Organic
: Domed bog
: >1.6 m over mineral soil
: Brown to dark reddish brown
: Weakly decomposed
: Sphagnum peat
: Very low
: Domed (<1.5%) in an undulating
landscape (<5%)
: Very poor
: Typic Fibrisol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 60
> 60
Von Post rating
1-3
2-4
% Wood
5
5
pH (H2 O)
< 4.0
< 4.0
BD (g/cm3 )
< 0.05
0.08
Ksat (cm/hr)
50
20
AWHC (cm/cm)
0.10
0.10
particle sizes ranging from silts and clays to stones and
boulders. Clast shapes are a function of the parent bedrock.
Coarse fragment content is particularly high where weathered
bedrock has been incorporated into thin veneer deposits. Long
Lake soils are very stony on the surface, with 3 to 15% of the
land area occupied by coarse fragments. In imperfectly and
poorly drained sites frost action frequently concentrates profile
cobbles on the mineral soil surface under the forest floor.
Boulders are common but usually not in sufficient quantities
to warrant designation as a bouldery phase. Long Lake
landforms are dominated by undulating, and rolling surface
expressions with slopes varying from less than 3% to in excess
of 30%. Some hilly, ridged or sloping map units with slopes
of up to 70% also occur. The soils are relatively uniform in
thickness and bedrock outcrops are not all that common.
Those bedrock exposures that do occur are found on
topographic highs and summits or along steeply inclined
drainage channels that are deeply incised into the bedrock.
Bedrock exposures often consist of more resistant strata that
weather at a slower rate than adjacent rock. Well drained soils
of the Long Lake association support forest communities of
black spruce, balsam fir, yellow and white birch, red oak,
white pine, and sugar and red maple. On poorly to very poorly
drained sites the tree vegetation consists of black spruce,
balsam fir, red maple, cedar and some tamarack and yellow
birch.
Long Lake Association
The Long Lake association consists of soils that have
developed in relatively thin (mostly less than 2 m thick)
deposits of acidic, coarse loamy, compact morainal till derived
from slate, siltstone, argillite, schist, quartzite and greywacke.
They occur mostly in the Central Highlands physiographic
region of the study area, and to a lesser extent in the Chaleur
Uplands, at elevations of 300 to 700 m above sea level (Fig.
39). Long Lake soils occupy approximately 262,504 ha, or
9.42% of the map sheet.
The soil parent material has been deposited as ground moraine,
plastered in place under the weight of advancing glacial ice.
Composition strongly reflects the incorporation of local
bedrock formations. Thin surficial mantles of ablational till,
usually McGee material, are common, but their identification
is difficult. The McGee and Long Lake parent materials are
similar in composition and mixing actions during soil
formation have modified the upper soil profile, obliterating
most evidence of multiple till layers.
The till is a
heterogeneous mixture of flat, angular to subangular shaped
Figure 39. Location of mapped Long Lake soils.
Well drained Long Lake soils are mostly Orthic Ferro-Humic
Podzols (Fig. 40) with some Orthic Hum o-Ferric Podzols.
Climatic conditions in central New Brunswick are conducive
to the accumulation of organic matter in the podzolic B
horizon. Most macro and meso environmental conditions are
such that Long Lake soils have enough organic carbon content
to qualify for the Ferro-Humic Podzols great group. The
remaining well drained soils are Humo-Ferric Podzols.
Ferro-humic podzolization is not as strongly expressed along
the eastern periphery of the Long Lake range where the
Central Highlands merge with the Maritime Plain.
Humo-Ferric Podzols dominate the Maritime Plain, which has
66
a slightly milder climate than the Highlands.
Mesoenvironmental differences due to the type of vegetation
and thus the type of litter are also important in determining
variation in solum formation within a map unit. Well drained
conditions dominate steeply sloping hilly and rolling
landscapes. In these landforms poorly and imperfectly drained
conditions are confined to relatively narrow drainage channels.
Significant hectarages of imperfectly drained Long Lake soils
occur as Gleyed Humo-Ferric Podzols in areas of undulating
and gently rolling topography, where they are found in
association with both well drained or poorly drained associates.
Poorly drained soils of the Long Lake association are Orthic
Gleysols. Internal drainage is restricted by a slow ly to
moderately slowly permeable subsoil with an estimated
saturated hydraulic conductivity value of 0.1 to 1.0 cm/hr.
Available water storage capacity ranges from 0.20 to 0.10
cm/cm, decreasing with depth because of reduced total
porosity in the compact subsoil. Well drained sites are
supplied with water solely via precipitation. Downward
movement of excess moisture through the profile is impeded
by the subsoil so some lateral flow occurs for short durations.
Imperfectly and poorly to very poorly drained areas have
developed because of a combination of topographic position,
lack of gradient, subsoil compaction, seepage and high
groundwater table.
Soil development varies from 45 to 60 cm in thickness. The
common horizon sequence on well drained sites is LFH or O,
Ae, Bhf, Bf, BC and C. O horizons are common under
coniferous forests where mosses dominate the ground
vegetation. The organic layer is 5 to 15 cm thick, becoming
more humified with depth. It overlies a thin to moderately
thick (5 to 20 cm), ashy coloured Ae horizon which breaks
abruptly into the B horizon. The upper dark brown to dark
reddish brown Bhf horizon varies from 5 to 20 cm in
thickness. It merges with the strong brown to yellowish brown
Bf horizon which gradually grades into the oxidized olive
brown parent material. Morphological appearance may be
deceptive. Significant amounts of translocated iron and
aluminum are often present in horizons that display little
colour change from the parent material. On the other hand,
organic coatings on coarser textured Bf horizons give the
impression of more organic matter than is actually present.
Imperfectly drained soils have similar arrangements of profile
horizons but are modified because of periodic saturation. They
are mottled in the B and C horizons, especially a thin zone
immediately above the compact subsoil where water is
perched. The Ae horizon is often irregular or broken because
of tree uprooting due to windthrow. An Ahe horizon up to 10
cm thick may be sandwiched between the H and Ae horizons
in imperfectly drained Long Lake soils. Poorly to very poorly
drained horizon sequences lack a podzolic B horizon. They
consist of LFH or O, Aeg, Bg, BCg, and Cg horizons. The
forest duff layer is usually thicker than found in well drained
counterparts. The Long Lake textural profile consists of a
loam or silt loam to sandy loam (8 to 18% clay) throughout,
but the solum is often slightly finer textured (higher in silt and
clay content) than the subsoil. This is most obvious in
imperfectly to poorly drained sites and is considered to be the
result of increased weathering and/or siltation. Profile coarse
fragment content averages 20 to 40%, with a preponderance of
flat, horizontally lying channers, gravels and flagstones. In
lithic phases uplifted fragments of fractured bedrock increase
the percentage of coarse fragments in the lower profile. Long
Lake soils are medium in inherent fertility, but acidic
throughout, with pH(H 2O) values of 4.0 to 5.5. The friable to
very friable, weak to moderate, fine to medium, granular or
subangular blocky solum overlies a firm to very firm, massive,
breaking to medium subangular blocky, subsoil. The subsoil
shatters readily upon extraction.
Figure 40. Well drained Long Lake soil profile.
The Long Lake association is most comm only found with
members of the M cGee association. The two soils have been
derived from materials of similar lithological origin. They are
also alike in many other physical, chemical and morphological
features. Differentiation is primarily made on the basis of
subsoil compaction, and associated characteristics. Long Lake
subsoils have firm to very firm consistence, high bulk density
(greater than 1.75 gm/cm 3) and voids consisting predominantly
of micro pores. McGee subsoils are friable (to slightly firm),
lower in bulk density (usually less than 1.55 gm/cm3) and have
a higher proportion of macro pores. Along transition zones
Long Lake soils have also been mapped in complexes with a
number of other soils: Tetagouche, Jacquet River, Holmesville,
Violette, Popple Depot, Juniper, Reece, Catamaran, and
67
Tuadook soils.
Excluding problems due to wetness in imperfectly and poorly
drained locations, the dominant features affecting land use are
related to topography (excessive slope), coarse fragment
content (both surface and profile) and the presence of a subsoil
restricting layer which impedes root penetration and water
percolation. Long Lake soils are moderately fertile and so
produce respectable stands of most tree species that are
climatically suited.
New Brunswick Highlands, Chaleur Uplands and Notre Dame
Mountains physiographic regions at elevations ranging from
200 to 500 m above sea level (Fig. 41). Maliseet soils cover
approximately 3,332 ha or 0.12% of the map area. They occur
in small, scattered tracts.
Summary of general characteristics of the Long Lake Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: LL
: N.B. Highlands, Chaleur Uplands
: 300-700 m
: 262,504 ha
: 9.42%
: Mineral
: Glacial till, compact
: <2 m
: Olive brown
: Coarse loamy
: Slate, siltstone, agrillite, schist and some
quartzite and greywacke
: Medium
: Rolling and undulating to sloping and
hilly (0.5-45%)
: Well to moderately well
: Orthic Ferro-Humic Podzol and Orthic
Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 50
50 - 100+
Texture Class
Loam
Loam - sandy loam
% Sand
45
50
% Silt
39
38
% Clay
16
12
% Coarse
Fragments
20 flat, subangular
C/G/S
30 flat, subangular
C/G/S
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.10
1.75
Ksat (cm/hr)
2.5 - 10
0.1 - 1.0
AWHC (cm/cm)
0.15 - 0.20
0.10 - 0.15
M aliseet Association
The Maliseet association consists of soils developed in
relatively thick (3 m plus) deposits of acidic, sandy to coarse
loamy fluvial (ancient alluvium) or possibly glaciofluvial
material derived from slate, shale and miscellaneous quartzite
and volcanic rock types. Maliseet materials are underlain at
depth by the regionally prevailing till. They are found in the
Figure 41. Location of mapped Maliseet soils..
Maliseet soil parent materials were deposited as river terraces
and are level to gently undulating with steep slopes between
terraces. As such, they tend to be elongated deposits found in
narrow strips along river and stream courses. Deposition has
been by waters flowing at moderate velocity. Velocity of the
flowing water determined the size of the particles that were
deposited. Suspended particles were deposited when water
turbulence ceased to exceed their settling velocities, a function
of particle diameter, shape and specific gravity, and fluid
density. Most sediments consist of well rounded fine to
medium sand grains with varying amounts of silt. Changes in
stream velocity resulted in layers of varying thickness and
particle size. Some gravel transport and deposition occurring
during periods of faster than norm al streamflow have lead to
the inclusion of the occasional gravelly layer within Maliseet
materials. Maliseet landscapes are variable in that they consist
of terrace surfaces, with horizontal or gently inclined planes (0
to 3% slope) separated by scarp faces (15 to 45% slope).
Maliseet soils support mixed wood stands of balsam fir, black
spruce, white pine, white birch, trembling aspen, white elm and
white ash on the drier well drained sites. Moist sites along
stream bottoms and lower terraces have cedar, black spruce,
tamarack, red maple, white elm, speckled alder and black ash.
The Maliseet association consists of rapidly to well drained
Orthic Humic-Ferric Podzols, imperfectly drained Gleyed
Humo-Ferric Podzols and Gleyed Eluviated Dystric Brunisols,
and poorly to very poorly drained G leyed Eluviated Dystric
Brunisols and Orthic Gleysols and occasionally Rego Hum ic
Gleysols under very poorly drained conditions. On well
drained sites water is supplied only by precipitation. Maliseet
soils have moderate available water storage capacity in the
solum, (0.20 to 25 cm/cm), but it decreases to as little as 0.10
68
cm/cm or less in the subsoil. Finer textures and higher levels
of organic matter content aid water retention in the upper
solum. Imperfectly and poorly drained sites are mostly
restricted to lower terraces along valley floors. In these sites,
groundwater presence is the determining factor in soil
drainage. Impeded drainage may also occur on some upper
terraces at the base of the transition slope from the above
terrace. Subsoil permeability varies from 1.0 cm/hr to more
than 10 cm/hr. This wide range is due to parent material
stratification. The C horizon is made up of layers of sandy
loam, loamy sand, fine gravel and silt. Most layers are
moderately rapidly permeable.
Soil development in Maliseet materials ranges from 30 to 50
cm in thickness, but is typically less than 40 cm. Moderately
well to imperfectly drained sites have the deepest solum
development. These sites have more suitable moisture regimes
for biological production and soil formation. The horizon
sequence in well to rapidly drained soils is typically: LFH, Ae,
Bhf, Bf, BC and C. The Bhf horizon is thin and poorly
developed. Imperfectly drained profiles have LFH, Ae, Bfgj,
BCgj and Cg horizons. Poorly to very poorly drained profiles
have a number of different possible profiles: LFH, Ae, Bmgj,
BCg and Cg; or LFH or O, Aeg, Bg and Cg; or, very thin LFH
or O, Ahg, BCg and Cg. Weathering has resulted in the
surface soils having more fines (silt and clay) than is found in
the subsoil. Windthrow , frost action and biological activity
have obliterated any stratification that may have originally
been present in the solum. The Maliseet texture profile grades
from a fine sandy loam to sandy loam solum into a loamy sand
to sandy loam subsoil. Clay content only exceeds 10% in the
upper solum. Coarse fragments are few. Where they do occur
they are usually fine gravels of slate, shale and quartzite.
Maliseet soils are medium to low in natural fertility and acidic
throughout the profile, with a range in pH (H 2O) of 4.0 to 5.5.
The exception to this is found in some poorly to very poorly
drained sites in which the subsoil pH is elevated to 6.5 or even
higher as a result of inwashing of carbonates from surrounding
calcareous soil parent materials and/or bedrocks. The parent
material colour is olive gray. In well drained sites the solum
consists of a thin LFH layer overlying a leached light gray
coloured Ae horizon. The underlying B horizon consists of a
thin (less than 5 cm thick) reddish brown Bhf horizon over a
dark to yellowish brown Bf horizon that becomes
progressively yellower in hue with depth. Imperfectly and
poorly drained soils have iron (Fe) mottling or gleyed colours
of low chroma, or both. The subsoils are loose and single
grain or structureless but stratified. The A horizon is friable to
very friable, very weak, fine platy. Most B horizons are very
friable, weak to moderate, fine granular. Very poorly drained
profiles may be restricted to a moderately thick (15 to 20 cm)
Ah horizon over a thin transitional BC horizon that grades into
the subsoil at 30 to 40 cm depth.
Maliseet soils are usually associated with other soils developed
in fluvial sediments, such as Grand Falls and Muniac.
Maliseet, Grand Falls and Muniac are lithologically similar,
but both Grand Falls and Muniac are sandy skeletal, i.e.,
gravelly or very gravelly in the parent material. They are
separated on percent coarse fragment content. Grand Falls and
Muniac soils usually have 50 to 70% gravels in the subsoil
while Maliseet soils have less than 20% gravels and usually
less than 5%. Interval soils occupy similar soil landscapes to
Maliseet soils, but Interval soils are distinctly finer-textured
than Maliseet soils. Interval soils are also restricted in
occurrence to flood plains.
Maliseet soils are productive for both agricultural and forestry
crops. They respond to fertilizer treatments and the solum
texture is generally fine enough to have adequate waterholding capacity. Medium natural fertility is an asset in
forestry.
Summary of general characteristics of the Maliseet Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: MA
: Chaleur Uplands
: 200 to 500 m
: 3,332 ha
: 0.12%
: Mineral
: Fluvial (ancient alluvium)
:>3m
: Olive brown to yellowish brown
: Sandy to coarse loamy
: Slate, shale and miscellaneous quartz and
volcanics
: Medium
: Undulating or terraced (2-15%)
: Well
: Orthic Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 35
35 - 100+
Texture Class
Fine sandy loam
Fine sandy loam fine loamy sand
% Sand
60
80
% Silt
25
10
% Clay
15
10
% Coarse
Fragments
5 rounded G
5 rounded G
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.00
1.45
Ksat (cm/hr)
5 - 10
1 - 10
AWHC (cm/cm)
0.20 - 0.25
0.10
M cGee Association
The McGee association consists of soils that have developed
in relatively thin (most less than 2 m thick) deposits of acidic,
coarse loamy to loamy skeletal, noncompact, "water-
69
reworked" morainal till derived from slates, argillite, schist,
greywacke and quartzite. McGee soils are found throughout
the Central Highlands, Chaleur Uplands and Notre Dame
Mountains physiographic regions of the study area at
elevations ranging from 300 to 800 m above sea level (Fig.
42). They occupy large, extensive areas totalling some
417,254 ha which represents 14.97% of the map area.
Figure 42. Location of mapped McGee soils.
The origin or mode of deposition of McG ee parent material is
variable. It consists of morainal till sediments, probably both
ablational and lodgment debris, that has been reworked to
varying degrees by either water, periglacial action or colluvial
action, alone or in combination. As the glaciers ablated,
materials within the ice were deposited. Melt waters also
modified previously deposited glacial sediments of lodgment
(basal) till, removing fines, weakly stratifying some surficial
materials, etc. Periglacial environments on the margins of
waning glacial ice sheets were characterised by cold
temperature climates in which frost action was an important
factor. Original parent material conditions were altered by
frost heaving due to ice lense formation caused by freezing.
Deep frost penetration helped to loosen compacted basal till
sediments. Colluvial action, gravity induced movement on
steeply sloping surfaces, is an on-going process that has further
modified some McGee materials. These colluvial materials are
associated with site positions at the base of steep slopes or
cliffs. They consist of sediment that strongly resembles the till
parent material but may be poorly sorted or stratified. McGee
materials occupy m ostly rolling to hilly landscapes with gentle
to very strongly sloping gradients of 5 to 45%. Most deposits
are either veneers or blankets, ie. less than 2 m thick, and so
conform to the configuration of the underlying bedrock.
Thicker sediments usually occur on lower slope positions.
McGee soils are also found on steeply sloping banks of
streams that are deeply incised into the bedrock. Here, some
slopes may be in excess of 70%. Lessor areas of McGee soils
occur on undulating, ridged and hummocky landscapes.
Shallowness to bedrock and bedrock exposures are an inherent
characteristic of McGee map units. On undulating to rolling
landscapes, however, exposures usually cover less than 2% of
the surface and as such are considered as nonrocky.
Significant occurrences (2 to 25% surface area) of bedrock
exposures are confined to sloping, hilly and ridged conditions.
Well drained sites support stands of white and yellow birch,
sugar maple, black and red spruce, and balsam fir. Poorly to
very poorly drained sites are found in low-lying depressions
and drainage channels. Natural vegetation consists of water
tolerant and frost hardy species such as black spruce, balsam
fir, tamarack, cedar, red maple and alder.
The McGee association is dominated by well drained Orthic
Ferro-Humic Podzols (Fig. 43) and Orthic Hum o-Ferric
Podzols. Podzolization is strongly expressed. The colder
climate of central New Brunswick results in greater effective
precipitation and hence the formation of a podzolic B horizon
with appreciable amounts of organic matter accumulation. In
some locations the organic carbon content of McGee B
horizons straddles the taxa boundary. Where organic carbon
levels in 10 cm or more of the B horizon meet the requirements
of a Bhf (greater than 5% organic C), the profile is classified
as a Ferro-Humic Podzol, otherwise it is a Humo-Ferric
Podzol. It was not possible to separate these two great groups
into homogeneous units at the level of mapping undertaken in
this project. Imperfectly drained McGee soils are classified as
Gleyed Humo-Ferric Podzols. Poorly to very poorly drained
members are Orthic or Rego Gleysols. Where mapped,
imperfectly and poorly to very poorly drained McGee soils are
usually subdominant components of units dominated by well
drained McGee soils. They also occur as predictable
inclusions in units mapped solely as well drained. Well
drained sites occur on crest to middle or lower slope positions,
depending upon topographic conditions. Where slopes are
steep, the transition from well drained to poorly or very poorly
drained is quite abrupt. Imperfectly drained areas are usually
associated with rolling to undulating landscapes. Poorly to
very poorly drained sites occupy drainage ways. McG ee soils
have good internal drainage. The subsoil is pervious, and
based on pore size distribution, should be moderate to
moderately slow in permeability (1.0 to 5 cm/hr saturated
hydraulic conductivity). Available water storage capacity is
0.20 to less than 0.10 cm/cm, decreasing with depth.
Precipitation is the sole source of water on well drained sites.
Excess water readily flows downward through the profile and
into the underlying bedrock, which is usually weathered and
fractured on the surface. However, under periods of excessive
moisture supply, some lateral flow may occur along the
bedrock surface. Excess water in poorly drained sites is the
result of high groundwater levels and inflow of seepage water
from adjacent uplands. Soil drainage status is largely a
function of topographic position.
Profile development averages 40 to 60 cm in depth. The
common horizon sequence in well drained profiles is: LFH or
O, Ae, Bhf, Bf, BC and C. Under mixed woods the forest
floor layer is LFH, but under softwood stands, O horizons of
peaty mors develop. The grayish coloured Ae horizon is often
10 to 20 cm thick, tonguing into the brown to dark reddish
brown upper B horizon (Bhf). The Bhf horizon varies from 2
to 15 cm in thickness. The underlying Bf is a dark brown to
70
mottles occur. The Ah horizon is usually thin or absent. Under
very poorly drained conditions there may be no horizonation
apart from evidence of gleying. The McGee textural profile
varies from a loam or sandy loam to a silt loam. Texture may
vary considerably from profile to profile as well as within the
profile. Some profiles are relatively well sorted, others are not.
One peculiarity in the McGee texture profile is the high silt
content in the Ae horizon compared to underling horizons.
Percentage silt in the Ae may be more than twice that of the B
and C horizons. This is attributed to a combination of
weathering of coarser sized particles and differential
movement of soil constituents within the profile. Frost action
has caused disintegration of rock fragments into silt sized
particles and percolating waters have translocated some of the
clay fraction into the B horizon. The profile coarse fragment
content averages 20 to 50% flat to subangular, gravels, cobbles
and stones. Veneer phases may exceed this range. The coarse
fragments are derived mainly from hard, tough, firmly
indurated rock types such as slate, greywacke and quartzite.
Some deposits, however, contain large quantities of weathered
chloride-mica schist and argillite. Most landscapes are very
stony with 3 to 15% of the surface area occupied by stones 1
to 2 m apart. Boulders, fragments greater than 1 m in
diameter, are common. McGee soils are medium to low in
natural fertility and acidic, pH(H 2O) 4.0 to 5.5. No root or
water restricting soil layers occur within the profile. The
solum is mostly moderate, medium granular and friable to very
friable. The subsoil is weak, fine to medium subangular
blocky and friable providing a deep porous well aerated
potential rooting zone. Ortstein, cementation in the Bf or Bhf
horizon, may occur, but only sporadically. It has little effect
on land use.
Figure 43. Well drained McGee soil profile.
dark yellowish brown, becoming progressively yellower as it
grades into the BC. The McGee parent material is usually
olive brown. Colouration is often deceptive, indicating less
soil development than is confirmed by chemical analysis.
Other than being mottled and having thin (less than 5 cm thick)
Bhf formation, imperfectly drained sites are similar in
appearance to their well drained counterparts. An Ahe horizon
up to 5 cm thick may also be sandwiched between the H and
Ae horizons in imperfectly drained McGee soils. Poorly
drained profile sequences usually consist of O, (Ah), Aeg, Bg
and Cg. The colours are dull with low chromas and prominent
McGee soils have been mapped in complex units with
numerous other soils including Long Lake, Thibault,
Holmesville, Catamaran, Jacquet River, Juniper, Popple Depot,
Tetagouche, Tetagouche Falls and Violette, however, they are
most commonly associated with the first three soil
associations. Long Lake is texturally and lithologically very
similar to McGee. The two soils are differentiated on the basis
of subsoil compaction. Long Lake has a firm, dense compact
subsoil. McGee subsoil is noncompact. Thibault is also similar
in physical characteristics to McGee. One of the major
differences that separates these two soil associations is soil
reaction. Thibault soil parent materials are neutral. They have
been derived from weakly calcareous shales, slate, quartzite,
argillite and sandstone. Like Long Lake, Holmesville soils are
developed on lodgment till parent material and have compact
subsoils.
Major soil and landscape features affecting land use of McGee
soils include excessive stoniness, shallowness to bedrock and
slope steepness. These limitations place significant restrictions
on potential agricultural usage. Excluding poorly drained
conditions, McGee soils should be good to fair in terms of
forest production of suitable species such as white and black
spruce, balsam fir, jack pine, birch and maple.
71
Summary of general characteristics of the McGee Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: MG
: N.B. Highlands, Chaleur Uplands, Notre
Dame Mountains
: 300-800 m
: 417,254 ha
: 14.97%
: Mineral
: Glacial till, noncompact
: <2 m
: Olive to olive brown
: Coarse loamy
: Slate, agrillite, schist, greywacke and
quartzite
: Medium
: Undulating and rolling to sloping and
hilly (2-100%)
: Well
: Orthic Ferro-Humic Podzol and Orthic
Humo-Ferric Podzol
level. Esker deposits are long, narrow, low, sinuous, ridges or
mounds. Most sediments consists of well stratified sands and
gravels with some cobbles. The soil and rock fragments are
smooth and rounded. The layers or strata vary in thickness and
composition, a reflection of the changing environmental
conditions during w hich they were deposited. Muniac soils are
nonstony.
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 50
50 - 100+
Texture Class
Loam (sandy loam
or silt loam)
Sandy loam
% Sand
40
60
Figure 44. Location of mapped Muniac soils.
% Silt
45
25
% Clay
15
15
% Coarse
Fragments
25 flat, subangular
G/C/S
35 flat, subangular
G/C/S
The major forest species on well to rapidly drained sites are
black spruce, balsam fir, white birch, white pine, trembling
aspen, red maple and yellow birch. Poorly to very poorly
drained lower slopes and depressions support communities of
cedar, tamarack, black spruce, willow and balsam fir.
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm )
1.10
1.55
Ksat (cm/hr)
> 10
> 10
AWHC (cm/cm)
0.15 - 0.20
0.10
3
M uniac Association
The Muniac Association consists of soils developed in thick
deposits (often in excess of 20 m) of neutral, sandy skeletal,
glaciofluvial material with calcareous to weakly calcareous
slate, shale, quartzite and sandstone coarse fragments. The
glaciofluvial material is underlain by glacial till or bedrock.
These soils occur in small tracts scattered throughout the
Chaleur Uplands and New Brunswick Highlands regions of the
survey area (Fig. 44). Muniac association soils cover
approximately 2,450 ha or 0.09% of the map area.
Muniac soils usually occur in old river terraces or as eskers.
The topography varies from undulating to terraced, with
horizontal or gently inclined terraces separated by steeply
sloping scarp faces. The terraces are long, narrow surfaces
running parallel to streams and rivers, marking a former water
The Muniac Association is dominated by well to rapidly
drained Orthic Humo-Ferric Podzols. Gleyed Humo-Ferric
Podzols occupy imperfectly drained sites, and Gleyed
Humo-Ferric Podzols, Gleyed Eluviated Dystric Brunisols,
Orthic Gleysols and Rego Humic Gleysols occur on poorly to
very poorly drained sites. The subsoil parent material is
rapidly pervious (usually greater than 10 cm/hr). Excess
precipitation readily flows downward through the profile.
Upper solum water holding capacities are enhanced by their
finer texture (gravelly loam to gravelly sandy loam) and the
presence of organic matter. Here, water storage capacities may
reach 0.20 cm/cm. The available water storage capacity
decreases with depth. Muniac soils have low available water
storage capacity within the subsoil, averaging 0.10 cm/cm or
less. Precipitation is the sole source of water on well drained
sites. Off-drainage (imperfect, poor and very poor drainage)
is the result of high ground water tables and groundwater flow.
Most Muniac soils are either dry (well to excessively drained)
or wet (poorly to very poorly drained). Areas of imperfect
drainage are restricted to subdominant components of map
units of the above mentioned drainage categories.
The depth of the solum of Muniac Association soils varies
from 25 to 50 cm. Thickest solum development is found on
well to imperfectly drained sites. Sites with moisture regimes
72
at the extremes, either excessively dry or excessively wet, tend
to have shallower solum development. The common horizon
sequence in well to rapidly drained soils is: LFH, Ae, Bf, BC
and C. At higher elevations where there is greater effective
precipitation, increased accumulation of organic matter in the
upper podzolic B horizon leads to the formation of a thin Bhf
horizon. Imperfectly drained profiles have: LFH, Ae, Bfgj,
BCgj and Cg horizons, indicating the presence of distinct or
prominent mottles. Poorly to very poorly drained soils have
horizons sequences of: LFH, Ae, Bmgj or Bfjgj and Cg; LFH
or O, Aeg, Bg and Cg; or LFH, Ah and Cg as drainage gets
progressively worse. The stratification so characteristic of the
soil parent material is not present in the solum. Mixing actions
of soil organisms, frost churning and tree uprooting
(windthrow) have altered the upper soil profile, obliterating
any of its original stratification. The M uniac texture profile
usually grades from a gravelly sandy loam solum into a
gravelly to very gravelly loamy sand to sandy loam subsoil. In
poorly drained sites inwashed fines (siltation) may make the
surface material slightly heavier. Coarse fragment content
increases with depth to in excess of 70% in some strata (layers)
in the parent material. Percent coarse fragment content varies
from one stratum to another. Most coarse fragments are round
edged, flat, elongated gravels or channers, 0.2 to 15 cm long,
having been derived from highly fractured calcareous slate,
shale, quartzite, sandstone and related lithologies. Muniac
soils are medium in natural fertility. Most profiles are acidic
in the upper solum, increasing in pH with depth. Free
carbonates are present at varying depths below one metre.
Calcium is a highly mobile base ie. it is readily leached.
During podzolization, intense leaching by strong organic acids
has removed most of the calcium from the soil profile, thus
resulting in an acidic solum. The bases dissolved by these
percolating acids are removed in solution into the groundwater.
Subsequently some bases are redeposited in poorly drained
areas by calcium carbonate enriched groundwater. In well
drained soils the parent material colour is olive brown to light
olive brown. The solum consists of a relatively thin (1 to 5
cm) LFH horizon over a light brownish gray Ae which is
underlain by a dark brown to strong brown coloured Bf.
Imperfectly drained soils have iron mottling of high chroma
and value in the lower B and C horizons. Poorly drained soils
are characterized by gray colours and prominent mottling
indicative of intense reducing conditions. Matrix chromas are
generally 2 or less. The subsoils are loose and single grain,
while the sola are very friable to friable, with weak, fine to
medium, granular structure in the B horizon and weak to
moderate, fine, platy structure in the A horizon.
Muniac soils are found in areas dominated by soils formed
from calcareous shale, slate, quartzite and sandstone, such as
the Thibault, Caribou and Carleton associations. However,
these are till soils and readily distinguished from Muniac soils.
Till soils have developed in nonstratified deposits with angular
coarse fragments (cobbles, gravels, and stones), finer textures
and friable to very firm consistence. Muniac soils have been
mapped in association with other soils formed on fluvial
sediments: Grand Fall and Maliseet. They are differentiated on
the basis of particle size class and coarse fragment lithology.
Maliseet are coarse loamy nonskeletal materials, i.e., they lack
the gravel content of Muniac soils. Grand Falls soils have
developed on gravelly glaciofluvial materials, but they have
been derived from non-calcareous rock types.
Biological production on Muniac soils is limited by low
fertility retention and low water holding capacity. Excessive
wetness is an additional problem on poorly drained sites.
Where surface textures and organic matter enhance water
retention, Muniac soils are productive for some agricultural
crops, this primarily being because they are quick to dry and
warm up in the early spring. Muniac soil parent material is an
excellent source of aggregate for road building, construction
and related uses. It is extracted for local use from numerous
sites.
Summary of general characteristics of the Muniac Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: MU
: Chaleur Uplands
: 300-600 m
: 2450 ha
: 0.09%
: Mineral
: Fluvial (glaciofluvial)
: Up to 20 m
: Olive to olive brown
: Sandy skeletal
: Calcareous slate, shale, quartzites and
sandstones
: Medium
: Undulating or terraced (2-15%)
: Rapid
: Orthic Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 35
35 - 100+
Texture Class
Sandy loam
Loamy sand - sandy
loam
% Sand
65
80
% Silt
23
10
% Clay
12
10
% Coarse
Fragments
35 rounded, flat,
elongated G
60 rounded, flat,
elongated G
pH (H2 O)
5.0 - 5.5
5.5 - 7.5
BD (g/cm3 )
1.20
1.50
Ksat (cm/hr)
> 25
> 25
AWHC (cm/cm)
0.10 - 0.20
< 0.10
73
Nigadoo River Association
The Nigadoo River association consists of soils that have
developed in relatively thin (less than 2 m thick) deposits of
acidic, coarse loamy, compact morainal till sediments derived
from metagabbro and metabasalt, with some granites,
conglom erate and metagreywacke. They are scattered across
the northern half of the Chaleur Uplands and New Brunswick
Highlands physiographic regions at elevations of 200 to 700 m
above sea level (Fig. 45). Nigadoo River soils occupy
approximately 35,342 ha, or 1.27% of the map sheet.
soils have enough organic carbon in the B horizon to be
classified as Orthic Ferro-Humic Podzols. Humo-ferric
podzolization is the rule where climatic conditions are milder.
Imperfectly drained Nigadoo River soils occur as Gleyed
Humo-Ferric Podzols. Poorly drained soils are Orthic
Gleysols or Fera Gleysols. They are found more extensively
in gently undulating landscapes, but also occur as localized
areas in depressions and along drainage channels in more
strongly sloping map units. Internal drainage is restricted by
a slowly to moderately slowly permeable subsoil with an
estimated saturated hydraulic conductivity value of less than
0.1 cm/hr. Available water storage capacity ranges from 0.25
to 0.10 cm/cm, decreasing with depth because of increased
coarse fragment content and reduced total porosity in the
compact subsoil. Well drained sites are supplied with water
solely via precipitation. Nigadoo River subsoils have firm
consistence with a bulk density greater than 1.75 gm/cm 3 and
voids consisting predominantly of micro pores. Downward
movement of excess moisture through the profile is impeded
by the subsoil and lateral flow or seepage occurs along the
subsoil contact. The seepage waters are moderately rich in
nutrients and thus beneficial to most biological production.
Imperfectly and poorly to very poorly drained areas have
developed because of a combination of topographic position,
lack of gradient, subsoil compaction, seepage and high
groundwater table.
Figure 45. Location of mapped Nigadoo River soils.
The soil parent material has been deposited as ground moraine,
plastered in place under the weight of advancing glacial ice.
Composition strongly reflects the incorporation of local
bedrock formations consisting of dark-coloured, basic, finegrained volcanics. Smaller amounts of light-coloured, acidic
granitic and metasedimentary rocks also occur. Nigadoo River
soils are moderately to very stony with 2 to 15% of the land
surface occupied by stones. Boulders are common but usually
not in sufficient quantities to warrant designation as a bouldery
phase. Nigadoo River soils have been mapped on a number of
landforms ranging from undulating and rolling, to hummocky,
hilly, sloping and ridged. Slopes vary from 2 to 45%.
Bedrock outcrops are not common but may occur in some of
the more strongly sloping landscapes, particularly topographic
highs or along steeply inclined drainage channels. Well
drained soils of the Nigadoo River association support mixed
wood forest communities of red and sugar maple, beech, red
oak, birch, white pine, black spruce and balsam fir. On
poorly to very poorly drained sites the tree vegetation consists
of black spruce, balsam fir, cedar and tamarack with some red
maple and yellow birch.
Nigadoo River soils are dominated by well, moderately well
and imperfect drainage. Well drained sites are generally Orthic
Ferro-Humic Podzols (Fig. 46). Climatic conditions in central
New Brunswick promote the accumulation of organic matter
in the podzolic B horizon. As a result, most Nigadoo River
Figure 46. Well drained Nigadoo River soil profile.
Soil development varies from 40 to 50 cm in thickness. The
common horizon sequence on well drained sites is LFH, Ae,
Bhf, Bf, BC and C. The organic layer averages 5 to 10 cm
thick. It overlies a thin (5 to 10 cm), ashy coloured Ae horizon
which breaks abruptly into the B horizon. The upper reddish
brown to strong brown Bhf horizon varies from 5 to 15 cm in
74
thickness. It merges with a yellowish brown Bf horizon which
gradually grades into the brown to yellowish brown parent
material. Imperfectly drained soils have similar profile
horizons but are mottled in the B and C horizons, especially a
thin zone immediately above the compact subsoil where water
is perched. The Bhf horizon is also typically thinner in
imperfectly drained sites. Poorly to very poorly drained
horizon sequences lack a podzolic B horizon. They consist of
LFH or O, Aeg, Bg or Bgf, BCg, and Cg horizons. As with
most ill-drained catenary members, the forest duff layer is
usually thicker in the poorly and very poorly drained sites than
that found in well and imperfectly drained counterparts. The
Nigadoo River textural profile consists of a loam to silt loam
or sandy loam (8 to 18% clay) throughout. Profile coarse
fragment content averages 15 to 30%, with a preponderance of
subangular gravels and cobbles. Although the parent rocks are
intermediate in weatherability, they yield sediments of medium
to high fertility. Nigadoo River soils are relatively acidic
throughout the profile with pH(H 2O) values ranging from 4.0
to 5.5. The solum is friable to very friable and grades into a
firm and massive subsoil at approximately 45 cm. The subsoil
may be pseudoplaty as a result of its mode of deposition
(having been plastered in place by glacial ice).
The Nigadoo River association is most commonly found with
other soil associations that have developed on till soil materials
of volcanic rock-type origin, particularly Tetagouche,
Tetagouche Falls and Popple Depot.
Nigadoo River,
Tetagouche and Tetagouche Falls soils have all developed
from materials dominated by ferromagnesian, dark-coloured,
“mafic”, volcanic rock types. They are differentiated on the
basis of consistence and particle size. Nigadoo River soils are
coarse loamy and compact in the subsoil. Tetagouche soils are
fine loamy and compact in the subsoil. Tetagouche Falls soils
are loamy and non-compact in the subsoil. Of all soils,
Nigadoo River is probably most similar physically and
morphologically to Popple Depot soils. Both have developed
on coarse loamy compact tills. They are separated on the basis
of lithology. Popple depot soils are dominated by lightcoloured, or “felsic” volcanic rock types. In areas of complex
bedrock geology and/or along bedrock transition zones,
Nigadoo River soils are also mapped with Carleton, Long
Lake and Thibault soils.
Excluding problems due to wetness in imperfectly and poorly
to very poorly drained locations, the dominant features
affecting land use are: coarse fragment content (both surface
and profile); topographic conditions (excessive slope) and the
presence of a subsoil restricting layer which impedes root
penetration and water percolation. However, medium inherent
fertility is an asset to forest production.
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: Glacial till, compact
: <2 m
: Yellowish brown
: Coarse loamy
: Metagabbro and metabasalt with some
granites, conglomerate and
metagreywacke
: Medium
: Undulating to rolling and hummocky,
hilly, sloping and ridged (2-45%)
: Moderately well
: Orthic Ferro-Humic Podzol and Orthic
Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Loam
Sandy loam - loam
% Sand
40
55
% Silt
44
33
% Clay
16
12
% Coarse
Fragments
15 subangular G/C
25 subangular G/C
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.10
1.80
Ksat (cm/hr)
2 - 10
< 0.1
AWHC (cm/cm)
0.20
0.10
Parleeville Association
The Parleeville association consists of soils developed in thin
(less than 1 m) to moderately thick (greater than 2 m) deposits
of acidic (but increasing in pH with depth), coarse loamy to
loamy skeletal, noncompact, morainal glacial till material
(ablational till) with coarse fragments of soft arkosic sandstone
and weathered conglomerate pieces (granites, quartzites,
volcanics and so me sandstones). Parleeville soils occur in the
southern portions of the New Brunswick Highlands and
Chaleur Uplands at elevations of 100 to 300 m above mean sea
level (Fig. 47). The Parleeville ablational till material is
underlain by weathered red sandstone and conglom erate
bedrock that has a weakly calcareous cementing agent. In
veneer phases the bedrock occurs within 1 metre of the surface
and is often weathered in situ, thus some of the soil parent
material is residual in origin. Parleeville soils occupy
approximately 16,800 ha or 0.60% of the map area.
Summary of general characteristics of the Nigadoo River Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
: NR
: Chaleur Uplands, N.B. Highlands
: 200-700 m
: 35,342 ha
: 1.27%
: Mineral
Parleeville soils are considered to have developed in ablational
till. Ablational till is the accumulation of debris deposited
from glacial ice during down wasting or melting of the glacier.
In the case of Parleeville, some of the parent material may be
non-compact lodgment till or residual. Landforms range from
75
Figure 47. Location of mapped Parleeville soils.
rolling to strongly undulating, with slopes of 2 to 15%. Where
down wasting of glacial ice was more rapid, thin layers of
Parleeville ablational till were deposited. Although the soil is
shallow in these units, bedrock outcrops are scarce. The soil
parent material consists of a heterogeneous mixture of sand,
silt, clay and coarse fragments, mostly gravels, but with some
cobbles. Most coarse fragments are subrounded to subangular
gravels of granite, quartzite, volcanics and arkosic sandstone.
Parleeville soils are usually slightly to moderately stony on the
surface. Stones are greater than 2 m apart and occupy less than
3% of the surface area. Well drained Parleeville sites support
mixed stands of black spruce, balsam fir, grey and yellow
birch, sugar maple and some beech. On ill-drained sites the
sugar maple and beech component is superseded by red maple,
cedar, tamarack, speckled alders and willow.
The Parleeville association is dominated by well to moderately
well drained Orthic Humo-Ferric Podzols. Podzolization is
strongly expressed, even in sites that are less than well drained.
Imperfectly drained sites are Gleyed Humo-Ferric Podzols and
poorly to very poorly drained sites, Gleyed Eluviated Dystric
Brunisols or Orthic Gleysols. Internal drainage is good. The
profile consists of a rapidly permeable solum over a
moderately permeable subsoil.
Saturated hydraulic
conductivity values range from greater than 10 cm/hr in the
solum to 2 to 5 cm/hr in the subsoil. Available water storage
capacity ranges from 0.10 to 0.20 cm/cm, the higher values
being in the solum where finer textures and organic matter
contents enhance moisture retention. Precipitation is the sole
source of water input on well drained sites. Imperfectly and
poorly to very poorly drained sites are the result of high water
table and groundwater flow. Drainage is largely determined by
topography. Well to moderately well drained soils dominate
areas of rolling topography. Undulating map units are
dominated by imperfectly drained conditions. Poorly drained
sites are restricted to depressions and stream channel locations.
Solum development in Parleeville soils varies from 35 to 55
cm in thickness. The common horizon sequence is: LFH, Ae,
thin Bhf, Bf, Bfj, BC and C on well to moderately well drained
sites; LFH or O, Ae, Bfgj, BCgj or BCg and Cg on imperfectly
or poorly drained sites; and LFH or O, Ae, Bmgj, BCg and Cg,
or LFH or O, Aeg, Bg and Cg on poorly or very poorly drained
sites. Soil textures grade from a loam to sandy loam, which is
sometimes gravelly, into a gravelly to very gravelly sandy
loam to loam subsoil. Coarse fragment content increases with
depth. It ranges from 15 to 30% but may be as high as 50% in
some shallow lithic phases. Most coarse fragments are gravels
of granite, quartzite, volcanics and arkosic sandstone that have
weathered from the conglomerate bedrock. Parleeville soils
are medium in natural fertility, owing to the bases associated
with the weathered weakly calcareous cementing agent in the
parent conglomerate bedrock. However, the profile is acidic
throughout the upper metre, ranging from a pH(H 2O) of 4.0 to
5.5. The parent material is reddish brown to weak red.
Typically, well drained soil profiles consist of a pinkish gray,
friable, weak, fine platy Ae horizon over a yellowish red to
yellowish brown, very friable, weak to moderately fine
granular Bhf/Bf (the Bf being the lighter colour) which merges
gradually into the friable, very weak, subangular blocky to
structureless BC and then C. Mottles and grayish gley colours
modify the profile morphology in imperfectly and poorly
drained sites. Under poorly and very poorly drained
conditions the podzolic sequence is not present.
Parleeville soils were not mapped in association with any other
soil types. They tend to occur as “islands” within a sea of soils
developed from yellowish brown to olive brown coloured
parent materials. As such, Parleeville soils are readily
identified by their strong reddish brown colour. In this respect,
parent material colour, they are most similar to Stony Brook
soils. Stony Brook soils have fine loamy, very dense compact
subsoils in comparison to the coarse loamy, open, porous
subsoils in Parleeville. Parleeville soil parent materials are
also more lithologically diverse.
Parleeville soils are suitable for a wide range of agricultural
and forestry crops. Veneer phases may pose some limitations
to crop production due to lowered water-holding capacities.
Forest site capability is enhanced by the moderately rich
natural fertility.
Summary of general characteristics of the Parleeville Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: PA
: Chaleur Uplands, N.B. Highlands
: 100-300 m
: 16,800 ha
: 0.60%
: Mineral
: Glacial till, noncompact, some residual
material
:<2m
: Reddish brown
: Coarse loamy to loamy skeletal
: Sandstone and conglomerate
: Medium
: Undulating to rolling (2-30%)
: Well
: Orthic Humo-Ferric Podzol
76
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Loam - sandy loam
Sandy loam - loam
% Sand
45
55
% Silt
40
30
% Clay
15
15
% Coarse
Fragments
15 rounded G
30 rounded G
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.10
1.50
Ksat (cm/hr)
> 10
2-5
AWHC (cm/cm)
0.15 - 0.20
0.10
similar composition. Mixing actions of soil formation have
obliterated most evidence of the ablational capping. The solum
is underlain by a dense compact lodgment till subsoil (parent
material). Because of the relatively thin nature of these
deposits, the surface expression generally reflects the
topography of the underlying bedrock. Landforms consist of
a mixture of blankets and veneers over undulating, rolling,
hilly and sloping bedrock formations. Slopes range from 2 to
30% with the occasional slope ranging up to 70% were streams
and rivers are deeply incised into the landscape. Bedrock
exposures occupying up to 25% of the map unit area may be
found in these more steeply sloping areas. Well drained
Popple Depot soils support mixed softwood-hardwood stands
of balsam fir, black spruce, red spruce, white birch, yellow
birch, and sugar and red maple. Forest cover on poorly drained
sites is comprised of balsam fir, black spruce, cedar, red maple,
tamarack and some yellow birch.
Figure 48. Location of mapped Popple Depot soils.
Popple Depot soils are dominated by well drained Orthic
Ferro-Humic Podzols and Orthic Humo-Ferric Podzols.
Climatic conditions in central New Brunswick are conducive
to the accumulation of organic matter in the podzolic B
horizon. Macro- and mesoenvironmental conditions are such
that organic carbon accumulates in sufficient quantities to
qualify most Popple Depot soils for Ferro-Humic Podzol great
group status. Ferro-humic podzolization is not as strongly
expressed along the eastern periphery of the Popple Depot
range where the Central Highlands merge with the Maritime
Plain, which has a slightly milder climate than the Highlands.
Mesoenvironmental differences due to the type of vegetation
and thus the type of litter are also important in determining
variation in solum formation within a map unit. Well drained
conditions dominate steeply sloping hilly and rolling
landscapes. In these landforms poorly and imperfectly drained
conditions are confined to relatively narrow drainage channels.
Significant hectarages of imperfectly drained Popple Depot
soils occur as Gleyed Humo-Ferric Podzols in areas of
undulating and gently rolling topography, where they are
found in association with well drained or poorly drained
associates. Poorly drained soils of the Popple Depot
association are Orthic Gleysols or Fera Gleysols. Internal
drainage is restricted by a slowly permeable subsoil with an
estimated saturated hydraulic conductivity value of 0.1 to 0.5
cm/hr. Available water storage capacity ranges from 0.20 to
0.10 cm/cm, decreasing with depth because of reduced total
porosity in the compact subsoil. Well drained sites are
supplied with water solely via precipitation. Downward
movement of excess moisture through the profile is impeded
by the subsoil. Some lateral flow occurs for short durations.
Imperfectly and poorly to very poorly drained areas have
developed because of a combination of topographic position,
lack of gradient, subsoil compaction, seepage and high
groundwater table.
Popple Depot parent material has been deposited as ground
moraine, basal till plastered in place during glacial advance and
subsequently covered with a thin discontinuous mantle of
ablational till upon glacial retreat. Both materials are of
Solum thickness ranges from 35 to 55 cm. On well drained
sites the common horizon sequence is LFH, Ae, Bhf, Bf, BC
and C or Cx. The upper horizons, LFH, Ae, and Bhf are all
relatively thin (3 to 15 cm) but distinct in appearance.
Mineralization and humification processes in the organic layer
Popple Depot Association
The Popple Depot association consists of soils that have
developed in moderately thin (less than 2 m) deposits of acidic,
coarse loamy compact morainal till derived from mixed
rhyolite and trachytes with some basalt and miscellaneous
slates and greywackes. Popple Depot soils are located in the
New Brunswick Highlands and eastern Chaleur Uplands
physiographic regions (Fig. 48). Elevations range from 120 to
700 m above sea level.
In total these soils occupy
approximately 148,083 ha or 5.31% of the total map area.
77
are slow. The F horizon dominates over the H horizon. The
light grayish coloured Ae overlies the dark reddish brown
coloured Bhf which in turn changes abruptly to a 10 to 25 cm
thick, yellowish brown coloured Bf horizon. The Bf horizon
grades through a transitional BC horizon into a compact C
horizon. The C horizon may have fragipan formation, which
when moist is difficult to differentiate from the compact parent
material. When dry, the fragic material is brittle and slakes in
water. Well drained profiles with fragipan development are
classified as Fragic Humo-Ferric Podzols. However, most of
the fragipan in Popple Depot soils is weakly expressed and
limited in areal extent. Bedrock exposures occur in better
drained more steeply sloping sites and may occupy as much as
10 to 25% of these units. Imperfectly drained members of the
Popple Depot association have a similar sequence of horizons,
but display distinct or prominent mottling, especially along the
contact with the dense, compact subsoil. Gleying becomes
more prominent in lower-slope site positions.
Some
imperfectly drained Popple Dep ot soils have thin
(approximately 5 cm thick) Ahe horizons sandwiched between
the H and Ae horizons. Poorly to very poorly drained Popple
Depot soils have profiles consisting of LFH of O, Aeg, Bg or
Bgf, and Cg horizons. The predominance of coniferous forest
vegetation on these sites encourages mosses and the
accumulation of thicker organic layers.
The Popple Depot texture profile consists of a sandy loam to
loam throughout, with 8 to 18% clay content. Weathering
within the solum may result in a slightly finer texture in the
upper profile than in the subsoil , however, this variation is still
within the sandy loam-loam grouping. Profile coarse fragment
content ranges from 20 to 40% with subangular stones, cobbles
and gravels and even boulders. Most Popple Depot land
surfaces are moderately to very stony with stones occupying 2
to 15% of the surface area. Usually these soils are also
moderately to very cobbly with surface coverage similar to that
of the stones. Surface boulders are present but not in
significant quantities to warrant designation. Popple Depot
soils are low in natural fertility. The parent rocks weather
slowly and yield relatively infertile soil material. Both the
solum and subsoil are acidic, falling within a pH(H2O) range
of 4.0 to 5.5. The solum is moderate, fine to medium,
granular to subangular blocky structured and very friable. It
provides a 40 to 50 cm potential rooting zone. The parent
material is firm to very firm, compact, and slightly cemented
in the upper C horizon. The C horizon is usually pseudo platy
in situ but breaks to medium subangular blocky when
extracted.
Popple Depot soils have been mapped with Catamaran, Jacquet
River, Nigadoo River, Long Lake, McGee, Tetagouche and
Tetagouche Falls soils. Jacquet River soils have developed in
tills of similar lithology to Popple Depot soils. They are
differentiated on the basis of subsoil compaction. Jacquet
River soils have a noncompact subsoil. Popple Depot soils
have a compact subsoil. Catamaran soils are closest to the
Popple Depot association in terms of physical, chemical and
morphological properties. They are similar in colours, textures
and structures, but Catamaran soils are derived from granites,
schists and quartzite.
Biological production on Popple Depot soils is affected by low
inherent fertility, surface stoniness, depth to a root/water
restricting layer, climate, and to a lesser degree wetness and
topography. These limitations more severely handicap
agriculture than forestry. Agricultural potential is marginal.
Popple Depot soils should prove adequate to support
moderately productive stands of forest tree species climatically
suited to the region.
Summary of general characteristics of the Popple Depot Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: PD
: N..B. Highlands
: 120-700 m
: 148,083 ha
: 5.31%
: Mineral
: Glacial till, compact
: <2 m
: Yellowish brown to olive brown
: Coarse loamy (skeletal)
: Rhyolite and trachyte with some basalt
and slates and greywacke
: Low
: Undulating to rolling or hilly (2-30%)
: Moderately well
: Orthic Ferro-Humic Podzol and Orthic
Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Loam
Sandy loam - loam
% Sand
50
55
% Silt
35
33
% Clay
15
12
% Coarse
Fragments
20 subangular G/C
30 subangular G/C
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.10
1.80
Ksat (cm/hr)
2-5
0.1 - 0.5
AWHC (cm/cm)
0.15 - 0.20
0.10
Reece Association
The Reece Association consists of soils developed in
moderately thin (1 to 2.5 m) to thin (less than 1 m) deposits of
acidic, fine loamy, compact glacial till material (lodgment till)
with coarse fragments of soft sandstone. Reece soils occur in
the lowlands portion of the study area at elevations ranging
from 40 to 140 m above sea level (Fig. 49). The lodgment till
frequently has a surficial capping of coarse loamy ablational
78
till (Sunbury material). Reece soil materials are underlain by
the soft gray-green Pennsylvanian sandstone that underlies
most of the New Brunswick Lowlands or Maritime Plain.
Some veneer phases occur where the bedrock is within 1 metre
of the soil surface. Reece soils occupy approximately 332,784
ha, representing 11.94% of the map area.
Figure 49. Location of mapped Reece soils.
Lodgment till consists of successive layers of glacial debris
which is plastered into place below the glacier as it advances.
The finer textured nature of Reece soil parent material is
attributable to a shale component within the debris. At the
time of glaciation the Pennsylvanian aged bedrock is thought
to have had interbedded shale-sandstone near the surface. The
scouring nature of glacial ice readily abraded the shales. The
softer shale (and siltstone) fragments have completely
disintegrated. Only fragments of the more durable sandstone
remain intact. The lodgment till is characterized by its
physical heterogeneity. There is no size assortment and no
evidence of stratification with exception of a pseudo platy
structure caused by compaction under ice pressures during
deposition. Soil and coarse fragment shapes vary from sharp
and angular to subrounded, depending upon fluctuations in the
grinding actions caused by the ice. Reece soils have
moderately stony to very stony land surfaces. Stones are 1 to
10 m apart and occupy 0.1 to 15% of the surface area. Reece
soils tend to be most stony where mapped in association with
Sunbury soils. This is the result of the ablational till capping
on the lodgment till. Reece landforms are typified by
undulating to very gently rolling surface expressions with 2 to
7% slopes. Well drained sites support stands of black spruce,
balsam fir, sugar maple, white birch and beech. As drainage
conditions deteriorate the sugar maple, white birch and beech
give way to red maple and yellow birch. Cedar and tamarack
occur on very poorly drained sites.
The Reece association is dominated by imperfectly drained
Gleyed Humo-Ferric Podzols. There are extensive areas of
impeded drainage. Well to moderately well drained Orthic
Humo-Ferric Podzols (Fig. 50) and Fragic Humo-Ferric
Podzols or poorly to very poorly drained Fera Gleysols are
usually subdominant components of map units dominated by
imperfectly drained soils. Internal drainage is restricted by a
slowly permeable subsoil (0.1 to 0.5 cm/hr saturated hydraulic
conductivity). The solum permeability is usually 5 cm/hr or
faster. Available water storage capacity ranges from 0.15 to
0.20 cm/cm in the solum, but is less than 0.10 cm/cm in the
subsoil. Low available water storage capacity in the subsoil is
due to compaction and thus lower total pore space. On well
drained sites precipitation is the dominant water source.
Excess water flows laterally as subsurface flow. Where there
is less gradient, water is removed from the soil somewhat
slowly in relation to supply giving rise to m oderately well
drained conditions. Imperfectly drained sites occupy mid to
lower slope positions where water is supplied by precipitation
and subsurface flow or seepage. Poorly and very poorly
drained conditions are strongly influenced by subsurface
inflow and groundwater flow, in addition to precipitation.
They occupy lower slope, toe and depressional sites. Lateral
water movement is promoted by the dense, slowly permeable
Reece subsoil.
Profile development is moderately thick, 40 to 70 cm. The
common horizon sequence is LFH, Ae, Bf, BC or BCx and
(II)C or (II)Cx, on well drained sites; LFH, Ae, Bfgj, BCgj or
BCxgj and (II)Cg or (II)Cxg on imperfectly drained sites; and
LFH or O, Aeg, Bgf and (II)Cg or (II)Cxg on poorly to very
poorly drained sites. Soil horizon continuity is often disrupted
by tree uprooting, especially on imperfectly and poorly drained
sites. Windthrow also promotes hummocky micro topography
in these sites. Poorly drained profiles may have a 10 to 30 cm
thick accumulation of organic debris on the surface, especially
in level and depressional areas where Reece soils are
associated with organic soils, Lavillette or Acadie Siding.
Climatic conditions on the western edge of the lowlands plain
adjacent to the uplands boundary result in thin Bhf
development in the upper B horizon. Fragipan, indicated by
the "x" suffix in the horizon designation, is a common
characteristic of Reece soils. It is a hardpan with high bulk
density, very low organic matter content and slow to very slow
permeability that forms in the lower B and C horizons. When
moist, fragipans are moderately to weakly brittle and difficult
to differentiate from the compact lodgment till. When dry,
they have a hard consistence and seem to be cemented. But
they are reversible pans and air dried clods of fragic horizons
slake or fracture when placed in water. Most Reece soils occur
below the maximum level of post glacial marine submergence.
Coarser textures in the upper solum may be attributed to this.
Sandy marine sediments may have been deposited during this
period of submergence and subsequently incorporated into the
upper soil profile. The Reece texture profile consists of a sandy
loam to loam solum over a loam to sandy clay loam or clay
loam subsoil. Profile coarse fragment content averages 10 to
25%, with higher percentages occurring in some lithic (veneer)
phases. Coarse fragments are subangular to flat cobbles,
gravels and stones of soft, gray-green sandstone derived from
the local bedrock. The sandstone is fine- to medium-grained.
It is dominated by quartz but with significant feldspars, biotite
and muscovite. Reece soils are medium in natural fertility.
79
glacial till soils that occur on the lowland plain with Reece
soils. Reece, Rogersville and Stony Brook soils have all
developed on fine-loamy lodgment till materials. Rogersville
soils are more reddish brown in colour, are somewhat heavier
in texture, but most obviously, have a granitic component in
their lithological composition. Stony Brook soils have a red to
reddish brown subsoil which is the most obvious
differentiating criteria from Reece soils. They are also slightly
heavier in texture. Reece soils are most intimately associated
with Sunbury soils. In fact, they may be identical in the upper
solum.
They are separated on the basis of subsoil
characteristics. Sunbury soils are coarser textured and
noncompact. Poorly drained Reece soils are often situated
adjacent to organic soils, either Acadie Siding or Lavillette.
Thickness of the organic layer is used to differentiate mineral
from organic soils. Mineral soils such as Reece have less than
40 cm of organic debris on the surface. Reece soils have also
been mapped with Long Lake and Catamaran soils along the
Maritime Plain - New Brunswick Highlands boundary. Both
Long Lake and Catamaran soils have developed on compact
lodgment till materials, but they are coarse-loamy.
Lithological differences are also used to separate Long Lake
(slate, siltstone, argillite, schist, quartzite and greywacke) and
Catamaran (granites with greywacke, schists, quartzite, slates
and sandstones) from Reece (sandstone).
The major limitations to biological production on Reece soils
are a result of the drainage-compact subsoil situation.
Stoniness may also be detrimental in agricultural usage. From
a forestry perspective Reece soils are among the most
productive soil types found in the lowlands.
Figure 50. Well drained Reece soil profile.
Summary of general characteristics of the Reece Association
The profile is acidic throughout, falling between pH(H2O) 4.0
and 5.5. Well drained soil parent materials are strong brown to
dark yellowish brown. The profile consists of a grayish,
friable, weak, fine platy Ae horizon over a yellowish red to
yellowish brown, very friable, weak to moderate, fine granular
Bf horizon which grades through a BC horizon into a firm to
very firm, weak subangular blocky or platy to structureless C
horizon. A thin slightly grayish zone of lateral leaching may
be present immediately above the compact layer.
In
imperfectly drained soils temporarily perched water tables
create a mottled zone along the friable-compact interface.
Grayish gley colours dominate poorly drained profiles.
Fragipan formation is related to site drainage. It is most
strongly expressed on well drained sites where development
averages 40 to 60 cm in thickness, the upper boundary of
which occurs at depths of 50 to 70 cm below the mineral soil
surface. Poorly drained conditions have weakly developed
pans that are thinner, 20 to 30 cm thick, and have formed
closer to the surface, at depths of 30 to 40 cm. The upper
boundary is clear and abrupt while the lower boundary is
gradual or diffuse. Fragipans have very coarse prismatic
structure separated by bleached vertical fissures or planes that
produce a polyhedron pattern when cut horizontally, such as in
ditch bottoms.
Rogersville, Stony Brook and Sunbury associations are other
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: RE
: Maritime Plain
: 40-140 m
: 332,784 ha
: 11.94%
: Mineral
: Glacial till, compact
: <2.5 m
: Strong brown to dark yellowish brown
: Fine loamy
: Gray-green sandstone and weathered shale
: Medium
: Undulating to gently rolling (2-7%)
: Imperfect
: Gleyed Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 50
50 - 100+
Texture Class
Sandy loam - loam
Loam - sandy clay
loam
% Sand
55
50
% Silt
30
23
% Clay
15
22
80
% Coarse
Fragments
10 subangular
C/G/S
20 subangular C/G/S
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.10
1.80
Ksat (cm/hr)
>5
0.1 - 0.5
AWHC (cm/cm)
0.15 - 0.20
< 0.10
Richibucto Association
The Richibucto association consists of soils developed in
relatively thin (less than 2.5 m) deposits of acidic, sandy
marine sediments derived from soft sandstone. They occur
only in the lowlands portion of the study area where they are
confined to a narrow strip about 10 km wide along the coast,
occasionally fingering inland more deeply along tidal rivers
(Fig. 51). Thin deposits (veneers less than 1 m thick) rest
directly on weathered gray-green Pennsylvanian sandstone
bedrock. Thicker deposits (greater that 1 m) may be underlain
by a thin mantle of morainal till overlying the bedrock.
Richibucto sands are also underlain by marine/lacustrine clays
along some estuarial valleys. Most Richibucto soils are found
at elevations of less than 50 m above sea level. They cover
approximately 60,029 ha, or about 2.15% of the map area.
Figure 51. Location of mapped Richibucto soils.
Richibucto parent materials are marine sediments or marine
reworked glaciofluvial material, some of which may have been
deposited subaqueously. They were deposited in an early
postglacial, shallow brackish water environment. Acid
leaching has destroyed any calcareous fossils that may have
been present but material composition and configuration
coupled with its general location below the level of postglacial
marine submergence indicate a marine mode of deposition.
Richibucto soils have developed on wave-washed sediments
deposited as marine beach ridges, marine terraces and
discontinuous blankets and veneers of marine sand. They
consist of well sorted sands, primarily medium- to fine-grained
particles, but some strata are gravelly or pebbly. Associated
landforms have level to gently undulating surface expressions,
with slopes of 0.5 to 2%. Steeper gradients may occur along
river valleys. Well to rapidly drained Richibucto soils support
softwood stands of predominantly jack pine and black spruce.
Stunted gray birch occurs on the more droughty sites. Red
maple, white birch, black spruce and balsam fir occur on the
wetter sites.
The Richibucto association is made up of rapidly to well
drained Orthic Humo-Ferric Podzols and Eluviated Dystric
Brunisols, imperfectly drained gleyed subgroups of the
afore-mentioned, and poorly to very poorly drained Gleyed
Eluviated Dystric Brunisols and Orthic Gleysols. In well and
imperfectly drained associates the B horizon, although
appearing morphologically typical of a Bf horizon, just meets
the chemical requirements for a podzol. The deceiving
appearance is the result of the sandy nature of the material and
the fact that very little illuviated iron and organic matter is
required to significantly affect a colour change. Poorly drained
soils do not meet podzolic requirements. On rapidly to well
drained sites precipitation is the sole source of water. Excess
water readily flows downward through the pervious subsoil
which has saturated hydraulic conductivity values of greater
than 25 cm/hr. Available water storage capacity is low, usually
less than 0.10 cm/cm and decreases with depth. Slightly finer
textures and higher organic matter contents enhance moisture
retention in the solum. Imperfectly and poorly drained
conditions are the result of high groundwater tables.
Groundwater levels respond quickly to additions by
precipitation because of the low moisture holding capacity of
the soil profile and the relative ease of groundwater flow
through the coarse textured subsoil. Substrata, bedrock (Fig.
52) or relatively impermeable morainal till or marine clays,
also create deep (below the control section) seepage conditions
which recharge these sites.
Soil formation averages 30 to 50 cm in depth, however, most
development is concentrated in the upper 30 cm of the profile,
below which is a zone of transition into the parent material.
Common horizon sequences consist of: LFH , Ae, Bf or Bm,
BC and C in rapidly to well drained sites; LFH , Ae, Bfgj or
Bmgj, BCgj and Cg in imperfectly drained sites; and LFH or
O, Aegj, Bmgj, BCg and Cg, or O, Aeg, Bg and Cg in poorly
to very poorly drained sites. Rapidly to imperfectly drained
profiles have a typical podzolic appearance. They have a thin
organic duff layer over a light grayish coloured eluvial A
horizon. The underlying reddish brown to yellowish brown B
horizon has an abrupt upper boundary and becom es
progressively yellower as it grades through the BC into the
brown to yellowish brown C horizon. Iron (Fe) mottling
modifies this appearance in imperfectly drained sites. Poorly
and very poorly drained sites are often severely gleyed because
of the persistence of waterlogged conditions. Very poorly
drained sites often have bluish gray subsoils. Horizonation is
weakly expressed. The texture profile grades from a loamy
sand to sandy loam solum into a loamy sand to sand subsoil.
Clay content seldom exceeds 10% and is usually less than 5%
81
in the subsoil. The high degree of particle size sorting is
exemplified by subsoils in which sand accounts for 95 to 97%
of the soil material. Most profiles are relatively free of coarse
fragments. Those coarse fragments that are present are usually
rounded gravels of soft gray-green sandstone. Occasionally
there is as high as 20% gravels. These areas are thought to be
remnants of beach ridges. Veneer phases may also be an
exception to this. Frost action and windthrow mix thin, flat
fragments of the underlying bedrock into the lower profile.
Richibucto soils are very low in natural fertility and nutrient
retention capability. They are also acidic, with pH (H2O) 4.0
to 5.0, throughout. Soil structure is weakly expressed in the
solum and structureless or single grain in the subsoil.
Consistence is typically very friable to loose, except for the
presence of ortstein, a firmly cemented hardpan, that occurs
sporadically in the solum. Ortstein is a discontinuous,
irreversible pan in which the soil particles are bonded by Fe,
Al and organic matter complexes. It is more strongly
developed under poorly drained conditions where pans are
harder and cover a greater lateral extent.
than 1 m of marine sand over a compact cobbly morainal till.
Tracadie soils are marine clays. Riverbank soils are very
similar to Richibucto soils in morphological characteristics.
However, unlike Richibucto soils, Riverbank soils are derived
from a mixture of lithologies and thus have greater
mineralogical variability. Riverbank is also associated with
different landforms; kames, eskers, stream terraces, etc. Very
poorly drained Richibucto soils are often mapped in complexes
with organic soils, either Acadie Siding or Lavillette.
Thickness of the organic layer is used to differentiate mineral
soils from organic soils. Mineral soils such as Richibucto have
less than 40 cm of organic debris on the surface.
Biological productivity on Richibucto soils is limited by very
low moisture holding capacity, inherent natural fertility and
nutrient retention. Selection of crops must be made with these
constraints in mind. Richibucto sands are easily manipulated
in terms of moisture and nutrient status by irrigation and
fertilizer applications and so are ideal sites for specialty crops
that require closely controlled environments. Richibucto
parent material is also a source of industrial sand.
Summary of general characteristics of the Richibucto Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
Figure 52. Well drained Richibucto soil profile, veneer phase.
Richibucto soils are found in close proximity to other soils that
have developed on marine sediments, the Barrieau-Buctouche
and Tracadie associations. Both soils are readily differentiated
from Richibucto soils. Barrieau-Buctouche soils consist of less
: RB
: Maritime Plain
: < 50 m
: 60,029 ha
: 2.15%
: Mineral
: Marine
: < 2.5 m
: Yellowish brown to brown
: Sandy
: Soft gray-green sandstone
: Very low
: Level to undulating (0.5-2%)
: Rapid
: Orthic Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 40
40 - 100+
Texture Class
Loamy sand - sandy
loam
Loamy sand - sand
% Sand
80
85
% Silt
10
10
% Clay
10
5
% Coarse
Fragments
< 2 rounded G
< 2 rounded G
pH (H2 O)
4.0 - 4.5
4.5 - 5.0
BD (g/cm3 )
1.20
1.50
Ksat (cm/hr)
> 25
> 25
AWHC (cm/cm)
0.10
0.05 - 0.10
82
Riverbank Association
The Riverbank association consists of soils developed in
relatively thick (sometimes in excess of 10 m) deposits of
acidic, sandy glaciofluvial material derived from igneous,
metamorphic and some sedimentary rock types. Riverbank
materials are underlain by either bedrock, or the prevailing
regional glacial till material. They are found primarily in the
New Brunswick Highlands but also occur on the western edge
of the Maritime Plain at elevations ranging from 50 to 300 m
above sea level (Fig. 53). Riverbank soils cover approximately
12,733 ha or 0.46% of the map area. They occur in small,
scattered tracts.
Figure 53. Location of mapped Riverbank soils.
Riverbank parent materials were deposited as either glacial
outwash plains and valley trains, or as ice contact stratified
drift in features such as kames and eskers. Most deposits are
found in narrow strips on river terraces and bottoms.
Deposition has been by moderately fast flowing waters.
Suspended particles were deposited when water turbulence
ceased to exceed their settling velocities, a function of particle
diameter, shape and specific gravity and fluid density.
Therefore, to a large degree, the velocity of the flowing water
determined the size of the particles that were deposited. Most
sediments consist of well rounded fine to medium sand grains.
Changes in streamflow velocity resulted in layers of varying
thickness and particle size. Deposits often contain thin layers
of silt or gravel. These strata may significantly modify internal
drainage characteristics. Riverbank landscapes are varied.
They include terraced surfaces, with horizontal or gently
inclined planes (0-3% slope) separated by scarp faces (15-45%
slope); outwash plains, with undulating (0-5% slope) surface
expressions; and ridges or eskers, with rounded crests and
steep sides (5-30% slope).
Riverbank soils support
predominately softwood stands of jack pine and black spruce,
with stunted grey birch on the drier sites. Moist sites along
stream bottoms and lower terraces have black spruce, red
maple and white birch.
The Riverbank association consists of rapidly to well drained
Orthic Humic-Ferric Podzols (Fig. 54), imperfectly drained
Gleyed Humo-Ferric Podzols, and poorly to very poorly
drained Gleyed Eluviated Dystric Brunisols, Orthic Gleysols
and Fera Gleysols. On rapidly to well drained sites water is
supplied only by precipitation. Rainfall rapidly enters the soil
and a large part of the water passes through the profile or
evaporates into the air. These soils have a low available water
storage capacity, 0.15 to 0.10 cm/cm or less, usually
decreasing with depth. Slightly finer textures and higher levels
of organic matter content aid water retention in the upper
solum. Imperfectly and poorly drained sites are restricted to
areas that are affected by high ground water levels, such as
depressions and lower terraces along valley floors.
Groundw ater flow is the main water source. Seepage is absent.
Subsoil permeability varies from less than 1 cm/hr to more
than 25 cm/hr. This wide range is due to parent material
stratification. However, most layers are rapidly permeable
with transm issibility rates of more than 10 cm/hr..
Soil development in Riverbank materials averages 30 to 50 cm
in thickness. Those sites with more suitable moisture regimes
for biological production tend to have the greatest degree of
solum development. Excessively dry and excessively moist
sites have shallower sola. The common horizon sequence in
well to rapidly drained soils is: LFH, Ae, Bf, BC and C.
Imperfectly drained profiles have LFH, Ae, Bfgj, BCgj and Cg
horizons. Poorly to very poorly drained profiles have a
number of different possible profiles: LFH, Ae, Bmgj, BCg
and Cg; or LFH or O, Aeg, Bg and Cg; or, LFH or O, Aeg, Bgf
and Cg. The surface horizons of Riverbank soils display little
evidence of the stratification so typical of their parent
materials. They also contain more silt and clay than found in
the subsoil. These modifications are attributed to soil forming
processes. Windthrow, frost action and biological activity
have mixed together the originally stratified surface materials.
Physical and chemical weathering in the solum has lead to the
disintegration and decomposition of rocks and minerals. The
Riverbank texture profile grades from a sandy loam to loamy
sand solum into a loamy sand to sand subsoil. Clay content
seldom exceeds 10% in any horizon. The sand fraction varies
from 70 to 95%. It has a wide variety of minerals such as
quartz, hornblende, biotite, muscovite and numerous feldspars.
Most profiles are relatively free of coarse fragments, but
occasionally some deposits have as much as 20% gravels and
cobbles derived from mixed igneous, metamorphic and
sedimentary rock types such as granites, schists, gneisses,
slates, quartzite and volcanics. Riverbank soils are low in
natural fertility. They are also acidic throughout the profile,
with pH (H 2O) of 4.0 to 5.0. The parent material colour is
yellowish brown to olive brown. In well drained sites the
solum consists of a thin LFH layer overlaying a leached
grayish coloured Ae horizon. The underlying Bf horizon is
yellowish brown to strong brown, becoming progressively
yellower in hue with depth. Imperfectly and poorly to very
poorly drained soils have either iron (Fe) mottling or gleyed
colours of low chroma, or both. The subsoils are loose and
single grain (structureless) but stratified. The A horizon is
friable to very friable, very weak, fine platy. Most B horizons
83
Richibucto soils are almost identical to Riverbank soils. Both
consist of well sorted sands. Richibucto sands are of marine
origin and restricted to the lowlands, usually in close proximity
to the coast. Their parent materials were derived from soft
Pennsylvanian sandstone. They lack the mineralogical
variability found in the Riverbank association.
Low water holding capacity, low natural fertility and low
fertility retention characteristics restrict biological productivity
to selected crops. In forestry, tree species must be selected that
minimize these impacts. Riverbank soils can be highly
productive for specialty crops (strawberries, apples, etc.) where
management inputs are high and moisture levels artificially
controlled. Riverbank parent material is also a source of
industrial or commercial sand.
Summary of general characteristics of the Riverbank Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: RI
: Maritime Plain, N.B. Highlands
: 50-300 m
: 12,733 ha
: 0.46%
: Mineral
: Fluvial (glaciofluvial or possibly
alluvium)
: Up to 10 m
: Yellowish brown to olive brown
: Sandy
: Mixed igneous, metamorphic and minor
sedimentary
: Low
: Undulating to terraced (0.5-5%)
: Rapid
: Orthic Humo-Ferric Podzol
Figure 54. Rapidly drained Riverbank soil profile.
are very friable, weak to moderate, fine granular, however,
occasionally they may have cemented, massive ortstein layers.
Ortstein is a strongly cem ented irreversible but discontinuous
hardpan that restricts root penetration and is only slowly
permeable to water. Fe, Al and organic complexes are the
bonding agents. Ortstein layers vary from 10 to 60 cm in
thickness. Technically speaking, ortstein is a cemented Bh,
Bhf or Bf horizon at least 3 cm thick. Those cemented
horizons that do not make the podzolic B criteria are not "true"
ortsteins. Ortstein development is drainage dependent. In
poorly drained sites it is harder and covers a greater lateral
extent than in sites with better drainage.
Riverbank soils are usually associated with other soils
developed in glaciofluvial sediments, such as Gagetown.
Gagetown is sandy skeletal, i.e., gravelly or very gravelly in
the parent material.
Gagetown and Riverbank are
lithologically identical. They are separated on percent coarse
fragment content. Gagetown soils have greater than 20%
gravels (usually 50 to 70%) and Riverbank soils have less than
20% gravels (usually less than 2%). Riverbank soils have also
been mapped with Interval soils. Interval soils have formed in
coarse loamy alluvial sediments, usually silt loams to fine
sandy loams, and are located within present-day flood plains.
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 50
50 - 100+
Texture Class
Sandy loam - loamy
sand
Loamy sand - sand
% Sand
75
90
% Silt
15
5
% Clay
10
5
% Coarse
Fragments
< 2 rounded G
< 2 rounded G
pH (H2 O)
4.0 - 4.5
4.5 - 5.0
BD (g/cm3 )
1.20
1.50
Ksat (cm/hr)
> 25
> 10
AWHC (cm/cm)
0.10 - 0.15
0.05 - 0.10
84
Rogersville Association
The Rogersville Association consists of soils developed in
moderately thin (1 to 2 m) deposits of acidic, fine loamy,
compact glacial till material (lodgment till) with coarse
fragments of sandstone, granites, gneiss, schists and some
volcanics. Rogersville soils occur in the M aritime Plain
portion of the study area at elevations ranging from 40 to 140
m above sea level (Fig. 55). The lodgment till may have a thin
surficial capping of coarse loamy ablational till or water
reworked material. Rogersville soil materials are underlain by
the soft gray-green Pennsylvanian sandstone that underlies
most of the New Brunswick Lowlands. Rogersville soils
occupy approximately 3,312 ha, representing 0.12% of the
map area.
Figure 55. Location of mapped Rogersville soils.
As a lodgment till, Rogersville soil parent material consists of
successive layers of glacial debris scoured from the earth’s
surface and redeposited or plastered into place below the
glacier as it advanced. As such, the underlying bedrock
lithology played an important role in soil characteristics. The
finer textured nature of Rogersville soil parent material is
attributed to a shale component within the debris. At the time
of glaciation, the Pennsylvanian aged bedrock is thought to
have had interbedded shale-sandstone near the surface. The
scouring nature of glacial ice readily abraded the shales. The
softer shale (and siltstone) fragments have completely
disintegrated. Only fragments of the more durable sandstone
remain intact. The granites, gneiss, schists and volcanics were
transported in from central New Brunswick as the glacial ice
travelled in a southeastern direction. The weight of glacial ice
has resulted in the subsoil having a pseudo platy structure.
Coarse fragment shapes vary but are mostly subangular to
subrounded. Rogersville soils have moderately stony to very
stony land surfaces. Stones are 1 to 10 m apart and occupy 0.1
to 15% of the surface area. Rogersville landforms are typified
by undulating surface expressions with slopes of 2 to 5%.
Well drained sites support stands of black spruce, balsam fir,
sugar maple, white birch and beech. As drainage conditions
deteriorate the sugar maple, white birch and beech give way to
red maple and yellow birch. Cedar and tamarack occur on
very poorly drained sites.
The Rogersville association is dominated by imperfectly
drained Gleyed Humo-Ferric Podzols and G leyed Podzolic
Gray Luvisols. Moderately well drained Orthic Humo-Ferric
Podzols, Fragic Humo-Ferric Podzols and some Podzolic Gray
Luvisols occur along with the imperfectly drained Rogersville
members where topographic conditions are more pronounced.
Poorly to very poorly drained Orthic Luvic Gleysols and
Fragic Luvic Gleysols occur extensively on level to very gently
undulating sites. Internal drainage is restricted by a very
slowly permeable subsoil (less than 0.1 cm/hr saturated
hydraulic conductivity) that occurs within 50 cm of the mineral
soil surface. The solum permeability is usually 5 cm/hr or
faster. Available water storage capacity ranges from 0.15 to
0.20 cm/cm in the solum, but is less than 0.10 cm/cm in the
subsoil. Low available water storage capacity in the subsoil is
due to lower total pore space as a result of compaction. Excess
water as a result of snowmelt and/or heavy precipitation flows
laterally as subsurface flow (seepage). Because of the
prevailing level topography and restricted internal drainage,
imperfectly drained sites may occupy mid to upper slope
positions as well as lower slope positions. Poorly and very
poorly drained conditions are strongly influenced by
subsurface inflow and groundwater flow, in addition to
precipitation. They occupy lower slope, toe and depressional
sites.
Profile development is moderately thick, 40 to 70 cm. The
common horizon sequence is LFH, Ae, Bf, Btj or Btjx and
(II)Cgj, on moderately well drained sites; LFH, Ae, Bfgj, Btgj
or Btxgj and (II)Cg on imperfectly drained sites; and LFH or
O, Aeg, Bgf, BCg or Bxg and (II)Cg on poorly to very poorly
drained sites. Soil horizon continuity is often disrupted by tree
uprooting because the imperfect and poor drainage limits
rooting depth. Windthrow also promotes hummocky micro
topography in these sites. Poorly drained profiles may have a
10 to 30 cm thick accumulation of organic debris on the
surface, especially in level and depressional areas where
Rogersville soils are associated with organic soils such as
Lavillette or Acadie Siding. Climatic conditions on the
western edge of the lowlands plain adjacent to the uplands
boundary result in thin Bhf development in the upper B
horizon. Fragipan, indicated by the "x" suffix in the horizon
designation, is a common characteristic of Rogersville soils.
It is a hardpan with high bulk density, very low organic matter
content and slow to very slow permeability that forms in the
lower B and C horizons. When moist, fragipans are
moderately to weakly brittle and difficult to differentiate from
the compact lodgment till. Fragipan formation is more
strongly expressed on well drained sites, but it occurs at greater
depths, usually first appearing 50 to 70 cm below the mineral
soil surface. Poorly drained conditions have weakly developed
pans that are thinner, 20 to 30 cm thick, and have formed
closer to the surface, at depths of 30 to 40 cm. Fragipan
formation is discontinuous in Rogersville soils. Clay
85
translocation from the upper solum has resulted in the presence
of a weak Bt horizon. Illuvial clay accumulations form Btj,
Btgj and Btg horizons. The Bt horizon has a very weak, coarse
subangular blocky structure and is resistant to both root and
water penetration. These horizons are similar to the subsoil in
terms of their compact consistence. Fragic layers may occur
within these horizons. The Rogersville soil texture profile
consists of a loam to sandy loam solum over a loam to sandy
clay loam or clay loam subsoil. Profile coarse fragment
content averages 10 to 25%. Coarse fragments are subangular
to somewhat subrounded cobbles, gravels and stones of mixed
lithologies - sandstone, granites, gneiss, schists and some
volcanics. Rogersville soils are medium in natural fertility.
The profile is acidic throughout, falling between pH(H2O) 4.0
and 5.5. Well drained soil parent materials are brown but may
be slightly reddish brown where Rogersville soils are
transitional to Stony Brook soils. The profile consists of a
grayish, friable, weak, fine platy Ae horizon over a yellowish
red to yellowish brown, very friable, weak to moderate, fine
granular Bf horizon which grades through a BC or Bt horizon
into a firm to very firm, weak, coarse platy to structureless C
horizon. A thin grayish zone of lateral leaching is usually
present immediately above the compact layer. In imperfectly
drained soils temporarily perched water tables create a strongly
mottled zone along this friable-compact interface. Grayish
gley colours dominate poorly drained profiles. Average depth
of friable soil material over a root or water restricting layer is
30 to 50 cm.
Rogersville association soils most closely resemble Reece soils
in morphological appearance as well as physical and chemical
characteristics. The main difference is the petrological
composition of the till. Reece soils are derived from sandstone
and weathered shale/siltstone; Rogersville soils have a
significant component of granites, gneiss, schists and
volcanics. As a result, Reece soils tend to be slightly coarser
textured than Rogersville soils. Rogersville soils are also less
permeable in the subsoil than Reece soils. While both soils
have fragipans, Reece soils have more pronounced pan
development. Reece soils also do not have horizons with
appreciable amounts of illuviated clay (Bt horizons).
Rogersville soils commonly have Bt horizons. Stony Brook is
another lodgment-till soil that occurs on the Maritime Plain
along with Rogersville soils. Stony Brook soils have a red to
reddish brown subsoil which is the most obvious
differentiating criteria. They are also slightly heavier in
texture. Stony Brook soils lack the petrological variability
found in Rogersville soils. Stony Brook soils have sandstone
coarse fragments exclusive of other rock types. Poorly and
very poorly drained Rogersville soils are also associated with,
or situated in, proximity to organic soils, either Acadie Siding
or Lavillette.
The major limitations to biological production on Rogersville
soils are related to the drainage-compact subsoil situation.
Stoniness may also be detrimental in agricultural usage. From
a forestry perspective Rogersville soils are among the more
productive soil types found in the lowlands.
Summary of general characteristics of the Rogersville Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: RS
: Maritime Plain, N.B. Highlands
: 40-140 m
: 3312 ha
: 0.12%
: Mineral
: Glacial till, compact
: 1-2 m
: Brown
: Fine loamy
: Sandstone, granites, gneiss, schists and
some volcanics and weathered shale
: Medium
: Undulating (0.5-5%)
: Imperfect
: Gleyed Humo-Ferric Podzol and Gleyed
Podzolic Gray Luvisols
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 40
40 - 100+
Texture Class
Loam - sandy loam
Loam - sandy clay
loam - clay loam
% Sand
45
40
% Silt
40
35
% Clay
15
25
% Coarse
Fragments
10 subangular
C/G/S
20 subangular C/G/S
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.15
1.80
Ksat (cm/hr)
>5
< 0.1
AWHC (cm/cm)
0.15 - 0.20
< 0.10
Stony Brook Association
The Stony Brook association consists of soils developed in
moderately thin (1 to 2 m) deposits of acidic, fine loamy,
compact glacial till material (lodgment till) with soft sandstone
coarse fragments. Stony Brook soils only occur in the lowland
portion of the study area, usually at elevations of 40 to 120 m
above sea level (Fig. 56). The thickness of the lodgment till
tends to be a uniform blanket. It is underlain by soft
gray-green Pennsylvanian sandstone, from which most profile
coarse fragments have been derived. Frequently there is a thin
40 to 50 cm thick mantle of Sunbury association coarse loamy
ablation till on the surface. It is also possible that this capping
may be due to incorporation of sandy marine sediments. Stony
Brook soils occur below the zone of maximum post-glacial
marine submergence. They occupy approximately 151,867
ha, or 5.45% of the map area.
Stony Brook subsoils are very dense and compact, properties
86
that can be attributed to their mode of deposition as lodgment
tills plastered in place below hundreds of metres of glacial ice.
Their fine texture and red to reddish brown colour come from
incorporated red shale (35% clay content) and/or reddish
clayey marine sediments. Abrasive actions during glaciation
have almost completely disintegrated the soft shales. Upon
close examination small remnants can be identified in the soil
matrix. The soil material is a heterogeneous mixture of
subangular to subrounded particles ranging in size from fine
clays to stones and even the occasional boulder. Stony Brook
soils are moderately stony on the surface, with stones 2 to 10
m apart occupying 0.1 to 3% of the land area. Stonier phases
may occur in complex units with Sunbury. Stony Brook
landscapes are undulating to level or flat morainal blankets.
Most slopes are complex but less than 5%. Bedrock outcrops
are not common. Well drained sites support stands of black
spruce, balsam fir, white birch and some sugar maple and
beech. On imperfectly drained sites the sugar maple and beech
are absent. Red maple, yellow birch, cedar, larch, black spruce
and balsam fir occupy poorly to very poorly drained sites.
Figure 56. Location of mapped Stony Brook soils.
Dense, compact subsoils with high clay-silt content combined
with level to gently undulating topography results in a high
proportion of wet soils. The predominant soils are imperfectly
drained Gleyed Podzolic Gray Luvisols intermixed with some
Luvisolic Humo-Ferric Podzols. Increased clay content in the
luvisolic horizon restricts downward movement of water.
Moderately well drained Podzolic Gray Luvisols (Fig. 57) and
Luvisolic Humo-Ferric Podzols occupy upper slope and crest
positions. Poorly to very poorly drained Orthic Luvic Gleysols
and Fera Luvic Gleysols are found on low er slope to
depressional site locations. Internal drainage is severely
impeded by a very slowly permeable subsoil with hydraulic
conductivities of less than 0.1 cm/hr. The solum is moderately
rapid to rapidly permeable (saturated hydraulic conductivity
greater than 5 cm/hr). Perched water tables are common.
Excess water flows through the solum and concentrates above
the relatively impermeable subsoil. This saturated layer of soil
is separated from the underlying true ground water table by an
unsaturated zone. Available water storage capacity is 0.15 to
0.20 cm/cm in the solum but less than 0.10 cm/cm in the
subsoil. On moderately well drained sites, precipitation is the
dominant water source. Excess w ater is removed somewhat
slowly in relation to supply because of low perviousness in the
subsoil and lack of gradient. Conversely, subsoil compaction
prevents root penetration and also limits recharge of soil
moisture in the solum. Because of this, some sites experience
moisture deficiencies or droughtiness during summers with
low precipitation. Imperfectly and poorly to very poorly
drained sites are strongly influenced by inflow of lateral
seepage waters. The seepage water found in these soils is
usually nutrient poor, but it is often aerated, and thus still
somew hat beneficial to tree growth. In poorly to very poorly
drained depressional sites the water stagnates and is deleterious
to biological production. Most saturated conditions are due to
perched water tables or a combination of perched and true
groundwater.
Solum development is usually quite deep, 50 to 100 cm,
however, only the upper 30 to 50 cm is adequately friable to be
considered potential rooting zone. The common horizon
sequence in moderately well drained profiles is LFH, Ae1, Bf,
Ae2, (II)Bt and (II)C. The Ae2 horizon is created by lateral
flow leaching. Imperfectly drained sites have a similar
sequence but with distinct mottling in the upper 50 cm and
prominent greyish streaks in the lower (Bt and C) horizons.
Poorly to very poorly drained profiles have horizon sequences
of LFH or O, Aeg, Bg, (II)Btg and (II)Cg, or, LFH or O, Aeg,
Bgf, (II)Btg and (II)Cg. Shallow rooting, especially on ill
drained sites, makes trees susceptible to windthrow.
Hummocky micro topographies and irregular, broken soil
horizons result. The Stony Brook texture profile consists of a
loam to sandy loam upper solum over a loam to clay loam or
sandy clay loam lower solum and subsoil. Inwashed fines tend
to make soils in receiving sites slightly heavier textured.
Profile coarse fragment content averages 10 to 25%. Most are
subangular to flat, cobbles and gravels, but with some stones,
of weathered fine- to medium-grained Pennsylvanian
grey-green sandstone. In deposits that are two tiered, i.e.,
ablational till over lodgment till, coarse fragments may be
concentrated along the interface. These are referred to as
“stone lines”. Stony Brook soils are derived from parent rocks
that weather moderately rapidly but yield materials that are low
in natural fertility. The profile is acidic throughout, pH (H 2O)
4.0 to 5.5. Moderately well drained soils consist of a yellowish
brown to reddish brown upper solum over characteristically
reddish brown Bt and C horizons. The Ae1 horizon is friable,
weak, fine platy. It overlies a 15 to 35 cm thick, very friable,
weak to moderate, fine granular Bf/Bfj horizon. The Ae2
horizon is weakly leached, friable, fine platy and often faintly
mottled. The Bt and C horizons are firm to very firm and
usually moderate, coarse platy, a structure inherited from the
parent material. Transition of the Bt horizon into the C
horizon is gradual. Poorly drained materials are gleyed in the
upper horizons but the reddish coloured parent material
persists in spite of reducing conditions. They also have
thicker, 10 to 25 cm, surface organic layers.
87
that limit crop production. Relatively low levels of natural
fertility restrict forest productivity.
Summary of general characteristics of the Stony Brook Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
Figure 57. Moderately well drained Stony Brook soil profile.
Stony Brook soils share the Maritime Plain portion of the map
area with other soils developed on morainal tills, the Reece,
Rogersville and Sunbury associations. Stony Brook soils are
readily differentiated based on their red to reddish brown
coloured subsoils. Reece subsoils are yellowish brown and
slightly lighter textured.
Rogersville subsoils may be
somewhat reddish brown along soil transitional boundaries, but
they are dominated by non-sandstone rock types such as
granites, gneiss, schists and volcanics. Sunbury soils are
readily differentiated from Stony Brook soils. Their subsoils
are yellowish brown, much coarser textured, and noncompact.
Some Stony Brook soils are mapped with Barrieau-Buctouche
soils in areas along the coast where sandy marine deposits of
varying thickness overly the lodgment till. Poorly drained
Stony Brook soils are often associated with organic soils,
Lavillette and especially Acadie Siding. Organic soils have at
least 40 cm of organic debris. Mineral soils, such as poorly
drained Stony Brook, may have surface organic layers up to 40
cm thick, but more commonly, organic surface layers are less
than 20 cm thick.
Most uses of Stony Brook soils are affected by the low
permeability and undesirable structure of the subsoil. When
this condition is coupled with a lack of slope gradient and the
prevailing levels of precipitation and snow melt, it results in a
large percentage of Stony Brook soils with wetness problems
: SB
: Maritime Plain
: 40-120 m
: 151,867 ha
: 5.45%
: Mineral
: Glacial till, compact
: 1-2 m
: Red to reddish brown
: Fine loamy
: Soft gray-green sandstone and weathered
shale
: Low
: Undulating and level (0.5-5%)
: Imperfect
:Gleyed Podzolic Gray Luvisol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 40
40 - 100+
Texture Class
Loam - sandy loam
Clay loam - loam sandy clay loam
% Sand
45
42
% Silt
35
30
% Clay
20
28
% Coarse
Fragments
10 subangular C/G
20 subangular C/G
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.15
1.80
Ksat (cm/hr)
>5
< 0.1
AWHC (cm/cm)
0.15 - 0.20
< 0.10
St. Quentin Association
St. Quentin soils consist of peat materials found in swamps
formed from forest vegetation on poorly to very poorly drained
sites. They are the result of a gradual building up process
where the water table is near the surface and organic debris
accumulates They consist of relatively thin peatland deposits,
averaging less than 2 m in thickness. The peat is composed of
wood, leaves, needles, feather mosses and other forest debris.
St. Quentin soils occur in the Chaleur Uplands portion of the
survey area (Fig. 58) on level to undulating landscapes with
slopes of less than 5%. Although they only account for 1,111
ha, representing less than 0.04% of the survey area, St.
Quentin soils often occur as unmapped inclusions in areas of
very poorly drained mineral soils.
Strong water movement from the deposit margins or from
88
mineral soils results in a nutrient-rich environment.
St.
Quentin peatlands usually have relatively level or flat surfaces.
Although peat depths are relatively uniform, they decrease in
depth from the centre of the deposit outwards. Pronounced
surface patterns are usually lacking with the exception of the
presence of intermittent to semi-permanent drainage courses.
Most deposits are topographically confined in depression-like
areas.
Vegetative cover consists of coniferous and deciduous trees,
tall shrubs, herbs and mosses. Tree cover is usually thick and
quite diversified as a result of the nutrient-rich groundwater.
Cedar, black spruce, trembling aspen, ash, red maple and alder
are comm on.
Terric phases of the above listed taxa.
St. Quentin soils are usually surrounded by very poorly to
poorly drained mineral soil members. Mineral soils occurring
in areas of calcareous bedrock, such as Caribou, Thibault and
Carleton, are likely associates. St. Quentin soils are
differentiated from mineral soils based on the depth of organic
material present. To be classed as St. Quentin a soil must have
at least 40 cm of mesic or humic organic material, otherwise it
is included with the appropriate mineral soil association.
St. Quentin soils have little potential use for agriculture. While
they support often impressive forest stands, St. Quentin soils
require highly specialized management to ensure sustainability.
They are easily damaged by harvesting operations.
Summary of general characteristics of the St. Quentin Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Degree of Decomposition
Botanical Composition
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: SQ
: Chaleur Uplands
: 300-600 m
: 1111 ha
: 0.04%
: Organic
: Swamps
: < 2 m over mineral soil
: Dark brown
: Moderately to very strongly decomposed
: Forest-fen peat
: High
: Flat, bowl and horizontal (<1%) in an
undulating landscape (<5%)
: Very poor
: Terric Mesisol or Terric Humisol
Figure 58. Location of mapped St. Quentin soils.
St. Quentin soils are dominated by forest peat that is generally
moderately to well decomposed, with a structureless or very
fine fibred structure, resulting in a slightly matted appearance.
The colour is dark brown or reddish brown to almost black, pH
greater than 5.5, and the peat material is in a mesic to humic
state of decomposition with a rubbed fibre content that
averages 10%. Von Post scale of decomposition is usually 6
to 8. Bulk density is high for a peat, being 0.1 to more than 0.2
g/cm 3. Saturated hydraulic conductivity is very slow at less
than 0.1 cm/hr. Coarse- to medium-sized woody fragments are
randomly distributed throughout. The layer of forest peat is
often underlain by a thin layer (less than 30 cm) of fen peat
derived from sedges. The underlying mineral material is
variable, usually being the predominate material in the
surrounding area.
Drainage is very poor. Water table levels are at or near the
surface throughout the year, resulting in ponding. Ground
water is neutral and of elevated nutrient status.
Where depth to the mineral soil contact is greater than 1.6 m,
St. Quentin soils are classified as either Typic or Mesic
Humisols, or as Typic or Humic Mesisols, depending upon
their degree of decomposition. St. Quentin soils having a
depth of 0.4-1.6 m to the mineral soil contact are classified as
Layer
Friable upper
soil material
Subsoil
material #1
Subsoil
material #2
Depth (cm)
0 - 30
30 - 150
> 150
Von Post
rating
2-4
6-8
-
% Wood
15
15
-
Texture Class
-
-
Sandy clay
loam
% Sand
-
-
60
% Silt
-
-
15
% Clay
-
-
25
% Coarse
Fragments
-
-
20 angular
G/C
pH (H2 O)
6.0 - 6.5
> 6.5
> 7.0
BD (g/cm3 )
0.10
0.20
1.80
Ksat (cm/hr)
10
< 0.1
< 0.1
AWHC
(cm/cm)
0.15
0.20
< 0.10
89
Sunbury Association
The Sunbury association consists of soils developed in
moderately thin (less than 2 m) deposits of acidic, coarse
loamy to sandy and frequently skeletal, noncompact, morainal
glacial till material (ablational till) with coarse fragments of
soft sandstone. Sunbury soils occur only on the Maritime Plain
or lowlands portion of the study area (Fig. 59). They are found
at elevations of 50 to 140 m above sea level. The Sunbury
ablational till material is underlain by either dense compact
basal (lodgment) till or lies directly on the bedrock. In veneer
phases the bedrock occurs within 1 metre of the surface. The
bedrock is horizontally bedded gray-green Pennsylvanian
sandstone dominated by quartz but with some feldspars and
lesser amounts of biotite, muscovite and chloride. The coarse
fragments within the profile have been derived from this
sandstone bedrock. Sunbury soils occupy approximately
102,477 ha or 3.68% of the map area.
Figure 59. Location of mapped Sunbury soils.
Ablational till is the accumulation of debris deposited from
glacial ice during down wasting or melting of the glacier.
Where Sunbury material has been deposited as end moraines
by dumping off the glacier margin as the ice melts, the till is
thicker, masking the underlying landform configuration with
hummocky or ridged mesotopography, but still maintaining the
undulating to gently rolling surface expression characteristic of
the lowlands plain. Slopes average 3 to 9%. Where down
wasting of glacial ice has been more rapid, thin layers of
Sunbury ablational till were deposited over large areas. Areas
of shallow (less than 1 m ) ablational till over bedrock are
mapped as Sunbury veneers. However, areas of similarly
shallow ablational till over lodgment till are assigned to the
appropriate lodgment till-derived soil association (usually
Reece or Stony Brook). Some Sunbury map units also occupy
steeply sloping positions along incised river channels, where
slopes commonly range from 9 to more than 15% and material
thickness is less than 1 metre over bedrock. Sunbury material
consists of nonstratified glacial drift with coarse fragments and
soil particles not sorted according to size or weight, but rather
lying in the random sequence in which they were released from
the melting ice. Materials consist of a heterogeneous mixture
of sand, silt, clay and coarse fragments ranging from gravels
and cobbles to stones and boulders. Most particles are angular
and sharp edged, but where fluvial action was more intense,
subrounded and even rounded coarse fragments occur.
Meltwaters have removed many of the fines (silt and clay)
leaving a matrix dominated by sand (greater than 60%).
Sunbury soils are usually very stony on the surface. Stones are
1 to 2 m apart and occupy 3 to 15% of the surface area.
Stoniness may vary greatly over a very short distance.
Boulders are present but usually not in significant quantities to
designate. Well drained Sunbury sites support stands of black
spruce, jack pine, balsam fir and some sugar maple, white
birch and beech. On ill-drained sites the jack pine-sugar
maple-beech component is superseded by red maple, yellow
birch, cedar and larch.
The Sunbury association is dominated by well to moderately
well drained Orthic Hum o-Ferric Podzols (Fig. 60).
Podzolization is strongly expressed, even in sites that are less
than well drained. Imperfectly drained sites are Gleyed
Humo-Ferric Podzols. Poorly to very poorly drained sites are
Gleyed Humo-Ferric Podzols, Gleyed Eluviated Dystric
Brunisols or Orthic Gleysols, depending upon the degree of
impeded drainage. Internal drainage is excellent. The profile
consists of a very rapidly permeable solum over a rapidly
permeable subsoil. Saturated hydraulic conductivity values are
greater than 5 cm/hr throughout the profile. Available water
storage capacity ranges from less than 0.10 to 0.15 cm/cm, the
higher values being in the solum where finer textures and
organic matter contents enhance moisture retention. On well
drained sites precipitation is the sole source of water. Excess
water flows downward into the underlying subsoil.
Imperfectly and poorly drained sites are the results of high
water tables. Poorly drained sites are restricted to depressional
or stream channel locations. They are typically associated with
well and imperfectly drained Sunbury soils but seldom occupy
a large enough area to be designated in the map unit.
Solum development in Sunbury soils varies from 35 to 55 cm
in thickness. The common horizon sequence is: LFH, Ae, Bf,
BC and C on well to moderately well drained sites; LFH or O,
Ae, Bfgj, BCgj or BCg and Cg on imperfectly or poorly
drained sites; and LFH or O, Ae, Bmgj, BCg and Cg, or LFH
or O, Aeg, Bg and Cg on poorly or very poorly drained sites.
The upper horizons in poorly drained sites are often
discontinuous because of uprooting of trees due to windthrow,
resulting in mounded micro topography. Most Sunbury soils
are below the maximum level of post-glacial marine
submergence (approximately 140 m asl). However, little or no
evidence remains to identify this event. Soil formation has
obliterated any surficial modification that may have resulted
from marine submergence. Soil textures grade from a gravelly
or cobbly sandy loam solum into a cobbly or stony sandy loam
to loamy sand subsoil. Coarse fragment content increases with
depth. It ranges from 15 to 35% but may be as high as 60% in
some shallow lithic phases. Most coarse fragments are either
channers or flagstones, but with some angular or irregular
cobbles and stones. They are derived from soft gray-green
90
and consistence. They are reddish brown, fine loamy and firm
to very firm. Reece soils may be identical to Sunbury soils in
the colour (yellowish brown to brown) and morphological
appearance. They differ in subsoil characteristics. Reece
subsoil is fine loamy and compact (firm to very firm), whereas
Sunbury subsoil is coarse loamy and friable. Guimond River
soils are similar in composition to Sunbury soils, but they have
stratified water-worked (rounded) sediments in comparison to
the heterogenous, angular nature of Sunbury rock fragments.
Excessive stoniness and low available water holding capacity
are the major limitations to agriculture, especially the
stoniness. Some of the more strongly sloping Sunbury
landscapes would also be a hindrance to the usage of
agricultural equipment. Forestry uses are impacted by low
natural fertility and droughtiness. Species selection must
consider these two limitations.
Summary of general characteristics of the Sunbury Association
Figure 60. Well drained Sunbury soil profile.
Pennsylvanian sandstone. This thin, flat "channer-flagstone"
shape is inherited from the sandstone which splits readily and
uniformly along bedding planes or joints. The sandstone is
soft and highly weathered, rating less than 4 on the Mohs scale.
It is dominated by quartz (60-80%) but with significant
feldspars (10-30%) and biotite and muscovite (5-10%).
Sunbury soils are low in natural fertility, especially
exchangeable calcium and magnesium. The profile is acidic
throughout, ranging from pH(H 2O) 4.0 to 5.5 . In well drained
soils the parent material is yellowish brown to brown.
Typically the mineral soil profile consists of a grayish, friable,
weak, fine platy Ae horizon over a yellowish red to yellowish
brown, very friable, weak to moderately fine granular Bf
horizon which merges gradually into the friable, very weak,
subangular blocky to structureless BC and then C. Mottles
and grayish gley colours modify the profile morphology in
imperfectly and poorly drained sites. However, only under the
very wettest of conditions is the general podzolic sequence not
present. Occasionally, ortstein has formed in the solum,
resulting in a compact, very firm, massive B horizon. The
ortstein is an irreversible, but discontinuous hardpan cemented
by Fe, Al and organic complexes. It impedes downward
movement of water and is a barrier to root growth, but the
intermittent nature of its development is such that it does not
significantly impact land use.
Sunbury association soils are most intimately associated with
Reece soils, and to a lesser extent, Stony Brook soils. All three
associations occur on the eastern Maritime Plain. Reece and
Stony Brook soils often have a surficial capping of Sunbury
material. Stony Brook soils are readily differentiated from
Sunbury soils on the basis of parent material colour, texture
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: SN
: Maritime Plain
: 50-140 m
: 102,477 ha
: 3.68%
: Mineral
: Glacial till, noncompact
:<2m
: Yellowish brown to brown
: Coarse loamy to sandy (skeletal)
: Soft gray-green sandstone
: Low
: Undulating to gently rolling (3-9%)
: Well
: Orthic Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Sandy loam
Sandy loam - loamy
sand
% Sand
70
75
% Silt
15
15
% Clay
15
10
% Coarse
Fragments
20 flat, subangular
C/S/G
30 flat, subangular
C/S/G
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.10
1.50
Ksat (cm/hr)
> 25
> 10
AWHC (cm/cm)
0.10 - 0.15
< 0.10
91
Tetagouche Association
The Tetagouche association consists of soils that have
developed in acidic, fine loamy, compact morainal till derived
from metagabbro, metabasalt, metagreywacke and some
conglomerate. Deposits are mostly less than 2 m thick
(veneers and blankets) but some deeper phases also occur
(greater than 3 m thick). Tetagouche soils are mostly located
in the northern portion of the Chaleur Uplands portion of the
study area at elevations between 100 and 500 m above sea
level (Fig. 61). They occupy approximately 18,079 ha,
representing 0.65% of the map area.
Figure 61. Location of mapped Tetagouche soils.
The soil parent material has been deposited as ground moraine,
plastered in place under the weight of advancing glacial ice.
Composition strongly reflects the incorporation of local
bedrock formations composed largely of dark-coloured, basic,
fine-grained volcanics. Coarse fragment content is higher
where weathered bedrock has been incorporated into thin
veneer sediments. Tetagouche soils are very stony on the
surface, with 3 to 15% of the land area occupied by coarse
fragments. Boulders may be present, but not in sufficient
quantities to warrant designation as a bouldery phase.
Tetagouche landforms range from undulating to rolling surface
expressions with slopes of 2 to 9%, to some ridged and hilly
map units with slopes of in excess of 45%. Although thin, the
soils are relatively uniform in thickness and bedrock outcrops
are not common enough to warrant a rocky designation. Those
bedrock exposures that do occur are found on topographic
highs and summits or along steeply inclined drainage channels
that are more deeply incised into the bedrock. Well drained
soils of the Tetagouche association support forest communities
of mixed softwood-hardwood forest cover type consisting of
yellow birch, cedar, spruce, balsam fir, sugar maple, beech, red
oak, white birch, white pine and striped maple. Poorly to very
poorly drained members are dominated by cedar, black spruce,
balsam fir, white birch, red maple, speckled alder and willows.
Well to moderately well drained Tetagouche association soils
are Orthic Humo-Ferric Podzols but with some Orthic FerroHumic Podzols. Imperfectly drained sites are classified as
Gleyed Humo-Ferric Podzols, indicating the presence of
mottling and/or gleying. Poorly to very poorly drained sites
are typically Orthic Gleysols but may have some inclusions of
Fera Gleysols. Imperfectly and poorly to very poorly drained
sites dominate the undulating and gently rolling landscapes.
Well to moderately well drained Tetagouche soils usually
occur as significant components in more steeply sloping
landscapes dominated by other soil types. Internal drainage is
restricted by a slowly to very slowly permeable subsoil with an
estimated saturated hydraulic conductivity value of less than
0.2 cm/hr. Available water storage capacity ranges from 0.25
to less than 0.10 cm/cm, decreasing with depth because of
reduced total porosity in the compact subsoil. Downward
movement of excess moisture through the profile is impeded
by the subsoil and lateral flow or seepage occurs along the
subsoil surface. Imperfectly and poorly to very poorly drained
areas are strongly affected by seepage. Topographic position,
lack of gradient, and high groundwater table also play a role.
Soil development is relatively thin, with solums ranging from
35 to 55 cm. The common horizon sequence on well drained
sites is LFH, Ae, Bhf, Bf, Btj or BC and C. The organic layer
is 3 to 10 cm thick, becoming more humified with depth. It
overlies a thin (2 to 5 cm), light brownish gray coloured Ae
horizon which breaks abruptly into the B horizon. The brown
to dark brown Bhf horizon varies from 3 to 12 cm in thickness.
It is thickest in the colder regions of the central New
Brunswick Highlands. The Bhf horizon merges with a
yellowish brown Bf horizon. At 35 to 45 cm the podzolic B
horizon grades into a weakly developed Btj or BC horizon .
Clay translocation from the upper solum results in the
presence of a weak Btj horizon. The Btj or BC horizon has a
very weak, coarse subangular blocky structure and is resistant
to both root and water penetration. These transitional horizons
are similar to the subsoil in terms of their compact consistence.
They gradually grade into the unaltered parent material or C
horizon. Imperfectly drained soils have similar profiles but
are modified by periodic saturation. They are mottled and
gleyed in the B and C horizons. An Ahe horizon up to 5 cm
thick may be sandwiched between the H and Ae horizons in
imperfectly drained Tetagouche soils. The Ahe horizon
formation is at the expense of the Bhf horizon formation,
which is very thin or nonexistent. Poorly to very poorly
drained horizon sequences typically consist of LFH or O, Aeg,
Bg, Btjg or BCg, and Cg horizons. The forest duff layer is
thicker in the poorly and very poorly drained conditions than
found in well drained counterparts, varying from 5 to 15 cm,
but occasionally as thick as 30 cm. The Tetagouche textural
profile usually consists of a loam surface grading into a heavy
loam to clay loam subsoil. Clay content is usually highest in
the subsoil and also tends to increase as drainage becomes
poorer. Profile coarse fragment content varies from 10 to 25%.
Subangular gravels and cobbles dominate. Tetagouche soils
are medium in inherent fertility owing to the nature of the rock
types from which they have been derived. The soils are acidic
throughout, with pH(H 2O) values of 4.0 to 5.5. The friable,
weak to moderate, fine to medium, granular or subangular
92
blocky solum provides an available rooting zone of
approximately 45 cm. The underlying parent material is firm
to very firm, massive or pseudoplaty, the pseudoplatiness a
result of its having been plastered into place by glacial ice.
Tetagouche soils have been mapped in association with other
till soils that have igneous lithology - Tetagouche Falls,
Nigadoo River and Popple Depot. The Nigadoo River
association has the same lithology and dense compact subsoil,
but it is coarser-textured. The Tetagouche Falls association has
the same lithology and similar textural profile, but it has a
relatively friable, non-compact subsoil. Popple Depot has
developed on a compact basal till, but of different rock types
that are more quartz-based. Popple Depot is also coarse-loamy
in texture. Tetagouche soils have been mapped with
Catamaran, McGee, Long Lake and Violette in some
transitional areas between different bedrock formations. The
latter mentioned soils have developed from metasedimentary
bedrock types.
Ksat (cm/hr)
>5
< 0.2
AWHC (cm/cm)
0.20
0.10
Tetagouche Falls Association
The Tetagouche Falls association consists of soils that have
developed in acidic, loamy, non-compact morainal till derived
from metagabbro, metabasalt, metagreywacke and some
conglomerate. Essentially, Tetagouche Falls soils are noncompact Tetagouche or Nigadoo River soils. Deposits range
in thickness from veneers of less than 1 m thick to deeper
phases of greater than 3 m thickness. Tetagouche Falls soils
are scattered throughout the New Brunswick Highlands and
Chaleur Uplands portions of the study area at elevations
between 50 and 600 m above sea level (Fig. 62). They occupy
approximately 48,940 ha, representing some 1.76% of the
map area.
The primary limitations affecting land use of Tetagouche soils
are coarse fragment content (both surface and profile), soil
drainage and shallowness to a compact subsoil layer. Medium
inherent fertility, however, is an asset to forest production.
Summary of general characteristics of the Tetagouche Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: TT
: Chaleur Uplands
: 100-500 m
: 18,079 ha
: 0.65%
: Mineral
: Glacial till, compact
: < 2-3 m
: Strong brown
: Fine loamy
: Metagabbro, metabasalt, metagreywacke
and conglomerate
: Medium
: Undulating and rolling to ridged and hilly
(2-45%)
: Moderately well
:Orthic Humo-Ferric Podzol and Orthic
Ferro- Humic Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Loam
Loam - clay loam
% Sand
45
40
% Silt
35
35
% Clay
20
25
% Coarse
Fragments
10 subangular G/C
20 subangular G/C
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.15
1.80
Figure 62. Location of mapped Tetagouche Falls soils.
Tetagouche Falls soil parent material is non-compact and as
such is considered to be an ablational till, however, some
firmness may occur in the subsoil. The somewhat firm
consistence of the subsoil can be attributed to the composition
of the parent material in that it is loamy and acidic. The acidic
nature of the subsoil does not promote soil formation physical
and biochemical processes that favour the development and
stabilization of soil structure.
Tetagouche Falls soils have subangular coarse fragments
derived mostly from the underlying mafic volcanic bedrock.
The soil surface is typically very stony, with 3 to 15% of the
land surface occupied by coarse fragments. Well drained
Tetagouche Falls soils have developed under a mixed
softwood-hardwood forest cover type consisting of yellow
birch, cedar, spruce, balsam fir, sugar maple, beech, red oak,
white birch, white pine and striped maple. Poorly to very
93
poorly drained members are dominated by cedar, black spruce,
balsam fir, white birch, red maple, speckled alder and willows.
Well to moderately well drained soils of the Tetagouche Falls
association are either Orthic Humo-Ferric Podzols or Orthic
Ferro-Humic Podzols (Fig. 63). Imperfectly drained sites are
classified as Gleyed Humo-Ferric Podzols, indicating varying
oxidizing/reducing conditions due to periodic saturation.
Poorly to very poorly drained sites are typically Orthic
Gleysols but may have some inclusions of Fera Gleysols.
Poorly and very poorly drained sites are usually restricted to
localized areas such as drainage channels and small
depressions in landscapes dominated by well to moderately
well drained soils. Tetagouche Falls soils have moderately
rapid to moderate internal drainage. The upper solum usually
has moderately rapid permeability (5 to 15 cm/hr saturated
hydraulic conductivity) and the subsoil has moderate to
moderately slow permeability (2 to 3 cm/hr). Available
moisture storage capacity exceeds 0.15 cm/cm throughout the
profile and is greatest in the upper solum (0.20 to 0.25 cm/cm).
Well drained sites are supplied with moisture through
precipitation. In shallow to bedrock moderately well and
imperfectly drained sites, precipitation may be augmented with
some lateral flow or seepage along the bedrock interface.
Poorly to very poorly drained sites occur only because of high
groundwater levels. The soil parent material and underlying
bedrock is relatively rich in nutrients and so seepage waters are
beneficial to plant growth.
Soil development is relatively thin, with solums ranging from
35 to 55 cm. The common horizon sequence on well drained
sites is LFH, Ae, Bhf, Bf, BC and C. The organic layer is 3 to
10 cm thick, becoming more humified with depth. It overlies
a thin (2 to 5 cm), light brownish gray coloured Ae horizon
which breaks abruptly into the B horizon. The upper B
horizon consists of a brown to dark brown Bhf horizon 3 to 15
cm in thickness. The Bhf horizon merges with a yellowish
brown Bf horizon. At 35 to 45 cm the podzolic B horizon
grades into a BC horizon w hich then grades into the unaltered
strong brown coloured parent material or C horizon.
Imperfectly drained soils have similar profiles but are modified
by periodic saturation. They are mottled and gleyed in the B
and C horizons. An Ahe horizon up to 5 cm thick may be
sandwiched between the H and Ae horizons in imperfectly
drained Tetagouche Falls soils. The Ahe horizon formation is
at the expense of the Bhf horizon formation, which is very thin
or nonexistent. Poorly to very poorly drained horizon
sequences typically consist of LFH or O, Aeg, Bg, BCg, and
Cg horizons. The forest duff layer is thicker in the poorly and
very poorly drained conditions than found in well drained
counterparts, varying from 5 to 15 cm, but occasionally as
thick as 30 cm. The Tetagouche Falls textural profile usually
consists of a loam to sandy loam surface grading into a loam
subsoil. Clay content is typically around 18% in the subsoil
but tends to be higher in poorly drained sites than in well
drained sites due to inwashing of fines. Profile coarse
fragment content varies from 15 to 35%. Subangular gravels
and cobbles dominate. Tetagouche Falls soils are medium in
inherent fertility owing to the nature of the rock types from
Figure 63. Well drained Tetagouche Falls soil profile.
which they have been derived. The soils are acidic throughout,
with pH(H 2O) values of 4.0 to 5.5. The friable to very friable,
weak to moderate, fine to medium, granular or subangular
blocky solum grades into a slightly firm weak, medium
subangular blocky subsoil.
Tetagouche Falls soils have been mapped in association with
other till soils that have igneous lithology - Tetagouche,
Nigadoo River, Juniper, Popple Depot and Jacquet River. The
Nigadoo River association has the same lithology but is
slightly coarser-textured and has a very dense compact subsoil.
Juniper, Popple Depot and Jacquet River are all derived from
different rock types that are more quartz-based. All three soils
are also slightly coarser textured, being coarse loamy
compared to Tetagouche Falls which is loamy. Popple Depot
soils also have dense compact subsoils. Tetagouche soils have
developed from the same bedrock sources, but they are slightly
finer textured and have compact subsoils. Tetagouche Falls
soils have also been mapped with Boston Brook, Catamaran,
94
McGee, Long Lake and Thibault in some transitional areas
between different bedrock formations. The latter mentioned
soils have developed from sedimentary and metasedimentary
bedrock types.
The primary limitations affecting land use of Tetagouche Falls
soils are coarse fragment content (both surface and profile) and
topographic conditions (excessive slope). Medium inherent
fertility, however, is an asset to forest production.
morainal material that is the result of either ablational
deposition, periglacial and other reworking of lodgment till, or
residual development, alone or in combination.
The
underlying Devonian, Silurian and/or Ordovician age bedrock
types are easily weathered. Thibault soils occupy
approximately 138,569 ha, representing 4.97% of the map
area.
Summary of general characteristics of the Tetagouche Falls Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: TF
: Chaleur Uplands
: 50-600 m
: 48,940 ha
: 1.76%
: Mineral
: Glacial till, noncompact
: <1 - >3 m
: Strong brown
: Loamy
: Metagabbro, metabasalt, metagreywacke
and conglomerate
: Medium
: Rolling and ridged to hilly (5-70%)
: Well
: Orthic Humo-Ferric Podzol and Orthic
Ferro-Humic Podzol
Figure 64. Location of mapped Thibault soils.
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 45
45 - 100+
Texture Class
Loam - sandy loam
Loam
% Sand
50
47
% Silt
35
35
% Clay
15
18
% Coarse
Fragments
20 subangular C/G
30 subangular C/G
pH (H2 O)
4.5 - 5.0
4.5 - 5.5
BD (g/cm )
1.10
1.55
Ksat (cm/hr)
5 - 15
2-3
AWHC (cm/cm)
0.20 - 0.25
0.20
3
Thibault Association
The Thibault association consists of soils that have developed
in thin (less than 2 m thick) deposits of neutral to slightly
acidic, coarse loamy non-compact morainal till derived from
weakly calcareous shale, slate, quartzite, argillite and
sandstone. Thibault soils occur mostly in the Chaleur
Highlands physiographic region, and to a lesser extent in the
Notre Dame Mountains, at elevations of 250 to 550 m above
sea level (Fig. 64). They have formed in loose, noncompact
Although Thibault soil parent material is the end product of a
number of different processes, it is relatively uniform in
composition. Either as a result of deposition or development,
it consist of a friable medium. Interstitial fines have been
removed from the soil matrix by washing. High coarse
fragment contents (10 to 35%) prevail because of the fractured
bedrock component that has been incorporated into the profile
as a result of either glacial process or periglacial frost heaving.
The parent rock types produce a characteristic flat, channery or
flaggy clast shape. Thibault soils have moderately stony to
very stony land surfaces with 2 to 15% of the surface occupied
by stone sized clasts. Surface channers and flaggs are also
abundant. The topographic conditions under which Thibault
soils occur very considerably. They include undulating (2 to
5% slope), rolling (5 to 15% slope), ridged (5 to 15% slope),
hilly (15 to 45% slope), and sloping (15 to 70% slope) surface
expressions. Veneers, with less than 1 m of regolith over the
bedrock, are associated with the ridged, hilly and sloping
landforms. Rocky phases of the Thibault soils are abundant in
sloping map units where stream channels are deeply incised
into the landscape. Scattered rock outcrops also occur along
ridge or hill tops where more resistant bedrock strata persist.
Thicker deposits are associated with areas of undulating and
gently rolling topography where slopes are longer and less
dissected. Here, the till overburden tends to be more uniform
in thickness and bedrock outcrops are not common. Native
vegetation on well drained Thibault soils is a diverse
softwood-hardwood forest composed of black and red spruce,
balsam fir, white and yellow birch and sugar and red maple.
Less prolific species include white cedar, trembling aspen,
striped maple, mountain ash and beech. Vegetation on poorly
95
drained sites consists of such water tolerant trees as black
spruce, balsam fir, white cedar, red maple and speckled alder.
Moderately sloping landscapes combined with coarse loamy
particle size class and the open, porous nature of the subsoil,
result in a high proportion of Thibault soils being well drained.
The Thibault association is dominated by well drained Orthic
Humo-Ferric Podzols (Fig. 65). Imperfectly drained Gleyed
Humo-Ferric Podzolic Thibault soils are often intermixed with
their well drained counterparts on rolling or ridged topography.
They occupy segments of the landscapes where natural
drainage is impeded ie. lower slopes, depressions, etc. Poorly
drained members of the Thibault association are Orthic or Fera
Gleysols. They occur as predictable inclusions in most map
units but are usually restricted to narrow zones along drainage
ways or confined to depressions. Internal drainage in Thibault
soil material is good. The subsoil has 30 to 40% total pore
space of which more than one third is macropores. Based on
this pore size distribution, the subsoil has an estimated
permeability of moderate to moderately rapid (2.5 to 10 cm/hr
saturated hydraulic conductivity). Available water storage
capacity decreases with depth from greater than 0.25 cm/cm in
the solum to 0.15 cm/cm in the subsoil. On well drained sites
precipitation is the sole source of water supply. Excess water
flows through the profile and into the underlying verticallystanding, fractured bedrock. Impeded drainage conditions
Figure 65. Well drained Thibault soil profile.
conditions (imperfect and poor) are the result of high
groundwater levels. Intermittent springs also occur where
groundwater is forced onto the land surface by a buildup of
underground hydraulic pressures because of gravitational water
seepage along bedrock fracture planes.
Profile development averages 40 to 60 cm in thickness. The
common horizon sequence in well drained profiles is: LFH,
Ae, Bhf (discontinuous), Bf, BC, and C. The soils generally
have a thin organic layer 2 to 6 cm thick dominated by L and
F horizons. In some profiles soil fauna have complexed the
colloidal humus with the mineral soil forming a transitional
dark gray to black, porous crumbly Ah horizon. The
underlying light grayish coloured Ae horizon is 3 to 8 cm thick
but exceeds 15 cm in some pockets where tree-throw has
disturbed the solum pattern. Transition from the A to the B
horizon is abrupt. The 25 to 35 cm thick B horizon is a strong
brown colour along the upper boundary, becoming
progressively yellower with depth. It consists of a thin
discontinuous Bhf horizon overlaying a Bf horizon.
Podzolization is not as strongly developed as in more acidic
parent materials such as the McG ee association. In the weakly
calcareous Thibault parent material, initiation of podzolic
horizon formation was delayed until the carbonates had been
leached from the upper part of the soil. Subsequently, Thibault
soils are not always podzolized to the same degree as adjacent
soils that have developed in acidic parent materials. The
Thibault B horizon is, however, a well developed podzolic Bf.
The Bf horizon grades into a pale brown to light olive brown
coloured BC and then C. Imperfectly drained profiles have a
similar horizon sequence but are characterized by greyer
colours or distinct to prominent mottling indicative of periodic
reduction. Both the organic and A e horizons are also usually
thicker. Poorly drained soils consist of the following horizons:
LFH, Aeg, Bg or Bgf, and Cg. Peaty phases are common
where organic debris has accumulated to a thickness of greater
than 15 cm. Mineral soil matrix colours are dull and subdued
making differentiation of horizons difficult, especially where
the sequence is Aeg, Bg, and Cg. Where present, the Bfg
horizon is readily identifiable on the basis of prominent orange
mottles. The Thibault textural profile varies from a loam-silt
loam to a sandy loam. Silt plus clay content decreases from
the surface downwards, indicative of the effects of weathering
on soil particle size. This is particularly true of the Ae horizon
which is highest in silt-plus-clay content. Imperfectly and
poorly drained Thibault soils usually contain more fines in the
solum than do their well drained counterparts. This is
attributed to a combination of the inwashing of silt and clay
from adjacent upland positions and the more pronounced
influence of physical disintegration by frost action in water
saturated conditions. Profile coarse fragment content averages
10 to 35% channers and flaggs. In lithic phases this may
exceed 60 to 70% along the soil bedrock contact where in situ
formation has taken place and the coarse fragments retain the
vertically standing orientation of the bedrock. The weakly
calcareous shale, slate, quartzite, argillite and sandstone parent
rock is moderately rich in nutrients and weathers rapidly to
release these nutrient elements into the soil. However, much of
the exchangeable calcium and magnesium has been lost by
96
leaching and the soil has gradually become more acidic. Soil
reaction (pH in water) is less than 5.5 throughout the solum but
the parent material has retained a weakly neutral status (pH
greater than 5.5). Availability of plant nutrients how ever, is
restricted by soil acidity, thus negating some of the benefits of
the Thibault inherent fertility. In poorly drained conditions
inwashed bases often enhance the profile nutrient content and
increase the pH. There are no physically impeding layers
within the profile to restrict plant roots. The solum is moderate,
medium, granular and friable. Subsoil conditions vary with
drainage. Well drained sites are usually friable and weak, fine
granular to subangular blocky, but as drainage conditions
worsen, the subsoil becomes slightly firm and very weakly
structured to amorphous. The amorphous nature of the Cg
horizon in imperfectly and poorly drained soils reduces
percolation rates but is not considered to be a major factor in
determining drainage.
Thibault soils have been mapped in complex units with
Carleton, Caribou, Holmesville and McGee soils and
occasionally Jacquet River, Nigadoo River, Long Lake,
Tetagouche Falls and Violette soils. Thibault, Caribou and
Carleton soil associations have all developed on parent
materials derived from weakly calcareous sedimentary or
metasedimentary bedrocks. Both Caribou and Carleton are
fine-loamy materials in contrast with Thibault, which is coarseloamy. Carleton soils also have dense compact subsoils. The
McGee association is probably the most similar to the Thibault
association in terms of soil physical and morphological
characteristics. Both soils have developed on non-compact
coarse-loamy olive brown-coloured till materials. However,
while Thibault soils have been derived from
weakly
calcareous shale, slate, quartzite, argillite and sandstone parent
rocks, McGee soils have been derived from acidic slates,
argillite, schist, greywacke and quartzite. Holmesville soils,
although mapped in complexes with Thibault soils, are quite
different, having developed on lodgm ent till material.
Holmesville soils are very compact in the subsoil.
Land use of Thibault soils is restricted by topographic
conditions (excess slope), shallowness to bedrock, stoniness
and to a lesser degree by excess moisture. Where thicker
deposits occur on areas of moderate relief, Thibault soils have
very good potential for growing agricultural crops climatically
suited to the region. Thibault soils are considered highly
suitable for forestry because of their inherent fertility, good
moisture holding capacity and deep available rooting zone.
Summary of general characteristics of the Thibault Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
: TH
: Chaleur Uplands, Notre Dame Mountains
: 250-550 m
: 138,569 ha
: 4.97%
: Mineral
: Glacial till, noncompact
:<2m
: Light olive brown
: Coarse loamy
: Weakly calcareous shale, slate, quartzite,
argillite and sandstone
Inherent Fertility
Topography (slope)
: High
: Undulating and rolling to ridged, hilly and
sloping (2-70%)
: Well
: Orthic Humo-Ferric Podzol
Drainage (dominant)
Classification (typical)
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 50
50 - 100+
Texture Class
Loam - silt loam
Loam - sandy loam
% Sand
40
50
% Silt
40
38
% Clay
20
12
% Coarse
Fragments
10 flat C/S/G
25 flat C/S/G
pH (H2 O)
4.5 - 5.5
> 5.5
BD (g/cm3 )
1.10
1.50
Ksat (cm/hr)
> 10
2.5 - 10
AWHC (cm/cm)
0.20 - 0.25
0.15 - 0.20
Tracadie Association
The Tracadie association consists of soils that have developed
in moderately thin (1 to 2 m) to very thick (sometimes in
excess of 20 m) deposits of neutral, clayey marine and
glaciolacustrine sediments. Gauthier (1983) recorded up to
100 m of marine clay in the subsurface of the Bathurst Basin.
Well logs also indicate significantly thick deposits along other
tidal river valleys, however, most occurrences are patchy and
not nearly so thick. Tracadie soils are confined to the coastal
margins of the Maritime Plain, but with some occurrences
along Chaleur Bay in the New Brunswick Highlands
physiographic region of the study area (Fig. 66). They are
mostly at elevations of less than 50 m above sea level.
Tracadie soils cover approximately 15,590 ha, or about
0.56% of the map area.
Tracadie parent materials are marine or glaciolacustrine
sediments, mostly silt and clay. They were deposited in a
brackish, shallow water environment during postglacial marine
submergence and subsequently exposed when water levels
receded. Tracadie sediments have been derived from mixed
undifferentiated lithologies. They are rich in mica-illite and
chloride. Tracadie soil particles are well worn and weathered,
first by stream flow, then by ocean forces, and finally, upon
emergence, by soil forming factors. Most land surfaces are flat
to very gently undulating, with less than 2% slope, and
uniform, seldom interrupted by irregularities in topography.
Valley depositions may have more relief, conforming to
pre-sedimentation structures and further modified by
post-sedimentation erosion. Vegetative cover consists of water
97
tolerant species such as black spruce, cedar, tamarack, red
maple, trembling aspen and alder.
structured Bt horizon which grades into the parent material
some 70 to 120 cm below the mineral soil surface.
Immediately above the Bt horizon is a thin 3 to 10 cm thick,
leached layer. The Bt and C horizons are typically pseudo
platy, a structure inherited from the mode of deposition.
Varving, the bedded or laminated annual sequence of
deposition found in ponded freshwater, is present in varying
degrees, indicative of the "brackish water" environment.
Parent material colour varies from red to yellowish brown.
Poorly to very poorly drained profiles usually have the
following horizon arrangement: LFH or O, Aeg, Bg, Btg, and
Cg. A thin (less than 10 cm thick) Ah horizon may be present
at the organic-mineral soil interface. Prominent gray and
brown streaks occur along vertical cracks associated with the
prismatic structure of the Bt horizon.
Figure 66. Location of mapped Tracadie soils.
The Tracadie association is dominated by imperfectly drained
Gleyed Gray Luvisols and Gleyed Brunisolic Grey Luvisols.
These profiles are characterized by the combination of clay
accumulation in the B horizon (Bt) and moderate to strong
mottling and gley features. Moderately well drained sites are
insignificant in areal extent. They occur as inclusions in map
units dominated by either imperfectly or poorly drained
members. Where they do occur they are classified as either
Orthic Gray Luvisols or Brunisolic Gray Luvisols. Poorly and
very poorly drained Tracadie soils are Orthic Luvic Gleysols
(Fig. 67). Excess water is removed from the soil very slow ly
in relation to supply due to the low perviousness of the subsoil
(saturated hydraulic conductivity of less than 0.1 cm/hr) and
the lack of gradient. Subsurface water flow, in addition to
precipitation, is the main source of water recharge. Perched
water tables are common when water supply (seepage,
snowmelt and precipitation) exceeds evapotranspiration.
Surface water flows away so slowly that free water often ponds
on the soil for a significant period of time. Available water
storage capacity is high (0.20 to 0.25 cm/cm) in the upper
solum (top 20 to 35 m) but relatively low (less than 0.10
cm/cm) below this, because of reduced total porosity.
Solum development may exceed 100 cm. This is the result of
deep Bt horizon formation. However, the available rooting
zone or friable portion of the solum seldom extends to a depth
of more than 35 cm, and is frequently less than 25 cm thick.
In imperfectly drained sites the common horizon sequence is
LFH, Ae, AB or Bm, Aegj, Btgj, Btg and Cg. The
organic-mineral soil contact is not always abrupt and there may
be a degraded Ah or Ahe horizon. The forest floor is usually
a thin layer of deciduous-coniferous and related organic debris.
The upper solum is friable. It consists of a well-developed
platy Ae horizon over a weak to moderate coarse granular to
fine subangular blocky AB or Bm. This is underlain by a firm
to very firm, moderate to strong, prismatic or angular blocky
Figure 67. Poorly drained Tracadie soil profile.
In red coloured deposits the upper solum horizonation is
particularly weakly expressed. Regardless of drainage, clay
accumulation in the B horizon is usually quite pronounced,
with moderately thick clay films in many voids and channels
and along most ped forces. The textural profile consists of a
loam to silty clay loam surface material over a (silty) clay loam
to silty clay or clay subsoil (Bt and C) Coarser textured
surface soils occur where a thin overburden of marine sand
98
was deposited and incorporated into the solum. In the subsoil
the combined silt plus clay content accounts for 80 to 95% of
the soil material. The percent clay range from 35 to 60%.
Discontinuous sand lenses are an associated feature. Most
Tracadie soils are free of coarse fragments, both within the
profile and on the surface. Those coarse fragments that do
occur are explained as being ice rafted debris. They consist of
mixed lithological types. Some inclusions of marine modified
glacial till or glacier reworked marine/lacustrine sediments
may tend to have higher coarse fragment content. Tracadie
soils are naturally moderately fertile, with high exchangeable
calcium and magnesium. However, leaching, due to prevailing
rainfall conditions, has removed many of these bases from the
upper profile, thus lowering the pH. Although the parent
material is neutral to strongly calcareous, the surface soil (Ae
and upper B) is strongly acidic with pH(H 2O) 5.0 to 5.5. Due
to its high clay content, the soil has a high cation exchange
capacity and thus a good ability to retain or hold nutrients.
Tracadie soils are commonly associated with other marine
deposited soil types, Richibucto and Belldune River.
Richibucto soils consist of marine sands, the textural opposite
of the Tracadie clays. In some areas the Richibucto sand is
underlain by Tracadie clays. The Belledune River soil is a
coarse loamy material with 20 to 50% gravels. These
properties readily differentiate it from the Tracadie association.
Organic soil formation is encouraged by the impeded drainage
conditions present in Tracadie soils. As a result, some poorly
to very poorly drained Tracadie soils are mapped in association
with Lavillette organic soils.
Use of Tracadie soils is affected by shallowness to a
root-restricting layer; high clay content, which enhances
nutrient retention and moisture holding capacities, but makes
the soil difficult to work; and poor internal permeability and
relatively level topography which make land drainage a
problem. Although they are nutrient-rich materials, ill-drained
conditions limit their use in forestry.
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 30
30 - 100+
Texture Class
Loam - silt clay
loam
Clay loam - silty clay
% Sand
30
15
% Silt
45
45
% Clay
25
40
% Coarse
Fragments
0
0
pH (H2 O)
5.0 - 5.5
> 6.5
BD (g/cm3 )
1.20
1.85
Ksat (cm/hr)
2-5
< 0.1
AWHC (cm/cm)
0.20 - 0.25
< 0.10
Tuadook Association
The Tuadook association consists of soils that have developed
in relatively thin (mostly less than 2 m thick) deposits of
acidic, coarse loamy, compact morainal till materials derived
from granite, granodiorite, diorite, granite gneiss and some
miscellaneous volcanics. They occur predominantly in the
central to southern portion of the New Brunswick Highlands
physiographic region at elevations of 300 to 700 m above sea
level (Fig. 68). Tuadook soils occupy approximately 82,171
ha, or 2.95% of the map area.
Summary of general characteristics of the Tracadie Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: TC
: Maritime Plain
: < 50 m
: 15,590 ha
: 0.56%
: Mineral
: Marine or glaciolacustrine
: Up to 20 m
: Red to yellowish brown
: Clayey
: Undifferentiated
: High
: Level to undulating (<2%)
: Imperfect
: Gleyed Gray Luvisol and Gleyed
Brunisolic Gray Luvisol
Figure 68. Location of mapped Tuadook soils.
The soil parent material has been deposited as ground moraine,
plastered in place under the weight of advancing glacial ice.
Composition strongly reflects the incorporation of local
bedrock formations. Thin mantles of ablational till may be
99
present on the surface. Coarse fragment content is particularly
high where weathered bedrock has been incorporated into thin
veneer sediments. Tuadook soils are very stony on the surface,
with 3 to 15% of the land area occupied by coarse fragments.
Boulders are common but usually not in sufficient quantities
to warrant designation as a bouldery phase. Tuadook
landforms are dominated by rolling surface expressions with
slopes varying from 5 to 30%. Some undulating (2 to 5%
slope) and hilly (9 to 45% slope) map units also occur. The
soils are relatively uniform in thickness and bedrock outcrops
are not all that common. Those bedrock exposures that do
occur are found on topographic highs and summits or along
steeply inclined drainage channels that are more deeply incised
into the bedrock. Well drained soils of the Tuadook
association support forest communities of yellow birch, white
birch, sugar maple, red maple, striped maple, red oak, white
spruce and balsam fir. On poorly to very poorly drained sites
the tree vegetation consists of black spruce, balsam fir, red
maple, yellow birch and some cedar.
Tuadook soils are dominated by well drained Orthic FerroHumic Podzols with some Orthic Humo-Ferric Podzols (Fig.
69). Climatic conditions in central New Brunswick are
conducive to the accumulation of organic matter in the
podzolic B horizon. Most Tuadook soils have enough organic
carbon to qualify for the Ferro-Humic Podzol great group. The
remaining well drained soils are Humo-Ferrics. Ferro-Humic
podzolization is not as strongly expressed along the eastern and
southern edges of the Tuadook range where the New
Brunswick Highlands merge with the Maritime Plain, which
has a slightly milder climate than the Highlands. Well to
moderately well drained conditions dominate. Significant
hectarages of imperfectly drained Tuadook soils occur as
Gleyed Humo-Ferric Podzols.
Under these drainage
conditions, an Ahe horizon up to 10 cm thick may develop in
lieu of the Ae horizon. The Ahe horizon usually develops at
the expense of Bhf horizon thickness. Poorly drained soils of
the Tuadook association are Orthic Gleysols. They are found
more extensively in gently undulating landscapes, but also
occur as localized areas in depressions and along drainage
channels in more strongly sloping map units. Internal drainage
is restricted by a slowly to very slowly permeable subsoil with
an estimated saturated hydraulic conductivity value of less than
0.5 cm/hr. Available water storage capacity ranges from 0.20
to 0.10 cm/cm, decreasing with depth because of reduced total
porosity in the compact subsoil. Well drained sites are
supplied with water solely via precipitation. Downward
movement of excess moisture through the profile is impeded
by the subsoil and lateral flow or seepage occurs along the
subsoil contact. Imperfectly and poorly to very poorly drained
areas have developed because of a combination of topographic
position, lack of gradient, subsoil compaction, seepage and
high groundwater table.
Soil development varies from 40 to in excess of 60 cm in
thickness. The common horizon sequence on well drained
sites is LFH, Ae, Bhf, Bf, BC and C. The organic layer
averages 5 cm thick. It overlies a thin (5 to 10 cm), ashy
coloured Ae horizon which breaks abruptly into the B horizon.
The upper reddish brown to strong brown Bhf horizon varies
from 5 to 15 cm in thickness. It merges with a yellowish
brown Bf horizon which gradually grades into the brown
parent material. Morphological appearance may be deceptive.
Significant amounts of translocated iron and aluminum are
often present in horizons that display little colour change from
the parent material. Imperfectly drained soils have similar
Figure 69. Well drained Tuadook soil profile.
profile horizons but with thicker LFH horizons (5 to 10 cm)
and are mottled in the B and C horizons, especially a thin zone
immediately above the compact subsoil where water is
perched. The Ae horizon may be irregular or broken because
of tree uprooting due to windthrow . Poorly to very poorly
drained horizon sequences lack a podzolic B horizon. They
consist of LFH or O, Aeg, Bg, BCg, and Cg horizons. The
forest duff layer is usually thicker than found in well and
imperfectly drained counterparts. In some profiles an Ah
horizon may be found in place of the thicker organic horizon.
The Tuadook textural profile consists of a loam to silt loam or
sandy loam (8 to 18% clay) throughout. Profile coarse
fragment content averages 15 to 35%, with a preponderance of
subangular to somewhat subrounded cobbles and stones.
Poorly and very poorly drained sites may have a “stonepavement” on the mineral soil surface below the organic
layers. Tuadook soils are low in inherent fertility and acidic
100
throughout. pH(H 2O) values range from less than 4.0 to only
slightly greater than 5.0. The solum is friable to very friable,
and varies from a weak to moderate, medium platy structure in
the Ae to a weak, fine to medium, granular or subangular
blocky structure in the B. The subsoil is firm to very firm and
massive, breaking to coarse pseudoplaty.
% Clay
15
12
% Coarse
Fragments
20 subangular C/S
30 subangular C/S
pH (H2 O)
4.5 - 5.0
4.5 - 5.0
BD (g/cm )
1.10
1.80
Ksat (cm/hr)
2-5
0.1 - 0.5
AWHC (cm/cm)
0.15 - 0.20
0.10
3
The Tuadook association is most comm only found with
members of the Juniper association. While both soils have
been derived from materials of similar lithological origin, they
are strikingly different in many respects. The most obvious
difference is subsoil com paction, and asso ciated
characteristics. Tuadook subsoils have firm to very firm
consistence, high bulk density (greater than 1.75 gm/cm 3) and
voids consisting predominantly of micro pores. Juniper
subsoils are loose and friable, lower in bulk density (usually
less than 1.55 gm/cm 3) and have a higher proportion of macro
pores. Juniper soils are coarse-loamy to sandy in particle size
class while Tuadook are more “modal” coarse loamy. Along
transition zones Tuadook soils have also been mapped in
complexes with Catamaran and Long Lake soils.
Excluding problems due to wetness in imperfectly and poorly
to very poorly drained locations, the dominant feature
affecting land use is coarse fragm ent content (both surface and
profile). Excessive stones preclude their use for agriculture
and impact on their use for forestry. Topographic conditions
(excessive slope) and the presence of a subsoil restricting layer
which impedes root penetration and water percolation, also
impact on land use. Low inherent fertility limits potential
forest crops.
Violette Association
The Violette association consists of soils that have developed
in relatively thin (less than 2 m thick) deposits of acidic, fine
loamy, compact morainal till sediments derived from quartzite
and sandstones with miscellaneous argillite, slate and
schists. Essentially, Violette are the fine-loamy equivalent of
Holmesville. They occur in the Chaleur Uplands and New
Brunswick Highlands physiographic regions of the study area
at elevations of 300 to 700 m above sea level (Fig. 70).
Violette soils occupy approximately 32,076 ha, or 1.15% of
the map sheet.
Summary of general characteristics of the Tuadook Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: TU
: N..B. Highlands
: 300-700 m
: 82,171 ha
: 2.95%
: Mineral
: Glacial till, compact
: <2 m
: Yellowish brown to brown
: Coarse loamy (skeletal)
: Granite, granodiorite , diorite, granite
gneiss and some volcanics
: Low
: Rolling, hilly and sloping (5-45%)
: Moderately well
: Orthic Ferro-Humic Podzol and Orthic
Humo-Ferric Podzol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 50
50 - 100+
Texture Class
Loam - silt loam or
sandy loam
Loam - sandy loam
% Sand
40
45
% Silt
45
43
Figure 70. Location of mapped Violette soils.
The soil parent material has been deposited as ground moraine,
plastered in place under the weight of advancing glacial ice.
Parent material composition strongly reflects the incorporation
of local bedrock formations. The till is a heterogeneous
mixture of subangular-shaped particle sizes ranging from silts
and clays to cobbles and stones. Violette soils are generally
not too stony to prevent their use for agriculture, with usually
less than 3% of the land surface area occupied by coarse
fragments. Boulders are not common. V iolette soils are found
on landforms varying from undulating or gently rolling to hilly
or sloping. Slopes of 5 to 15% are typical, but some slopes are
up to 45%. Although Violette landscapes are bedrock
controlled, bedrock exposures are rare. Well drained soils of
the Violette association support forest communities of sugar
101
maple, beech, yellow birch, red oak, red and white spruce,
balsam fir, red maple and pin cherry. On poorly to very poorly
drained sites the tree vegetation consists of black spruce, cedar,
speckled alder and balsam fir, with some red maple, tamarack
and willows.
ranging up to 30 cm thick. The Violette textural profile
consists of a loam to clay loam or sandy clay loam with 18 to
35% clay in the subsoil. Surface textures are commonly
loams, silt loams, clay loams or silty clay loams. Profile coarse
fragment content varies from 10 to 25%, with a preponderance
of subangular to somewhat subrounded gravels and cobbles.
Well to moderately well drained Violette soils are Orthic
Humo-Ferric Podzols and Podzolic Gray Luvisols (Fig. 71).
They are found on the more steeply sloping landscapes. In
these landscapes, poorly drained conditions are confined to
relatively narrow drainage channels.
Slow internal
permeability contributes to impeded drainage conditions.
Downward movement of excess moisture through the profile
is impeded by the subsoil, resulting in lateral flow or seepage,
particularly in the spring after snowmelt. Seepage results in
wet lower slope and depressional positions. Even sites with
significant slopes may be affected by wetness. Imperfectly and
poorly drained Violette soils occur more extensively on
undulating topography. Imperfectly drained Violette soils are
Gleyed Humo-Ferric Podzols and Gleyed Podzolic Gray
Luvisols. Poorly drained members are Orthic Gleysols or
Orthic Luvic Gleysols. Internal drainage is restricted by a
slowly permeable subsoil with an estimated saturated hydraulic
conductivity value of less than 0.1 cm/hr. The solum is
moderately permeable (saturated hydraulic conductivity of 2.0
to 5.0 cm/hr). Available water storage capacity ranges from
0.20 to 0.10 cm/cm, decreasing with depth because of reduced
total porosity in the compact subsoil. Well to moderately well
drained sites are supplied with water mostly via precipitation.
Imperfectly and poorly to very poorly drained areas have
developed because of a combination of topographic position,
lack of gradient, subsoil compaction, seepage and high
groundwater table.
Soil development varies from 35 to 80 cm in thickness. The
common horizon sequence on well to moderately well drained
sites is LFH, Ae, Bhf, Bf, BC or Bt and C. O horizons may
occur under coniferous forests where mosses dominate the
ground vegetation. The organic layer is 2 to 10 cm thick,
becoming more humified with depth. It overlies a thin (5 to 10
cm), white, ashy coloured Ae horizon which breaks abruptly
into the B horizon. The upper strong brown to dark reddish
brown Bhf horizon varies from 2 to 5 cm in thickness. It
merges with the brown to yellowish brown Bf horizon which
gradually grades into the oxidized olive to grayish brown
parent material. At 35 to 45 cm the podzolic B horizon grades
into a BC, Btj or Bt horizon, which grades into the unaltered
parent material or C horizon between 45 and 80 cm from the
mineral soil surface. Imperfectly drained soils have similar
profile horizons but are modified by periodic saturation. They
are mottled in the B and C horizons, especially a thin zone
immediately above the compact subsoils where water is
perched. The Ae horizon is often irregular or broken because
of tree uprooting due to windthrow. Poorly to very poorly
drained horizon sequences lack a podzolic B horizon. They
consist of LFH or O, Aeg, Bg, and Cg horizons. A Btg
horizon may be present between the Bg and Cg horizons. The
forest organic layer is thicker in the poorly and very poorly
drained conditions than found in well drained counterparts,
Figure 71. Moderately well drained Violette soil profile.
Violette soils are medium in inherent fertility and acidic
throughout, with pH(H 2O) values of 4.0 to 5.5. The friable to
very friable, weak to moderate, fine to medium, granular or
subangular blocky solum overlies a firm to very firm, massive
to medium platy subsoil. The subsoil is dense and compact
and resists deformation. Subsoil bulk densities often exceed
1.80 gm/cm 3 and voids consist primarily of micro pores.
The Violette association has been mapped in complexes with
members of the Boston Brook, Caribou, Carleton, Catamaran,
Long Lake, McGee and Thibault associations. The Boston
Brook, Caribou, McGee, and Thibault soils have all developed
on non-compact till deposits in comparison to the compact
subsoil of the Violette association. In addition, McGee and
Thibault soils are coarse-loamy compared to the fine-loamy
Violette soil. Caribou soils have developed on fine loamy
materials that are derived from calcite-rich rock types. Boston
102
Brook is most similar in parent material mineralogical
composition and can be considered as a non-compact Violette
soil equivalent. Carleton, Catamaran and Long Lake soils have
all developed on compact lodgment tills, but the Catamaran
and Long Lake association soils are coarse loamy with less
than 18% clay in the subsoil while Violette soils have in excess
of 18% clay. Carleton soils are similar in physical appearance
to Violette soils. They are differentiated on lithological and
related differences. Carleton soils have formed in till materials
derived from weakly calcareous slates, shales and fine-grained
sandstones with some limestone. As a result, Carleton soils are
richer in nutrients and have subsoils with higher pH values, pH
6.5 and greater.
The dominant features affecting land use of Violette
association soils are related to problems due to wetness as a
result of the presence of a subsoil restricting layer which
impedes both root penetration and water percolation.
However, Violette soils are medium in natural fertility and are
quite productive from a forestry perspective wherever wetness
conditions are not excessively restricting.
Summary of general characteristics of the Violette Association
Map Symbol
Physiographic Region(s)
Elevation
Extent
Percentage of Mapped Area
Parent Material Type
Mode of Origin
Material Thickness
Soil Colour
Family Particle Size Class
Petrology (parent material)
Inherent Fertility
Topography (slope)
Drainage (dominant)
Classification (typical)
: VO
: Chaleur Uplands, N.B. Highlands
: 300-700 m
: 32,076 ha
: 1.15%
: Mineral
: Glacial till, compact
:<2m
: Light olive brown
: Fine loamy
: Quartzite, sandstone and some shale,
argillite and slate
: Medium
: Rolling and undulating to hilly (2-45%)
: Moderately well
: Orthic Humo-Ferric Podzol and Podzolic
Gray Luvisol
Layer
Friable upper soil
material
Subsoil material
Depth (cm)
0 - 40
40 - 100+
Texture Class
Loam - silt loam
Loam - clay loam
% Sand
40
40
% Silt
40
30
% Clay
20
30
% Coarse
Fragments
10 subangular G/C
25 subangular G/C
pH (H2 O)
4.5 - 5.0
5.0 - 5.5
BD (g/cm3 )
1.20
1.80
Ksat (cm/hr)
2-5
< 0.1
AWHC (cm/cm)
0.20
0.10
LAND TYPES
Salt M arsh (SM )
Salt marsh represents those areas of undifferentiated marine
dep osits along the coast or tidal rivers which are submerged
at high tide by bra ckish to strongly saline water. They
consist of flat very p oorly drained land that is usually
covered by a thick mat of salt tolerant water-loving plants
and plant debris. Th ese units are scattered alo ng the coast
line from Chatham to Dalhousie. Salt marsh has been
mapped in six polygons, occupying 669 ha.
Sand Dunes (SD)
Sand dunes consist of loose sand deposited by wind action
into ridge-like piles. They are located above high tide level
along the coast. Sand dunes occup y 140 ha, having been
mapp ed in only 3 p olygons.
Water (WA)
These are small water bodies that appear as unnamed units on
the soil map. They usually consist of fresh water but in some
instances along the coast they may include salt or brackish
water. Forty four (44) polygons were designated as water.
They occupy a total of 5581 ha.
103
PART 5. ELECTRONIC DATA FILES
The conventional product of a soil survey such as Soils of
Central and Northern New B runswick consists of a high
quality paper map with legend, and an acco mpa nying rep ort,
like this one. The soil map portrays the extent and location
of the soils and the soil report provides detailed technical
information about the soils and land surface. With the
increased application of computer technologies to data
hand ling, a second product is also available - soil survey
information, both polygon lines and map unit attribute data,
in electronic format. T his allows for greater ab ility to
manipulate and apply the information in a consistent and
timely manner.
The polygon and ma p attribute data in this report are stored
nationally in the National Soils DataBase (NSD B) in the
Canadian Soil Information System (CanSIS), and
provincially in the New Brunswick Agricultural Land
Information System (NB 'ALIS'). CanSIS is maintained by
the Eastern Cereal and Oilseed Research Centre, Research
Branch, Agriculture and Agri-Food Canada, in Ottawa and
can be accessed via its web page at
h ttp : / / si s . a g r . g c . ca /ca n s is . NB 'ALIS' is a joint fede ralprovincial government system located in the Land and
Environment Branch, N ew Brunswick Department of
Agriculture, Fisheries and Aquiculture, in Fredericton, New
Brunswick. Both CanSIS and NB'ALIS' are based on
com merc ially available geographic information systems
(GIS).
GIS is designed to manage and manipulate large volumes of
information that are spatially oriented. The ability to handle
relationships among locations is the geo graphic feature o f a
GIS that sets it apart from a standard d ata base information
system. It also has analytical capabilities. CanSIS uses
ARC/INFO software while NB 'ALIS' uses CARIS
(Computer Aided Resource Information System) software.
Data exchange protocols have been established between the
two systems to ensure that information can be easily
transferred back and fo rth. These systems are also
comp atible with most other land information systems.
Polygon data is essentially line information to define the
map polygon bound aries and location. It is stored in a series
of x-y coordinates referenced to a base map. This defines
the geographic location aspect of the map polygon. Each
polygon has an associated reference to link it with map
attribute files that describe the polygon.
suitably handled separately. Plant nutrient sup ply is
manipulated by management, espec ially in agriculture.
Therefore, the ability of soils to supply water to growing
plants is the focal point of these files. This does not
preclude their use for other applications, but rather indicates
that they may at times b e lacking in some specific properties
required to make an assessmen t.
Core properties of these attribute files consist of the
following features:
-
drainage
water tab le
rooting depth
texture
organic matter
pH
base saturation
cation exchange ca pacity
water ho lding capacity
saturated hydraulic conduc tivity
bulk density
electrical cond uctivity
slope
stoniness
taxonomy to the Subgroup level
state of decomposition (O rganic soils)
wood content (Organic soils)
FILE STRUCTURE
The data is stored in five related files:
Project File (PF) - documentation on survey specifications,
etc. from the So il Survey Rep ort.
Polygon Attribute Table F ile (PA T) - links map polygons to
soil map units.
Soil Map Unit File (SMUF) - links soil map units to soil
names and landscape mo difiers.
Soil Names F ile (SN F) - links so il names to attributes that
pertain to the whole so il.
Soil Layer File (SLF) - links soil names to attributes that
vary in the vertical direction.
Project File (PF)
The follow ing inform ation is included in the PF file:
As a system serving agricultural, forestry, and environmental
needs, the inform ation sto red in these attrib ute files is
primarily concerned with the biological productivity of the
soils.
Biological prod uctivity is controlled by the
availab ility of energy, water, and nutrients. Since energy
availab ility is controlled by atmospheric climate, it is most
- survey intensity level
- publica tion scale
- photo graphy scale
- sampling/observation strategy (free, transect, grid, etc.)
- symbol configu ration including concept of soil map unit
104
-
"building blo cks" (series, association, etc.)
authors and contributors
publica tion da te
analytical methods
estimate o f reliability
ARC/INFO library
date of last revision
9
SOIL_CODE3
CHAR
3
10
MODIFIER3
CHAR
3
11
EXTENT3
NU ME RIC 2
12
SLOPEP1
NU ME RIC 5
1
13
SLOPEP2
NU ME RIC 5
1
14
SLOPEP3
NU ME RIC 5
1
15
STONE1
CHAR
1
16
STONE2
CHAR
1
17
STONE3
CHAR
1
18
DATE
DATE
8 Y Y .M M .D D
________________________________________________
Polygon Attribute Table File (PAT)
The purp ose o f the polygon attribute table file is to link
polygon numb ers to soil map units. For the p urpo se of this
discussion, a soil map unit is the entire symbol found within
a polygon drawn o n the soil map. An explana tion of the soil
map symbol from this report is given in PART 3. SOIL
MAPPING METHO DOLOG Y, Map symbol.
1
SMUF file field name descriptions are listed below.
PROVINCE
MAPUNITNOM
SOIL_CODE
The list of attributes for the PAT file is as follows:
Field
Field Name 1
Type
W idth
Dec
1
AREA
FLOATING
4
3
2
PERIMETER
FLOATING
4
3
3
SOIL#
BINARY
4
4
SOIL-ID
BINARY
4
5
MAPUNITNOM CHAR
60
________________________________________________
1
MODIFIER
EXTENT
SLOPE
PAT file field name descriptions are listed below.
STONE
AREA
PERIMETER
SOIL#
SOIL-ID
MAPUNITNOM
Area of polygon in square metres
Perimeter of polygon in metres
Internal system number
Polygon number
Map symbol
DATE
Code for province, i.e., NB for New
Brunswick
Soil map unit symbol as cod ed in
CanSIS from the original paper map
Three character code for the soil name
(SOIL_CODE1, SOIL_CODE2,
SOIL_CODE3)
Three character code to show soil
variations. The modifier applies to the
soil name and the soil code
(MODIFIER1, MOD IFIE R 2,
MO DIFIER3)
Percent of the map unit occupied by a
specific soil
Slope steepness in percent (SLOPEP1,
SLOPEP2, SLOPEP3)
Stoniness class (STON E1, STONE2,
STON E3)
Date of last revision
Soil Names File (SNF)
This file contains information that applies to the entire soil.
Soil Map Unit File (SMUF)
A record in the SMUF file is unique with respect to the
following fields:
A record in the SNF file is unique with respect to the
following fields:
PROVINCE
SOIL_CODE
MODIFIER
LU
PROVINCE
MAPUNIT N OM
The list of attributes for the SM UF file is as follows:
The list of attributes for the SN F file is as follows:
Field
1
2
3
4
5
6
7
8
Field Name 1
PROVINCE
MAPUNITNOM
SOIL_CODE1
MODIFIER1
EXTENT1
SOIL_CODE2
MODIFIER2
EXTENT2
Type
CHAR
CHAR
CHAR
CHAR
NU ME RIC
CHAR
CHAR
NU ME RIC
W idth
2
60
3
3
3
3
3
2
Dec
Field
Field Name 1
Type
W idth
1
2
3
4
5
6
7
PROVINCE
SOILNA M E
SOIL_CODE
MODIFIER
LU
KIND
WATERTBL
CHAR
CHAR
CHAR
CHAR
CHAR
CHAR
CHAR
2
24
3
3
1
1
2
Dec
105
8
ROOTRESTRI
CHAR
1
9
RESTR_TYPE
CHAR
2
10
DRAINAGE
CHAR
2
11
MDEP1
CHAR
4
12
MDEP2
CHAR
4
13
MDEP3
CHAR
4
14
ORDER
CHAR
2
15
S_GROUP
CHAR
4
16
G_GROUP
CHAR
3
17
PROFILE
CHAR
14
18
DATE
DATE
8YY.MM.DD
19
SLFNA
CHAR
1
_______________________________________________
1
SNF file field name descriptions are listed below.
PROVINCE
S OIL NAME
SOIL_CODE
MODIFIER
LU
KIND
WATERTBL
ROOTRESTRI
RESTR_TYPE
DRAINAGE
MDEP
ORDER
S_GROUP
G_GROUP
PROFILE
DATE
SLFNA
See SOIL MAP UNIT FILE
Assigned soil name i.e., Caribou
See SOIL MAP UNIT FILE
See SOIL MAP UNIT FILE
Land use (agriculture or native)
Kind of soil (m ineral, organic, etc.)
W ater table characteristics
Soil layer that restricts root growth
Type of root restricting layer
Soil drainage class
Mode of deposition (MD EP1, MDEP 2,
MD EP3)
Soil Order (Canadian System of Soil
Classification, CSSC)
Soil Subgroup (CSSC)
Soil Great Group (CSSC)
Representative soil profile reference
Date of last revision
Denotes prese nce o f soil layer file
records
Field
Field Name 1
Type
W idth
Dec
1
PROVINCE
CHAR
2
2
SOIL_CODE
CHAR
3
3
MODIFIER
CHAR
3
4
LU
CHAR
1
5
LAYER_NO
CHAR
1
6
HZN _LIT
CHAR
1
7
HZN_MAS
CHAR
3
8
HZN_SUF
CHAR
5
9
HZN_MOD
CHAR
1
10
UDEPTH
NU ME RIC 3
11
LDEPTH
NU ME RIC 3
12
COFRAG
NU ME RIC 3
13
DOMSAND
CHAR
2
14
VFSAND
NU ME RIC 3
15
TSAND
NU ME RIC 3
16
TSILT
NU ME RIC 3
17
TCLAY
NU ME RIC 3
18
ORGCARB
NU ME RIC 5
1
19
PHCA
NU ME RIC 4
1
20
PH2
NU ME RIC 4
1
21
BASES
NU ME RIC 2
22
CEC
NU ME RIC 3
23
KSAT
NU ME RIC 6
3
24
KP0
NU ME RIC 3
25
KP10
NU ME RIC 3
26
KP33
NU ME RIC 3
27
KP1500
NU ME RIC 3
28
BD
NU ME RIC 4
2
29
EC
NU ME RIC 3
30
CACO3
NU ME RIC 2
31
VONP OST
NU ME RIC 2
32
WOOD
NU ME RIC 2
33
DATE
DATE
8 YY.MM.DD
________________________________________________
1
Soil Layer File (SLF)
Note: For fields 12 and 14-32, a three digit numeric field for the number
of observations is optional. A code of zero (0) indicates an estimate.
2
This file is designed to handle attributes which vary in a
vertical direction, i.e., soil profile information. The mean
value is repo rted for each attribute. The method of analysis
is listed in the project file.
A record in the SLF file is unique with respect to the
following fields:
PROVINCE
SOIL_CODE
MODIFIER
LAYER_NO
LU
The list of attributes for the SLF file is as follows:
SLF file field name descriptions follow.
PROVINCE
SOIL_CODE
MODIFIER
LU
LAYER_NO
HZN _LIT
HZN_MAS
HZN_SUF
HZN_MOD
UDEPTH
LDEPTH
COFRAG
DOMSAND
VFSAND
TSAND
See SOIL MAP UNIT FILE
See SOIL MAP UNIT FILE
See SOIL MAP UNIT FILE
See SOIL NAMES FILE
1-9, Horizon number
Canadian System of Soil Classification
(CSSC) horizon lithological discontinuity
CSSC master horizon (upper case)
CSSC horizon suffix (lower case)
CSSC horizon modifier
Upper horizon depth (cm)
Lower horizon depth (cm)
Coarse fragments (% by volume)
Dominant sand fraction size
Very fine sand (% by weight)
To tal sand (% by weight)
106
TSILT
TCLAY
ORGCARB
PHCA
PH2
BASES
CEC
KSAT
KP0
KP10
KP33
KP1500
BD
EC
CACO3
VONP OST
WOOD
DATE
To tal silt (% b y weight)
To tal clay (% by weight)
Organic ca rbon (% by weight)
pH in calcium chloride
pH in water
Base saturation (%)
Cation exchange capacity (meq/100 g)
Saturated hydraulic conductivity (cm/h)
W ater retention at 0 kilop ascals
W ater retention at 10 kilo pascals
W ater retention at 33 kilo pascals
W ater retention at 150 0 kilop ascals
Bulk density of the soil matrix (g/cm3)
Electrical conductivity (dS/m)
Calcium carbonate equivalent (%)
von Post estimate of decomposition
Volume (%) of woody material
Date of last revision
The five files for the Soils of Central and Northern New
Brunswick are stored under the following names:
PFCNNB.TXT
PATCNNB.DBF
SMUFCNNB.DBF
SNFCNNB.DBF
SLFCNNB.DBF
ASCII Format
dBase Format
dBase Format
dBase Format
dBase Format
W hile application o f the data sets using a GIS allows for the
ability to display results geographica lly , i.e., on maps, lack
of such a system does not preclude analyses of the attribu te
file information. These data files are easily uploaded to a
personal computer and can be analysed with any number of
commercial database management software pro grams. The
interpretations presented in the next section of this report are
based on these files.
107
PART 6. INTERPRETATIONS - SINGLE FACTOR AND GENERAL
AGRICULTURE AND FORESTRY RATINGS
The purp ose o f soil survey is to enha nce the ability to
pred ict, and to make precise, differential interpretations
from area to area that can be use d in land-use decisionmaking.
Groupings or interpretations of soils and
landscapes are techniques that are used to make soil
information and maps mo re understandable to users (Olson
1981). It is often difficult for the non-soils specialist to
comprehend all the intricate details provided in a soil
survey. Interpretations are a synthesis of soil surve y data to
facilitate its use, as not all readers/users will be equally well
versed in the use and application o f soils inform ation. Soils
interpretations or group ings allow users such as planners and
developers to consider only those soil properties and
characteristics that are important for their specific intended
uses. Soils interpretations are typically stratified into three
categories: single-facto r or single parameter; soil suitability,
limitation or capability; and integrated soil/non-soil
assessments.
The simplest form of soil survey interpretation is a map or
table that shows a “single-factor” soil condition (Olson
1981). These maps dep ict or present core properties of the
soils and landscapes that are mapped in the soil survey, such
as drainage, depth to a compact layer, depth to bedrock,
stoniness, rockiness, slope and soil texture. B ecause only
one factor is considered, these maps are readily understood
and can be very effective at showing the limitations to, or
conversely the opportunities for, a given land use.
By “overlaying” or considering several different singlefactors at once, soils can be grouped to show suitability,
limitations or capabilities for a given use. Soils interpretive
guidelines for various agricultural crops (alfalfa, apples,
cereals, forages, potatoes, etc), forest tree species (balsam
fir/white spruce, black spruce, eastern white cedar, jack
pine/red pine, white pine, sugar maple, white ash, yellow
birch, trembling aspen), urban development (frost action,
housing, roads and streets, septic tank absorp tion fields,
sewage lagoo ns), recreation (outdoo r living, paths and
trails), and so urce m aterials (gravel, ho rticultural p eat,
road fill, sand, topso il) have b een d evelo ped and used in
New Brunswick (W ang and Rees 198 3, Atlantic Advisory
Committee on Soil Survey 19 88, F ahmy and R ees 1996 ).
Categories are made for each soil characteristic that is
considered important to the specific use and limits are set
acco rdingly.
Integration of soil/landscape and non-soil themes is the third
and most complicated form of soil interpretation. Most land
evaluation requires other “n on-soil” information for a more
com plete assessm ent of land potential. Climate, land use
and property ownership are three other essential
compo nents. An examp le of this kind of interp retation is
presented in Dillon et al. (1996) in which potential for
potato land expansion is based on inherent soil limitations,
climatic suitability, land cover type an d prope rty owne rship
considera tions.
In this repo rt, interpretations will be limited to a presentation
of the more important single-factor soil properties and
general assessm ents for agriculture and forestry (Table 5).
The se interpretations are for the do minan t soil and
landscape elements in the map symbol. By no means is this
an exhaustive list of all possible interpretations that can be
made. This is only the "tip of the icebe rg." A s previously
mentioned, interpretations can range from those for very
specific reasons, to those of a much more general nature.
Interpretations should be comm ensurate with the level of
detail provided by the survey and thus the scale of mapping.
The soils mapping prese nted in this survey is 1:250,000 or
exploratory in nature. However, while the information
provided is not ap propriately detailed for interp reting so il
suitability for site-specific use, it can still prove valuable for
estimates of the different po tential problems/op portunities
that exist in d ifferent areas of the region .
Soil map s rema in useful long after the soil interpretations
pub lished with them have b ecome o utdated. It should also
be remembered that these interpretations are not
recom mendations, but rather are indications of potential
difficulties, or conversely, potential opportunities, that the
land base offers to vario us uses. On -site inv estiga tion is
required prior to any actual usage of the land.
SINGLE-FACTOR SOIL MAP UNIT CONDITIONS
Depth to bedrock (m) - Shallowness to bedrock limits the
availab le rooting zone. It also has severe limitations on any
land uses requiring moderately deep so il excavations, such
as subsurface tile drain installation in agriculture and for
basement construction, land-levelling for athletic fields and
installation of septic tank filter fields. Veneers (v) consist of
less than 1 m of unconsolidated material over bedrock.
They are too thin to mask underlying irregularities in the
bedrock. Blankets (b) are moderately thin (1 to 2 m)
mantles of unconsolidated material thick enough to mask
minor irregularities in the underlying bedrock but still
conform to the general bedrock topography. Where no
dep th to bedrock is reported, the soil material is considered
to be greater than 2 m thick.
Depth to compact layer (cm) - The thickness of friab le soil
material available for root growth and water percolation is
an impo rtant consideration in both agricultural and forest
crop production and land management. Dense compact
108
subso il layers resist penetration of pla nt roots and
percolation of water. These soils are also late to dry in the
spring and easily saturated (perched zone of saturation) by
high intensity or prolonged rainfall. Shallow rooting of
crops may result in plant nutrient deficiencies, lack of
resistance to mid-summ er dro ught, and winter damage due
to frost heaving . Water percolation to subsurface drainage
lines is also impeded. Soil layers with bulk densities (BD)
greater than 1.60 g/cm 3 or pe rmea bilities of less than 1.0
cm/hr, or bo th, are considered restricting layers.
Drainage or w etness - Soil drainage refers to the rapidity
and extent of the removal of water from the soil in relation
to additions, especially by surface runoff and by flow
through the so il. Persistence of excess water, especially in
the spring and after prolonged or heavy precipitation,
hinders trafficability for many uses. Productivity of poo rly
drained soils is limited by a lack of aeratio n, susceptibility
to compaction, and lower soil temperature. Soil drainage
classes are described below:
Rap idly drained ®) - Water is remo ved from the soil
rapid ly in relation to supply. Soils are usually coarsetextured, shallow, or bo th.
W ater sourc e is
precipitation.
W ell drained (W) - Water is removed from the soil
readily but not rapidly. Soils are generally interme diate
in texture and depth. W ater source is precipitation.
Mode rately well drained (MW) - W ater is removed
from the soil so mewhat slowly in relation to supply.
Soils are usually medium- to fine-textured.
Precipitation is the dominant water source in mediumto fine-textured soils; precipitation and significant
additions by subsurface flow are necessary in coarsetextured soils.
Imperfectly drained (I) - Water is removed from the soil
sufficiently slowly in relation to supp ly to keep the so il
wet for a significant part of the growing season.
Precipitation, subsurface flow and groundwater act as
a water source, alone or in combination. Soils have a
wide range in texture and depth.
Poorly drained (P ) - Water is removed so slo wly in
relation to supply that the soil remains wet for a
com paratively large part of the time the soil is not
frozen. Subsurface flow or groundwater flow, or both,
in addition to p recipitation, are the main water sources.
Soils have a wide range in texture and depth.
Very poo rly drained (VP) - W ater is removed from the
soil so slowly that the water table remains at or on the
surface for the greater p art of the time the soil is not
frozen. Groundwater flow and subsurface flow are the
major water so urces. Soils ha ve a wide range in texture
and depth.
Fertility - Soil fertility is the quality of the soil that enables
it to provide the proper balance of nutrients for plant growth.
Mineralo gy or petrographic origin of the soil materials is a
determining factor in inherent site nutrient status. The
composition of parent rock materials contribute largely to
the chemical characteristics and pH o f soil. Some rock types
are rich in bases and weathe r rapid ly, resulting in so ils with
potentially high nutrient status. Other rocks contain few
bases or are more resistant to weathering and release
nutrients more sparingly. For a more detailed discussion on
soils and tree nutrient supply, the reader is referred to Forest
soils of New Brunswick by Co lpitts et al. (1995 ). W hile
natural or inherent fertility of the soil is to a large degree a
function of soil mineralogy, it also relates to soil nutrient
retention. Coa rser-textured so ils that are low in clay content
tend to be more easily leached of nutrients than finertextured soils. T he fertility rating is an estimate of the soil
nutrient status based o n the anticipated cum ulative effects of
these factors:
Association
Fertility
Code
Acadie Siding
Barrieau-Buctouche
Belldune River
Big Bald Mountain
Boston Brook
Caribou
Carleton
Catamaran
Gagetown
Grand Falls
Guimond River
Holmesville
Interval
Jacquet River
Juniper
Lavillette
Long Lake
Maliseet
McGee
Muniac
Nigadoo River
Parleeville
Popple Depot
Reece
Richibucto
Riverbank
Rogersville
St. Quentin
Stony Brook
Sunbury
Tetagouche
Tetagouche Falls
Thibault
Tracadie
Tuadook
Violette
very low
low
medium
very low
medium
high
high
medium
low
low
very low
medium
high
low
low
very low
medium
medium
medium
medium
medium
medium
low
medium
very low
low
medium
high
low
low
medium
medium
high
high
low
medium
vl
l
m
vl
m
h
h
m
l
l
vl
m
h
l
l
vl
m
m
m
m
m
m
l
m
vl
l
m
h
l
l
m
m
h
h
l
m
109
Flood ing or inundation - Flooding occurs when water
levels rise above normal stream, river, and lake boun daries.
Flooding interferes with time of planting, thus reducing an
already short growing season. Erosion of unprotected bare
ground, and subsequent sediment loading of stream courses,
can also result. The following flooding classes are used:
Class
Phase
R0
R1
R2
non
slightly
moderately
R3
very
None (N ) - soils not subjected to flooding
R4
exceedingly
R5
excessively
Occasional (O) - so ils subjected to flooding of short duration
once every 3 years or more
Frequent (F) - soils subjected to flooding of medium
duration once every 2 years
Very frequent (VF) - soils subjected to prolonged flooding
every year
Stoniness - Stoniness refers to the percentage of the land
surface occupied by coarse fragments of stone size (25 to
100 cm diameter). Plo wing, harrowing, and seeding
equipment are significantly hindered by the presence of
surface stones. Roo t crops, such as p otatoes, are esp ecially
sensitive to stoniness, in terms o f poten tial tuber injury.
Alternately, stones are somewhat beneficial in terms of
improving the soil thermal regime and protecting soil
particles from being washed away. Classes of stoniness are
defined on the basis of the percentage of the land surface
occupied by stone fragments 25 to 100 cm in diameter:
Class Phase
Effect on
Cultivation
% Surface Distance
Occupied Apart (m)
S0
S1
S2
S3
S4
non
slightly
moderately
very
exceedingly
<0.01
0.01-0.1
0.1-3
3-15
15-50
>30
10-30
2-10
1-2
0.1-1
S5
excessively
no hindrance
slight hindrance
some interference
serious handicap
cultivation prevented
until stones cleared
too stony to permit
any cultivation
>50
<0.1
Bo ulderiness - Boulderiness refers to the percentage of the
land surface occupied by coarse fragments of boulder size
(greater than 1 m diameter). It is defined with the same
class limits as stoniness.
Rockiness - Rockiness is an indication of the land surface
area that is occupied by bedrock exposures. Bedrock
exposures interfere with tillage. Bedrock outcrops are
incap able of supporting viable crops and result in fields with
non-uniform crop growth and quality. Rockiness classes are
defined below:
Effect on
Cultivation
no sign. interference
slight interference
tillage of inter-tilled
crops is impractical
use of most machinery
is impractical
all use of machinery
is impractical
---
% Surface Distance
Occupied Apart (m)
<2
2-10
10-25
>75
25-75
10-25
25-50
2-10
50-90
<2
>90
---
Slope or topography - Slope steep ness is an indication of
the landsc ape gradient. Imp ortant practical aspects of soil
slope that impact on use and managem ent include: rate and
amount of runoff; erodibility of the soil; use of agricultural
machinery; and uniformity of crop growth and maturity.
Although slope shape, length, and pattern also play an
important role in slope effect, slope grad ient is a convenient
measure of slope impact on cro p produ ction and so il
management. Slope classes are defined below:
Slope
Class
%
Slope
1
2
3
4
5
6
7
8
9
0-0.5
0.5-2
2-5
5-9
9-15
15-30
30-45
45-70
70-100
Soil texture - Soil texture is an ind ication of the relative
proportions of the various mineral soil particle size groups
- sand (2 to 0 .05 mm ), silt (0.05 to 0.002 mm) and clay (less
than 0.002 mm). Each of the textural soil classes has an
established range for percentage sand, silt, and clay. Soil
texture is one of the most permanent characteristics of a soil,
and probab ly the most important. Size of the soil particles
affects most chemical, physical, and minera logical reactions,
and influences root growth for plants and engineering
behaviour for machinery o peration. So il texture influences:
capillarity (water holding capacity); soil ero dibility
potential; cation exchange capacity and nutrient retention;
percolation; trafficability; and soil tilth. Subsoil texture
impa cts on subsoiling success. Coa rser-textured so il
materials are m ore p rone to shattering when subso iled dry.
Soil texture class abbreviations are defined below:
110
soils are found in New B runswick.
Typ ical %
Symbol Soil Texture
Sand
c
cl
l
ls
s
sc
scl
si
sic
sicl
sil
sl
28
32
41
82
93
52
61
9
7
10
23
65
clay
clay loam
loam
loamy sand
sand
sandy clay
sandy clay loam
silt
silty clay
silty clay loam
silt loam
sandy loam
Silt
22
35
41
12
3
7
11
86
46
57
64
25
Clay
50
33
18
6
4
41
28
5
47
33
13
10
CANADA LAND INVENTORY CLASSIFICATION
The Canada Land Inventory program was designed to
provide a basis for land-use planning. Although some
regional modifications of its application were incorporated,
the system is national in scope. It provides a relative
ranking of the soil's or land's capability, in terms of a rating
that is familiar and understoo d by many users.
Soil capability classification for agriculture
In the So il Capability Classification for Agriculture, mineral
soils are gro uped into se ven cla sses accord ing to their
potential and limitations for agricultural use (Canada Land
Inventory 196 5). T he first three classes are considered
capable of sustained production of comm on cultivated
crops; the fourth is marginal for sustained arable culture; the
fifth is capable o f use only for improved pasture and hay; the
sixth is capable o f use for only unimproved natural grazing;
and the seve nth class is fo r soils and land types (including
rock outcrops and small bodies of water) considered
incap able of use for arable culture or perma nent pasture.
The system was designed for mineral soils only and so is not
applicab le to organic soils.
The capability classification consists of two main
categories: the cap ability class and the capab ility subclass.
Capability class
The class is the b road est category in this classification. It is
a grouping of subclasses that have the same relative degree
of limitation or hazard. The class indicates the general
suitability of the soils for agricultural use. The limitation or
hazard becom es progressively greater from Class 1 to Class
7.
Class 1. Soils in this class have no significant limitations in
use for crops.
Due to regional climate limitations
(insufficient heat units and low natural fertility) no Class 1
Class 2. Soils in this class have mod erate limitations that
restrict the range of crops or require moderate conservation
practices.
Class 3. Soils in this class have moderately severe
limitations that restrict the range of crops or require special
conservation practices. Und er good m anagement these so ils
are fair to mod erately high in produ ctivity.
Class 4. Soils in this class have severe limitations that
restrict the range of crops or require special conservation
practices or bo th. The limitations may seriously affect such
farming practices as the timing and ease of tillage, planting
and harvesting, and the application and maintenance of
conservation practices.
Class 5. Soils in this class have very severe limitations that
restrict their cap ability to producing perennial forage crops,
but improvement practices are feasible. Some Class 5 soils
can be used for cultivated crops provided unusua lly
intensive management is used.
Class 6. Soils in this class are capable only of producing
perennial forage crop s, and im provement practices are not
feasible. While these soils have some natural capa bility to
sustain grazing, if not ma intained , they rapidly revert back
to forest. For this reason, no soils are classified as Class 6,
but instead they have been classed as Class 7.
Class 7. Soils in this class have no capa bility for ara ble
culture of common field crop s or perma nent pasture.
Capability sub class
The subclass group s soils with similar kinds of limitations
and hazards. It provides information on the kind of conservation problem or limitatio n. Subclass designations found
within the survey area are :
Adv erse climate ©) denotes inadequate heat for optimal
growth, thus restricting the range of crops that can be grown.
It is only used for Class 2 soils.
Un desirable soil structure and/or low permeability (D)
is used for soils in which the depth of rooting zone is
restricted by conditions other than a high water table or
consolidated bed rock. The restricting layer is usually a
compacted till material. Soil layers w ith bulk densities
greater than 1.60 g/cm 3 and/o r perm eabilities less than 1 .0
cm/hr are considered significantly restricting.
Low fertility (F) is used for soils having low fertility that
either is correctable with careful management in the use of
fertilizers and so il amendme nts or is difficult to correct in a
feasible way. T he limitatio n of soils in this subclass is
usually due to a lack of available plant nutrients (low
111
nutrient holding capacity), high acidity and low exchange
capacity.
Inundation by streams, rivers, and lakes (I) includes soils
subjected to flooding causing crop damage or restricting
agricultural use.
M oisture limitation (M ) denotes soils where crops are
adversely affected by dro ughtiness owing to inherent soil
characteristics.
These soils have low water holding
capacities.
Stoniness (P) indicates soils sufficiently stony on the
surface to hinder tillage, planting, and harvesting opera tions.
Stony soils are usually less pro ductive than c omp arable nonstony soils.
Consolidated bedrock ®) designates soils where the
presence of bedrock nea r the surface restricts their
agricultural use. This includes soils that have bedrock
within 1 m of the surface and also considers the presence of
bedro ck expo sures.
Topography (T) indicates soils where top ography is a
limitation. Both the percent of slope and the pattern of
frequency of slopes in different directions are important
factors in increasing the cost of farming over that of smooth
ground, in decreasing the uniformity of growth and maturity
of crops, and in increasing the hazard of water erosion.
Excess water (W ) is used fo r soils where excess water other
than that brought about by inundation is a limitation to their
use for agriculture.
Excess water may result from
inade quate soil drainage, a high water table, seepage or
runoff from surrou nding areas.
Land capability classification for forestry
The Land Capability Classification for Forestry is based on
the soil's ability to grow commercial timber (Canada Land
Inventory 196 7). Three ca tegories are used in this system:
the capa bility class, the capa bility subclass, and the indicator
species.
Capability class.
W hen assigning land to a given class, the environment of
subso il, soil surface, local and regional climate, as well as
the characteristic tree species, are all taken into acc ount.
The capability class, then, is an expression of all the
environmental factors as they ap ply to tree gro wth, i.e., it
defines the degree of limitation to the growth of commercial
forests.
Associated with each capability class is a
productivity range based on mean annual increment of the
best species or group of species adapted to the site. Expressed in cubic metres per hectare per annum, the classes
are:
Class
Class
Class
Class
Class
Class
Class
1
2
3
4
5
6
7
greater than 7.7 m 3
6.3 to 7.7 m3
4.9 to 6.3 m3
3.5 to 4.9 m3
2.1 to 3.5 m3
0.7 to 2.1 m3
less than 0.7 m 3
Ca pab ility sub class.
As expressed by the principle o f limiting facto rs, plant
response is determined by the least o ptimum facto r. Factors
that limit tree growth are shown as subclasses. Knowing the
kind of limitation is important in determining the type of
forest management to be used. Silvicultural practices can be
used that ove rcom e or m inimize the detrimental effects of a
given growth-limiting factor. The degree of limitation of the
growth-limiting factor determines the class designation.
The capability subclasses found within the survey area are:
climate
U
exposure, which, althoug h significant in
coastal region s, is not listed, as only so il
limitations are considered
soil moisture
M
soil mo isture de ficiency
W
excess soil moisture
perm eability and depth o f rooting zone :
D
physical restriction to rooting caused by dense
or consolidated layers, other than bedrock
R
restriction of rooting zone by bedrock
other soil factors:
F
low fertility
I
soils periodically inundated by streams or
lakes
P
stoniness which affects forest density or
growth
Indicato r species
Tree species that can be expected to yield the volume associated with each class are shown as p art of the symbol.
They are indigenous coniferous species adapted to the
region and land:
bs for black spruce
or
jp for jack p ine.
Table 5. Selected interpretations of soil map units
Map Unit Symbol
AS
AS + TU(b)6/u2
BB(b)5 + RB(b)4/u2
BB(b)4/l-u2
BB(b)5 + SB(b)6/u2
BB(b)4 + TC5/u2
BB4 + SB4/u2
BB(b)4/u2
BB(b)6 + SB(b)6/u2 + AS
BB(b)6 + SB(b)6/u2
BB(b)6 + RB5/u2
BB(b)7/u2
BB(b)3 + RB(v)1/u3
BB(b)3 + SB(b)4/u2
BM(v)1/m4-6 R2
BM(v)1 + JU(v)1/y6 B2
BM(v)1 + JU(v)1/s6-7 R2
BM(v)1 + JU(b)1/y6 B2
BM(v)1 + JU(v)1/y6
BM(v)1 + JU(v)1 + JR(v)1/y7 R1
BO(b)3 + HM(v)2/u3
BR4/u3
BR2 + TC6/u3
BR3 + GG3/u3
CB(b)4 + CR(b)4/m5
CB(b)4 + CR(b)4 + CB(v)2/m5
CB6 + BO6/u3
CB(v)2/u3
CB(v)2 + TH(v)1/s5-7
CB(b)2/m4
CB(v)1 + TH(v)1 + HM(b)2/s6
CB(b)2 + TH(b)2/u3
CB(v)2 + BO(v)2/y5
CB(v)2 + HM(b)2/m4
CB(v)2 + TH(v)2 + CR(b)2/r5-4
CB(b)2 + TH(b)3/u3
No. of
polygons
3
1
1
1
1
1
1
2
1
2
1
2
1
1
1
1
1
1
2
1
1
2
1
1
1
1
1
1
1
1
1
1
1
1
1
1
Area
(ha)
383
137
253
1270
1384
7566
2171
2173
14917
10073
7453
542
517
3219
2427
1334
1955
1446
659
8859
1467
17634
13138
593
2585
358
2009
2234
3673
30362
2763
4883
1945
517
7717
465
Dominant
soil
AS
AS
BB
BB
BB
BB
BB
BB
BB
BB
BB
BB
BB
BB
BM
BM
BM
BM
BM
BM
BO
BR
BR
BR
CB
CB
CB
CB
CB
CB
CB
CB
CB
CB
CB
CB
Depth to
bedrock
(m)
>2
>2
1-2
1-2
1-2
1-2
>2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
<1
<1
<1
<1
<1
<1
1-2
>2
>2
>2
1-2
1-2
>2
<1
<1
1-2
<1
1-2
<1
<1
<1
1-2
Depth to
compact
(cm)
120
120
65
65
65
65
65
65
65
65
65
65
65
65
70
70
70
70
70
70
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
Drainage
VP
VP
I
I
I
I
I
I
P
P
P
VP
W
W
W
W
W
W
W
W
W
I
W
W
I
I
P
W
W
W
W
W
W
W
W
W
StonFertility Flooding iness
vl
N
S0
vl
N
S0
l
N
S0
l
N
S0
l
N
S0
l
N
S0
l
N
S0
l
N
S0
l
N
S0
l
N
S0
l
N
S0
l
N
S0
l
N
S0
l
N
S0
vl
N
S2
vl
N
S2
vl
N
S2
vl
N
S2
vl
N
S2
vl
N
S2
m
N
S3
m
N
S1
m
N
S1
m
N
S1
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R2
B2
R0
B0
R2
B2
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
Average
Slope
(%)
0.25
1.25
1.25
1.25
1.25
1.25
1.25
1.25
1.25
1.25
1.25
1.25
3.5
1.25
17
22.5
30
22.5
22.5
37.5
3.5
3.5
3.5
3.5
12
12
3.5
3.5
27
7
22.5
3.5
12
7
10
3.5
Surface
soil
texture
n/a
n/a
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
sl
sl
sl
sl
sl
sl
l
sl
sl
sl
sil
sil
sil
sil
sil
sil
sil
sil
sil
sil
sil
sil
Parent
material
texture
n/a
n/a
s/scl
s/scl
s/scl
s/scl
s/scl
s/scl
s/scl
s/scl
s/scl
s/scl
s/scl
s/scl
ls
ls
ls
ls
ls
ls
cl
sl
sl
sl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
CLI
Agriculture
O
O
3WF
3WF
3WF
3WF
3WF
3WF
4W
4W
4W
5W
3MF
3MF
5TR
5TRP
5TR
5TRP
5TR
6T
3P
3WF
3MF
3MF
4T
4T
4W
3R
5T
3T
5T
2C
4TR
3TR
4TR
2C
CLI
Forestry
7W
7W
4Fjp
4Fjp
4Fjp
4Fjp
4Fjp
4Fjp
5Wbs
5Wbs
5Wbs
6Wbs
4FMjp
4FMjp
6RMFjp
6MFjp
6RMFjp
6MFjp
6MFjp
6UMFjp
3Fbs
3UFjp
3UFMjp
3UFMjp
3FWbs
3FWbs
4Wbs
3Fbs
3Fbs
3Fbs
3Fbs
3Fbs
3Fbs
3Fbs
3Fbs
3Fbs
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
CB(v)1/s6
CB(b)3 + CR(b)3/m5
CR(b)5 + TH(b)4 + VO(b)5/u3
CR(b)4 + TH(b)4/m5
CR(v)2 + TH(v)1/s8-9 R1
CR(v)2 + CB(v)2 + VO(v)2/y6
CR(v)2 + TH(v)1/s7
CR(v)2 + CB(v)1 + TH(v)1/y7 R1
CR(v)2 + HM(v)1/y6
CR(b)2 + TH(b)2 + CT(b)2/m4
CR(v)2/m5-4
CR(v)2 + TH(v)1/y6-7
CR(b)2 + CB(b)1/m5-4
CR(b)2 + CB(b)2 + VO(b)2/m5-4
CR(v)2 + CB(b)2/m4
CR(v)1 + VO(v)1/y6
CR(b)3/m4
CR(v)1 + TH(v)1/s9 R1
CR(b)3 + TH(b)2/m4
CR(v)3/m4-5
CT(b)4/u3
CT(b)4 + LL(b)4/u3
CT5/u3
CT(b)5 + RE(b)5/u3
CT5 + JU5/u3
CT(b)4 + RE(b)4/u3
CT(b)4 + LL(b)4/i3-4
CT6 + JU4/u3
CT(b)6 + LL(b)6/u3
CT(v)6/u3
CT(b)7 + LL(b)7/u3 + AS
CT(b)2 + RE(b)2/u3
CT(v)2/m4-5
CT(b)2/m4 + JU3/h4
CT(v)1 + LL(v)1/s6
CT(b)2 + JU(v)1/y7-8 R1
No. of
polygons
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
4
2
1
2
1
1
1
1
1
1
1
1
1
1
1
1
Area
(ha)
1608
6132
2986
1055
9431
15839
839
23114
2449
2025
333
4648
5570
16370
1024
2490
667
1361
8555
3257
7576
7421
7769
9870
3683
1176
3718
448
2247
2094
1187
1999
4509
5032
805
814
Dominant
soil
CB
CB
CR
CR
CR
CR
CR
CR
CR
CR
CR
CR
CR
CR
CR
CR
CR
CR
CR
CR
CT
CT
CT
CT
CT
CT
CT
CT
CT
CT
CT
CT
CT
CT
CT
CT
Depth to
bedrock
(m)
<1
1-2
1-2
1-2
<1
<1
<1
<1
<1
1-2
<1
<1
1-2
1-2
<1
<1
1-2
<1
1-2
<1
1-2
1-2
>2
1-2
>2
1-2
1-2
>2
1-2
<1
1-2
1-2
<1
1-2
<1
1-2
Depth to
compact
(cm)
100
100
55
55
55
55
55
55
55
55
55
55
55
55
55
55
55
55
55
55
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
Drainage
W
W
I
I
MW
MW
MW
MW
MW
MW
MW
MW
MW
MW
MW
W
W
W
W
W
I
I
I
I
I
I
I
P
P
P
VP
W
W
W
W
W
StonFertility Flooding iness
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
Average
Slope
(%)
22.5
12
3.5
12
72.5
22.5
37.5
37.5
22.5
7
10
30
10
10
7
22.5
7
85
7
10
3.5
3.5
3.5
3.5
3.5
3.5
5.5
3.5
3.5
3.5
3.5
3.5
10
7
22.5
50
Surface
soil
texture
sil
sil
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
Parent
material
texture
cl
cl
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
CLI
Agriculture
5T
4T
4WD
4T
7T
5T
6T
6T
5T
3T
4TR
5T
4T
4T
3TR
5T
3T
7T
3T
4TR
4WD
4WD
4WD
4WD
4WD
4WD
4WD
5WD
5WD
5WD
7W
3DP
4TR
3TDP
5T
6T
CLI
Forestry
3Fbs
3Fbs
3FDWbs
3FDWbs
5Rbs
3FDbs
3FDbs
4Rbs
3FDbs
3FDbs
3FDbs
3FDbs
3FDbs
3FDbs
3FDbs
3FDbs
3FDbs
5Rbs
3FDbs
3FDbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
5WDbs
5WDbs
5WDbs
6Wbs
4DFbs
4DFbs
4DFbs
4DFbs
4RDFbs
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
CT(b)2 + JU(b)2/m5
CT(b)3/y5-6
CT(v)2 + LL(v)2/s5
CT(b)2 + LL(b)2/m4
CT(b)2/m4
CT(b)2 + JU(b)2/m4
CT(b)2 + PD(b)2 + JR(v)3/m4
CT(b)3/m4
CT(b)3 + LL(b)3/s5-6
CT(b)2/m4-5
CT(v)2 + JU(v)1/s6
CT(v)2 + LL(v)1/s6 R1
GF5/u3
GF3/t3-5
GF3/t3-5 + IN5/u2
GF3/h4
GF3 + GG3/t3-5
GF3 + MA3/t3-5
GF2/u3
GF3/m4
GF3/t3
GG5 + RI5/u3
GG5 + GF5/u2
GG5/u3
GG4 + MU4/u3
GG4 + GF4/t3-5
GG6 + JU6/u3
GG1/h4
GG3 + RI3/t2-4
GG3 + RI3/t3
GG3/t3-5
GG1/u2
GG3/u3
GG3 + RI3/t3 + IN6/u2
GG1/s8
GG3 + JU3/u3
No. of
polygons
1
1
1
3
1
1
1
1
1
1
1
1
2
3
1
2
1
1
1
1
1
1
1
1
1
1
1
1
1
2
1
1
1
1
1
1
Area
(ha)
1282
3005
904
47239
124
6484
5935
3828
2463
14661
933
2319
6392
2374
200
6330
3027
510
306
1533
692
377
1782
445
931
6820
1844
3055
9916
8204
2644
638
695
3068
257
1408
Dominant
soil
CT
CT
CT
CT
CT
CT
CT
CT
CT
CT
CT
CT
GF
GF
GF
GF
GF
GF
GF
GF
GF
GG
GG
GG
GG
GG
GG
GG
GG
GG
GG
GG
GG
GG
GG
GG
Depth to
bedrock
(m)
1-2
1-2
<1
1-2
1-2
1-2
1-2
1-2
1-2
1-2
<1
<1
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
Depth to
compact
(cm)
50
50
50
50
50
50
50
50
50
50
50
50
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
Drainage
W
W
W
W
W
W
W
W
W
W
W
W
I
R
R
R
R
R
R
R
R
I
I
I
I
I
P
R
R
R
R
R
R
R
R
R
StonFertility Flooding iness
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
l
N
SO
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
Average
Slope
(%)
12
19.5
12
7
7
7
7
7
19.5
10
22.5
22.5
3.5
8.5
8.5
7
8.5
8.5
3.5
7
3.5
3.5
1.25
3.5
3.5
8.5
3.5
7
4.75
3.5
8.5
1.25
3.5
3.5
57.5
3.5
Surface
soil
texture
l
l
l
l
l
l
l
l
l
l
l
l
sl
sl
sl
sl
sl
sl
sl
sl
sl
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
Parent
material
texture
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
CLI
Agriculture
4T
5T
4TR
3TDP
3TDP
3TDP
3TDP
3TDP
5T
3TDP
5T
5T
3WF
3TMF
3TMF
3TMF
3TMF
3TMF
3TMF
3TMF
3MF
3WF
3WF
3WF
3WF
3WF
5W
4MF
4MF
4MF
4MF
4MF
4MF
4MF
6T
4MF
CLI
Forestry
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4RDFbs
4Fjp
5MFjp
5MFjp
5MFjp
5MFjp
5MFjp
5MFjp
5MFjp
5MFjp
4Fjp
4Fjp
4Fjp
4Fjp
4Fjp
6Wbs
5MFjp
5MFjp
5MFjp
5MFjp
5MFjp
5MFjp
5MFjp
5MFjp
5MFjp
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
GG1/h6
GG3 + JU3/t3-5
GG3/h3-5
GM3/u3
GM(b)1 + BB(b)3/u2
HM(v)4 + LL(v)4 + MG(b)2/u3
HM(b)5 + CR(b)5/u3
HM(b)5 + MG(b)4/u3
HM(b)6 + LL(b)6/u3
HM(b)3 + MG(b)3/m4
HM(b)2 + MG(v)1/m*6-7
HM(b)2 + LL(b)2 + MG(v)1/m4
HM(v)2 + CR(v)2/m4
HM(v)2 + MG(b)1/y5-6
HM(v)1 + MG(v)1/y6-7 R1
HM(v)2 + MG(v)1/m6 R1
HM(b)2 + MG(b)2/m4
IN4 + RI4/u2
IN4 + GF4/u2
JR5 + PD5/u2
JR(b)6 + PD(b)6/u3
JR(b)2 + TH(b)2 + TF(b)2/m*4-5
JR(v)1/y7 R1-2
JR2/h4-5
JR(b)3 + PD(v)2/h4
JR(v)2 + MG(v)2/m4
JR(b)3 + MG(b)3/h4-6
JR(v)1 + PD(v)2/s7 R2
JR(v)1 + CT(v)2/y9 R3
JR(v)1 + PD(v)2/y6 R1
JR(v)1/r5-6
JU5/h4 B1
JU5 + GG5/h4 B2
JU5 + JR5/h4
JU(b)5/u3 B2
JU(b)5/u3
No. of
polygons
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
2
1
1
1
1
1
1
1
Area
(ha)
420
614
1814
1312
524
10067
5413
2860
1529
1460
1989
2315
1549
3766
5508
1963
138
3650
2346
2134
2104
4517
327
1692
3098
4221
7180
2190
556
7436
1161
29934
6745
2199
4906
836
Dominant
soil
GG
GG
GG
GM
GM
HM
HM
HM
HM
HM
HM
HM
HM
HM
HM
HM
HM
IN
IN
JR
JR
JR
JR
JR
JR
JR
JR
JR
JR
JR
JR
JU
JU
JU
JU
JU
Depth to
bedrock
(m)
>2
>2
>2
>2
1-2
<1
1-2
1-2
1-2
1-2
1-2
1-2
<1
<1
<1
<1
1-2
>2
>2
>2
1-2
1-2
<1
>2
1-2
<1
1-2
<1
<1
<1
<1
>2
>2
>2
1-2
1-2
Depth to
compact
(cm)
100
100
100
100
100
50
50
50
50
50
50
50
50
50
50
50
50
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
Drainage
R
R
R
R
R
I
I
I
P
W
W
W
W
W
W
W
W
I
I
I
P
W
W
W
W
W
W
W
W
W
W
I
I
I
I
I
StonFertility Flooding iness
l
N
SO
l
N
SO
l
N
SO
vl
N
SO
vl
N
SO
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
h
F
S0
h
F
S0
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1-2
B0
R0
B0
R0
B0
R0
B0
R0
B0
R2
B0
R3
B0
R1
B0
R0
B1
R0
B2
R0
B0
R0
B2
R0
B0
R0
Average
Slope
(%)
22.5
8.5
8.5
3.5
1.25
3.5
3.5
3.5
3.5
7
30
7
7
19.5
30
22.5
7
1.25
1.25
1.25
3.5
10
37.5
10
7
7
17
37.5
85
22.5
19.5
7
7
7
3.5
3.5
Surface
soil
texture
ls
ls
ls
ls
ls
l
l
l
l
l
l
l
l
l
l
l
l
sil
sil
l
l
l
l
l
l
l
l
l
l
l
l
sl
sl
sl
sl
sl
Parent
material
texture
ls
ls
ls
ls
ls
l
l
l
l
l
l
l
l
l
l
l
l
sil
sil
l
l
l
l
l
l
l
l
l
l
l
l
sl
sl
sl
sl
sl
CLI
Agriculture
5T
4MF
4MF
4MF
4MF
4RWD
4WD
4WD
5WD
3TD
5T
3TD
3TRD
5T
5TR
5TR
3TD
3IW
3IW
4P
4W
4TP
6T
4TP
4P
4RP
5T
6T
7T
5TR
5T
5P
5P
4P
5P
4P
CLI
Forestry
5MFjp
5MFjp
5MFjp
5MFjp
5MFjp
4RDWbs
4DWbs
4DWbs
5WDbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
4RDbs
4RDbs
4Dbs
3FIbs
3FIbs
4Fbs
5WFbs
4Fbs
4RFbs
4Fbs
4Fbs
4Fbs
4Fbs
5RFbs
6RFbs
4Fbs
4Fbs
4Fbs
5PFbs
4Fbs
5PFbs
4Fbs
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
JU5/u3 B2
JU5 + TU5/u3
JU5/u3
JU(b)4/m4
JU4 + GG4/h4
JU5/h4
JU5/h4 B5
JU5 + CT5/u3
JU5/h4 B2
JU(b)6/h4
JU6/u2-3 + AS
JU6 + GG5/u3
JU(v)1/y6
JU(v)1/y8 R2
JU(v)1 + BM(v)1 + TU(b)2/y8 R2
JU(v)1 + BM(v)1 + TU(b)2/s7
JU(v)2 + BM(v)1/m4
JU(v)1 + TU(b)2/y6 R1
JU3/h4
JU(v)1 + JR(v)1/y7 R1
JU(b)1 + BM(v)1/m5-6 B2
JU(b)2/m5-4
JU3 + TF3/h5
JU(v)3 + CT(b)2/s6
JU(v)1 + TU(v)2/y5-6 B2
JU(b)1 + BM(v)1/y5
JU(b)2/m4
JU(v)1/y5-6
JU(b)3/m5 B2
JU(v)1 + BM(v)1 + TU(b)2/y6
JU(b)2/m6
JU(b)2/m4-5
JU(v)1 + TU(v)2/y5-7
JU(v)2 + TU(b)2/m4
No. of
polygons
1
2
1
1
1
2
1
1
1
1
1
1
1
2
1
1
1
1
1
1
1
1
1
1
1
1
2
1
1
1
1
1
1
1
Area
(ha)
4689
13762
3207
1138
13594
4680
3309
938
4467
1268
1718
1281
189
1319
974
1427
374
546
4483
2491
1609
9465
360
3899
16784
3370
1531
7350
3482
7299
1187
3061
4808
3866
Dominant
soil
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
Depth to
bedrock
(m)
>2
>2
>2
1-2
>2
>2
>2
>2
>2
1-2
>2
>2
<1
<1
<1
<1
<1
<1
>2
<1
1-2
1-2
>2
<1
<1
1-2
1-2
<1
1-2
<1
1-2
1-2
<1
<1
Depth to
compact
(cm)
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
Drainage
I
I
I
I
I
I
I
I
I
P
P
P
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
StonFertility Flooding iness
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
JU(b)3/m3-4
1
225
JU
JU(v)2 + MG(v)2 + TU(b)4/m4
1
1699
JU
1-2
100
W
l
N
S3
B0
R0
5.5
<1
100
W
l
N
S3
B0
R0
7
Boulder- Rockiness
iness
B2
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B5
R0
B0
R0
B2
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R2
B0
R2
B0
R0
B0
R0
B0
R1
B0
R0
B0
R1
B2
R0
B0
R0
B0
R0
B0
R0
B2
R0
B0
R0
B0
R0
B0
R0
B2
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
Average
Slope
(%)
3.5
3.5
3.5
7
7
7
7
3.5
7
7
2.75
3.5
22.5
57.5
57.5
37.5
7
22.5
7
37.5
19.5
10
12
22.5
19.5
12
7
19.5
12
22.5
22.5
10
27
7
Surface
soil
texture
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
Parent
material
texture
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
CLI
Agriculture
5P
4P
4P
4P
4P
4P
7P
4P
5P
5W
5W
5W
5T
6T
6T
6T
4RP
5TR
4P
6T
5TP
4TP
4TP
5T
5TRP
4TP
4P
5T
5P
5T
5T
4TP
5T
4RP
CLI
Forestry
5PFbs
4Fbs
4Fbs
4Fbs
4Fbs
4Fbs
6Pjp
4Fbs
5PFbs
6Wbs
6Wbs
6Wbs
4Fjp
5RFjp
5RFjp
4Fjp
4Fjp
4RFjp
4Fjp
4Fjp
5PFjp
4Fjp
4Fjp
4Fjp
5PFjp
4Fjp
4Fjp
4Fjp
5PFjp
4Fjp
4Fjp
4Fjp
4Fjp
4Fjp
sl
sl
4P
4Fjp
sl
sl
4RP
4Fjp
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
JU(v)1 + MG(v)1/y6
JU(v)1/y7 R3
JU(v)1 + CT(v)2/y6
JU(b)1/m6
JU(v)1 + MG(v)1 + LL(b)2/y8 R1
JU(b)1 + TU(b)2/y5-6
JU2/m5
JU(v)2/m4
JU(b)3 + TU(b)3/u3
JU(v)1/y6-7
LL(b)4 + MG(v)4/u3
LL(b)4 + RE(b)4/m4
LL(b)4 + CT(b)4 + MG(b)3/m4
LL(b)4 + CT(b)3/m4
LL(b)5/u2-3
LL(b)4 + TT(b)4 + MG(b)3/m3-4
LL(b)4 + RE(b)4/u3
LL(b)4 + NR(b)4 + PD(b)4/u3
LL(v)4/u3
LL(b)5 + MG(b)4 + HM(b)5/u3
LL(b)5 + MG(b)4/u3
LL(b)6 + VO(b)6 + MG(b)5/u3
LL(b)6 + PD(b)6/r-u3
LL(b)6 + MG(b)5/u2
LL(b)6 + RE(b)6/u2
LL6 + MG5/u2-3
LL(b)2 + MG(v)1/s5-4
LL(b)2 + MG(v)1 + JU(v)1/y7 R1-2
LL(b)3 + MG(b)3 + JU(b)3/u3
LL(v)1 + HM(v)2/s6 R1
LL(v)1 + JU(v)1/y6-7 R1
LL3 + JR3/h4-5
LL(v)2 + MG(v)2/r4
LL(b)3 + MG(b)3/m4-6
No. of
polygons
1
1
1
1
1
1
1
1
1
1
2
1
1
1
1
1
3
1
1
1
1
1
1
1
2
1
1
1
1
1
1
1
1
1
Area
(ha)
1773
244
3662
857
4697
24240
253
182
902
9673
9363
2487
3215
13580
4511
13183
5423
12426
765
12721
516
29080
12698
824
29592
4151
3475
5546
1290
1377
576
4770
2940
8745
Dominant
soil
JU
JU
JU
JU
JU
JU
JU
JU
JU
JU
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
Depth to
bedrock
(m)
<1
<1
<1
1-2
<1
1-2
>2
<1
1-2
<1
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
<1
1-2
1-2
1-2
1-2
1-2
1-2
>2
1-2
1-2
1-2
<1
<1
>2
<1
1-2
Depth to
compact
(cm)
100
100
100
100
100
100
100
100
100
100
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
Drainage
W
W
W
W
W
W
W
W
W
W
I
I
I
I
I
I
I
I
I
I
I
P
P
P
P
P
W
W
W
W
W
W
W
W
StonFertility Flooding iness
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
Boulder- Rockiness
iness
B0
R0
B0
R3
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1-2
B0
R0
B0
R1
B0
R1
B0
R0
B0
R0
B0
R0
Average
Slope
(%)
22.5
37.5
22.5
22.5
57.5
19.5
12
7
3.5
30
3.5
7
7
7
2.75
5.5
3.5
3.5
3.5
3.5
3.5
3.5
3.5
1.25
1.25
2.75
10
37.5
3.5
22.5
30
10
7
17
Surface
soil
texture
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
Parent
material
texture
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
CLI
Agriculture
5T
6TR
5T
5T
6T
5T
4TP
4RP
4P
5T
4WDP
4WDP
4WDP
4WDP
4WDP
4WDP
4WDP
4WDP
4RPWD
4WDP
4WDP
5WD
5WD
5WD
5WD
5WD
4TP
6T
4P
5TR
5TR
4TP
4RP
4TP
CLI
Forestry
4Fjp
6RFjp
4Fjp
4Fjp
5RFjp
4Fjp
4Fjp
4Fjp
4Fjp
4Fjp
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
4Dbs
4RDbs
4Dbs
4RDbs
4RDbs
4Dbs
4Dbs
4Dbs
LL(b)2 + RE(b)2/u3
1
4014
LL
1-2
50
W
m
N
S3
B0
R0
3.5
l
l
4P
4Dbs
LL(v)2 + MG(v)1/y6 R1
1
3709
LL
<1
50
W
m
N
S3
B0
R1
22.5
l
l
5TR
4RDbs
Tab le 5. Selected interp retations of soil map units cont’d
No. of
Map Unit Symbol
polygons
LL(b)2 + MG(b)3/u3-4
2
LL(v)1 + MG(v)1/m5-6
1
LL(v)2 + PD(v)2/s7-6 R1
1
LL(b)3/m4
1
LL(v)2 + PD(v)2 + JR(v)1/y6
1
LL(v)2 + MG(b)2/m5
1
LL(v)2 + MG(v)1/y6-7 R1
1
LL(v)2 + MG(v)2/m4
1
LL(b)3 + RE(b)3/u3
1
LL(b)2 + MG(v)2/m4
2
LL(b)2 + MG(b)2/m4
1
LL(b)2 + TU(b)2/m4
1
LL(b)2/m4
1
LL(b)2 + MG(v)2/s5
1
LV + RE(b)7/l2
5
LV + TC7/l1
1
LV + SB(b)7/l2
1
LV + RE(b)6/u2
1
LV
54
LV + BB7/l1
1
LV + AS + RB(b)7/l1
1
LV + RB(b)7/l1
2
LV + RS(b)7/l2
1
MA5/u3
1
MA3 + GF3/u3
1
MA3 + GF3/t3-5
1
MG(v)4 + LL(b)4/u*3
1
MG(b)4 + LL(b)4/m4
1
MG(b)5 + LL(b)5/u3
1
MG(v)2/m5-6
1
MG(v)1 + LL(b)2/r6-7
1
MG(v)1 + JR(v)1 + HM(b)2/y-s5-6 R11
MG(v)1 + HM(v)2/m6 R1
1
MG(v)1 + TH(v)1/s6-8 R1
1
MG(v)1/y6-5
1
MG(v)1 + JR(v)1/s7-6 R1
1
Area
(ha)
25369
3818
278
4190
8402
1627
9974
3358
509
11280
2294
10211
1825
1279
745
216
92
4523
21502
223
324
198
88
907
1236
1222
4601
299
321
8468
2987
10752
1941
895
2413
8155
Dominant
soil
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LL
LV
LV
LV
LV
LV
LV
LV
LV
LV
MA
MA
MA
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
Depth to
bedrock
(m)
1-2
<1
<1
1-2
<1
<1
<1
<1
1-2
1-2
1-2
1-2
1-2
1-2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
>2
<1
1-2
1-2
<1
<1
<1
<1
<1
<1
<1
Depth to
compact
(cm)
50
50
50
50
50
50
50
50
50
50
50
50
50
50
160
160
160
160
160
160
160
160
160
100
100
100
100
100
100
100
100
100
100
100
100
100
Drainage
W
W
W
W
W
W
W
W
W
W
W
W
W
W
VP
VP
VP
VP
VP
VP
VP
VP
VP
I
R
R
I
I
I
W
W
W
W
W
W
W
StonFertility Flooding iness
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
m
N
S0
m
N
S0
m
N
S0
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R1
B0
R1
B0
R0
B0
R1
Average
Slope
(%)
5.5
19.5
30
7
22.5
12
30
7
3.5
7
7
7
7
12
1.25
0.25
1.25
1.25
0.25
0.25
0.25
0.25
1.25
3.5
3.5
8.5
3.5
7
3.5
19.5
30
19.5
22.5
42.5
19.5
30
Surface
soil
texture
l
l
l
l
l
l
l
l
l
l
l
l
l
l
n/a
n/a
n/a
n/a
n/a
n/a
n/a
n/a
n/a
sil
sil
sil
l
l
l
l
l
l
l
l
l
l
Parent
material
texture
l
l
l
l
l
l
l
l
l
l
l
l
l
l
n/a
n/a
n/a
n/a
n/a
n/a
n/a
n/a
n/a
fsl
fsl
fsl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
CLI
Agriculture
4P
5T
5TR
4P
5T
4TRP
5TR
4RP
4P
4P
4P
4P
4P
4TP
O
O
O
O
O
O
O
O
O
3W
2C
3T
4RP
4P
4P
5T
5T
5TR
5TR
6T
5T
5TR
CLI
Forestry
4Dbs
4Dbs
4RDbs
4Dbs
4Dbs
4Dbs
4RDbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
7W
7W
7W
7W
7W
7W
7W
7W
7W
3Fjp
3FMjp
3FMjp
4Fbs
4Fbs
4Fbs
4Fbs
4Fbs
4RFbs
4RFbs
4RFbs
4Fbs
4RFbs
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
MG(v)1 + TH(v)1/s6
MG(v)1 + TH(b)2/s8-9 R2
MG(v)1/s8-9 R2
MG(v)1 + HM(b)2/m*6
MG(v)1/s9 R2
MG(v)2 + LL(b)2/m4
MG(v)2 + LL(b)2/m-y5-6
MG(b)3 + CT(b)3/m4
MG(v)1 + HM(b)3/m5-6
MG(v)1 + LL(v)2/y6 R2
MG(v)2 + HM(b)2 + CR(b)2/m5
MG(v)3 + LL(b)3/m-r4
MG(v)2 + LL(v)3 + HM(v)3/m5-6
MG(v)1 + HM(v)2/s8-9 R2
MG(b)3 + LL(v)2 + CT(v)2/m5
MG(v)2/m5
MG(v)1 + HM(b)2/y5
MG(v)2 + LL(v)2/s5
MG(v)2 + JR(v)2/m4-6
MG(v)1 + JR(v)1/y8-9 R3
MG(v)1 + TH(v)1/m5
MG(v)1 + TF(v)1/y6
MG(b)2 + TH(b)2/m-y5
MG(b)1 + TH(b)1/m*5
MG(v)1 + JR(v)2/s6 R1
MG(v)1 + HM(b)2/r6-7
MG(v)1/y7 R1-2
MG(v)1/s8 R2
MG(v)1 + LL(v)2/m5
MG(b)1 + HM(b)2/y5-6
MG(v)1 + HM(b)2/y6
MG(v)2/s5-6
MG(v)1/y-r*6-7 R1
MG(v)1/m5
MG(v)1/r*7 R2
MG(b)2 + TH(b)2/m5-4
No. of
polygons
1
1
1
2
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
4
1
1
1
1
1
1
1
1
1
1
1
1
1
2
1
1
Area
(ha)
1869
1341
10436
15682
2614
19131
19152
2479
3075
4423
22106
6328
3347
840
11933
4149
18655
2879
4247
3487
4874
559
11882
54
7253
4491
12043
1151
3608
2416
4491
1017
43236
3099
16410
11961
Dominant
soil
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
Depth to
bedrock
(m)
<1
<1
<1
<1
<1
<1
<1
1-2
<1
<1
<1
<1
<1
<1
1-2
<1
<1
<1
<1
<1
<1
<1
1-2
1-2
<1
<1
<1
<1
<1
1-2
<1
<1
<1
<1
<1
1-2
Depth to
compact
(cm)
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
Drainage
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
StonFertility Flooding iness
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
Boulder- Rockiness
iness
B0
R0
B0
R2
B0
R2
B0
R0
B0
R2
B0
R0
B0
R0
B0
R0
B0
R0
B0
R2
B0
R0
B0
R0
B0
R0
B0
R2
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R3
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R1-2
B0
R2
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R2
B0
R0
Average
Slope
(%)
22.5
72.5
72.5
22.5
85
7
19.5
7
19.5
22.5
12
7
19.5
72.5
12
12
12
12
17
72.5
12
22.5
12
12
22.5
30
37.5
57.5
12
19.5
22.5
19.5
30
12
37.5
10
Surface
soil
texture
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
Parent
material
texture
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
CLI
Agriculture
5T
7T
7T
5T
7T
4RP
5T
4P
5T
5TR
4TRP
4RP
5T
7T
4TP
4TRP
4TRP
4TRP
5T
7T
4TRP
5T
4TP
4TP
5TR
5T
6T
6T
4TRP
5T
5T
5T
5TR
4TRP
6T
4TP
CLI
Forestry
4Fbs
5Rbs
5Rbs
4Fbs
5Rbs
4Fbs
4Fbs
4Fbs
4Fbs
5Rbs
4Fbs
4Fbs
4Fbs
5Rbs
4Fbs
4Fbs
4Fbs
4Fbs
4Fbs
6Rbs
4Fbs
4Fbs
4Fbs
4Fbs
4RFbs
4Fbs
4RFbs
5Rbs
4Fbs
4Fbs
4Fbs
4Fbs
4RFbs
4Fbs
5Rbs
4Fbs
Tab le 5. Selected interp retations of soil map units cont’d
No. of
Map Unit Symbol
polygons
MG(v)1 + TH(v)1/m*6
1
MG(v)1 + JU(v)1/s6-8 R1
1
MG3/h5
1
MG(v)1/s6-8 R1
1
MG(b)1 + TH(b)2/m*5
1
MG(b)2 + HM(b)2/m4
1
MG(v)1/y-r*7 R1-2
1
MG(b)2 + TH(b)2/m4-5
1
MG(v)3 + LL(b)4 + JU(v)3/y5
1
MG(b)1 + LL(b)2 + CT(b)2/s5
1
MG(v)1 + TT(b)2 + PD(v)1/y5
1
MG(b)2 + HM(b)2 + TH(b)2/m4-5
1
MG(v)1 + TH(v)1/s7-8 R1
1
MG(v)1/s7-8 R1
2
MG(b)2 + TH(b)2 + HM(b)2/m4-5
1
MG(b)2 + HM(v)3/m4-5
1
MU4 + MA4/t3-5
1
MU2 + GG4/u3
1
MU2/u3
1
NR(b)4 + PD(b)4 + LL(b)4/m4
1
NR(v)4 + TT(v)4/m4
1
NR(b)5/m4
1
NR(v)2/h6
1
NR(b)3/u3
1
NR(v)2 + PD(v)2/y6-7
1
NR(v)3/m3 + PD(b)3/m4 + TF3/h4-5 1
NR(v)1 + TF(v)1/r5-7 R1
1
NR(v)2/s5
1
PA(b)4/u3
1
PA4/u3
1
PA(v)2/m4
1
PA(v)1/m5-6
1
PA(v-b)2/m4-5
1
PD(v)4/m4 R1
1
PD(b)5 + LL(b)5/u3
1
PD(b)6 + JR(b)5/u3
1
Area
(ha)
2386
4471
1202
1689
11621
1707
33160
759
6197
4112
14872
28432
5968
2556
18762
2993
1835
483
548
2741
5104
1123
1643
1953
3319
12446
9131
154
2702
3102
1358
2885
6752
12895
1885
922
Dominant
soil
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MG
MU
MU
MU
NR
NR
NR
NR
NR
NR
NR
NR
NR
PA
PA
PA
PA
PA
PD
PD
PD
Depth to
bedrock
(m)
<1
<1
>2
<1
1-2
1-2
<1
1-2
<1
1-2
<1
1-2
<1
<1
1-2
1-2
>2
>2
>2
1-2
<1
1-2
<1
1-2
<1
<1
<1
<1
1-2
>2
<1
<1
<1
<1
1-2
1-2
Depth to
compact
(cm)
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
45
45
45
45
45
45
45
45
45
100
100
100
100
100
45
45
45
Drainage
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
I
R
R
I
I
I
W
W
W
W
W
W
I
I
W
W
W
I
I
P
StonFertility Flooding iness
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S0
m
N
S0
m
N
S0
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
l
N
S3
l
N
S3
l
N
S3
Boulder- Rockiness
iness
B0
R0
B0
R1
B0
R0
B0
R1
B0
R0
B0
R0
B0
R1-2
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
Average
Slope
(%)
22.5
42.5
12
42.5
12
7
37.5
10
12
12
12
10
50
50
10
10
8.5
3.5
3.5
7
7
7
22.5
3.5
30
3.5
27
12
3.5
3.5
7
19.5
10
7
3.5
3.5
Surface
soil
texture
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
sl
sl
sl
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
Parent
material
texture
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
ls
ls
ls
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
CLI
Agriculture
5T
6T
4TP
6T
4TP
4P
6T
4TP
4TRP
4TP
4TRP
4TP
6T
6T
4TP
4TP
3TWF
3MF
3MF
4WD
4RWD
4WD
5T
3D
5T
3RPD
5TR
4TR
3W
3W
3TR
5T
4TR
4RWDP
4WDP
5WD
CLI
Forestry
4Fbs
4RFbs
4Fbs
4RFbs
4Fbs
4Fbs
4RFbs
4Fbs
4Fbs
4Fbs
4Fbs
4Fbs
5RFbs
5RFbs
4Fbs
4Fbs
3Fbs
4Mjp
4Mjp
4DWbs
4DWbs
4DWbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
3Fbs
3Fbs
3Fbs
3Fbs
3Fbs
4RDWbs
4DWbs
5WDbs
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
PD(b)6 + LL(b)5/u2
PD(v)2 + LL(v)2 + MG(b)5/u3
PD(v)2/m5-4
PD(v)2 + LL(v)1/s8 R1
PD(v)3 + LL(v)3/m4
PD(b)2 + LL(b)2/u3
PD(b)3 + LL(b)3/u3
PD(b)2/u3
PD(b)2 + NR(b)2/m4-5
PD(v)1 + JR(v)1/y6-5 R2
PD(v)3 + TF(v)3/m4-5
PD(v)2 + JR(v)2/y5
PD(v)2 + JR(v)1/y5-6
PD(b)2 + TF(b)1/y6 R1
PD(v)2 + JR(v)1/s7 R2
RB(v)5/u2
RB(v)4/u2
RB(v)4/l-u2
RB(v)4 + BB(b)5/u2
RB(b-v)3/l2 + AS
RB3 + TC6/u2
RB3 + GM3/u3
RB(v)2/u2
RB(v)1 + BB(b)4 + SB(b)4/u3
RB(v)1/u3
RB2 + BB3/u3
RB(v)1/u2
RB(v)3/l2
RB(v)3/l2 + AS
RB(v)1 + BB(b)4/u3
RB(b)2 + BB(b)4/u2
RB(v)2 + BB(b)3/u2
RE(b)5/u3
RE(b)4 + SN(b)3/u3
RE(b)4 + SN(b)4/u2-3
RE(b)4/u2
No. of
polygons
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
6
1
1
4
1
1
6
1
1
1
1
1
1
1
1
1
2
2
1
1
Area
(ha)
2913
16178
272
4054
12949
8444
1947
3383
8752
18767
27320
14030
26286
4653
2538
5321
14412
810
1599
14136
7667
1633
7933
2292
237
1246
548
2092
291
415
4520
3156
8176
34795
12428
3406
Dominant
soil
PD
PD
PD
PD
PD
PD
PD
PD
PD
PD
PD
PD
PD
PD
PD
RB
RB
RB
RB
RB
RB
RB
RB
RB
RB
RB
RB
RB
RB
RB
RB
RB
RE
RE
RE
RE
Depth to
bedrock
(m)
1-2
<1
<1
<1
<1
1-2
1-2
1-2
1-2
<1
<1
<1
<1
1-2
<1
<1
<1
<1
<1
1-2
>2
>2
<1
<1
<1
>2
<1
<1
<1
<1
1-2
<1
1-2
1-2
1-2
1-2
Depth to
compact
(cm)
45
45
45
45
45
45
45
45
45
45
45
45
45
45
45
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
50
50
50
50
Drainage
P
W
W
W
W
W
W
W
W
W
W
W
W
W
W
I
I
I
I
R
R
R
R
R
R
R
R
R
R
R
R
R
I
I
I
I
StonFertility Flooding iness
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
vl
N
S0
m
N
S2
m
N
S2
m
N
S2
m
N
S2
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R2
B0
R0
B0
R0
B0
R0
B0
R1
B0
R2
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
Average
Slope
(%)
1.25
3.5
10
57.5
7
3.5
3.5
3.5
10
19.5
10
12
19.5
22.5
37.5
1.25
1.25
1.25
1.25
1.25
1.25
3.5
1.25
3.5
3.5
3.5
1.25
1.25
1.25
3.5
1.25
1.25
3.5
3.5
2.75
1.25
Surface
soil
texture
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
sl
sl
sl
sl
Parent
material
texture
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
ls
l
l
l
l
CLI
Agriculture
5WD
4P
4TRP
6T
4RP
4P
4P
4P
4TP
5TR
4TRP
4TRP
5T
5TR
6T
3RWF
3RWF
3RWF
3RWF
3MF
3MF
3MF
3RMF
3RMF
3RMF
3MF
3RMF
3RMF
3RMF
3RMF
3MF
3RMF
4WD
4WD
4WD
4WD
CLI
Forestry
5WDbs
4DFbs
4DFbs
5RDFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
5Rbs
4DFbs
4DFbs
4DFbs
4RDFbs
5Rbs
4Fjp
4Fjp
4Fjp
4Fjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4DWbs
4DWbs
4DWbs
4DWbs
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
RE(b)4/u3
RE(b)5 + SN(b)4/u3
RE(b)5/u2-3
RE(b)4 + SN(b)2/u3
RE(v)4/u3-4
RE(v)4 + SN(v)2/u3
RE(b)5 + SN(b)4/u2-3
RE(b)4 + SN(v)3/u3
RE(b)4 + SN(b)2/m4-3
RE(b)5/u2
RE(b)4 + SN(b)4/u3
RE(v)4 + SN(v)2/m4-3
RE(b)4/u2-3
RE(b)6/u2-3
RE(b)6/u2
RE(b)6 + SB(b)6/u2 + AS
RE(b)6/u2 + AS
RE(b)6 + SN(b)5/u2 + LV
RE(b)6 + SN(b)5/u3-2
RE(b)6 + LL(b)6/u2 + GG5/h3-4
RE(b)6 + LL(b)6/u3
RE(b)6 + SN(b)5/u2
RE(b)6 + SN(b)5/u2 + AS
RE(b)7 + CT(b)7/u2
RE(b)7/u2 + AS
RE(b)7/u2
RE(b)2/u3-2
RE(v)2 + SN(v)1/s5
RE(v)2/s4
RE(b)2 + SN(b)2/u3
RE(b)2 + SN(b)1/u3
RE(v)2 + SB(b)4/u3
RE(v)2 + LL(v)2/s6-5
RE(v)2 + SN(v)1/s5-4
RE(b)2/u3 + SN(v)2/s5
RE(b)2 + SN(b)2/u3-2
No. of
polygons
6
1
1
1
1
3
1
1
1
2
1
1
2
1
3
1
7
1
1
1
1
2
5
1
1
1
1
1
1
7
1
1
1
1
1
1
Area
(ha)
19642
1060
13072
1552
6566
11834
3905
7123
13955
184
1458
3716
2062
7377
11487
35936
41075
4439
10430
6851
14185
2969
16226
636
1223
1487
585
899
513
21049
9466
4345
3290
1026
10792
2821
Dominant
soil
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
RE
Depth to
bedrock
(m)
1-2
1-2
1-2
1-2
<1
<1
1-2
1-2
1-2
1-2
1-2
<1
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
<1
<1
1-2
1-2
<1
<1
<1
1-2
1-2
Depth to
compact
(cm)
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
Drainage
I
I
I
I
I
I
I
I
I
I
I
I
I
P
P
P
P
P
P
P
P
P
P
VP
VP
VP
W
W
W
W
W
W
W
W
W
W
StonFertility Flooding iness
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
Average
Slope
(%)
3.5
3.5
2.75
3.5
5.5
3.5
2.75
3.5
5.5
1.25
3.5
5.5
2.75
2.75
1.25
1.25
1.25
1.25
2.75
1.25
3.5
1.25
1.25
1.25
1.25
1.25
2.75
12
7
3.5
3.5
3.5
19.5
10
3.5
2.75
Surface
soil
texture
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
Parent
material
texture
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
CLI
Agriculture
4WD
4WD
4WD
4WD
4RWD
4RWD
4WD
4WD
4WD
4WD
4WD
4RWD
4WD
5WD
5WD
5WD
5WD
5WD
5WD
5WD
5WD
5WD
5WD
7W
7W
7W
3D
4TR
3TRD
3D
3D
3RD
5T
4TR
3D
3D
CLI
Forestry
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
6Wbs
6Wbs
6Wbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
4Dbs
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
RE(b)2/u3
RE(v)2 + SN(v)2/u2
RE(b)2 + SN(v)2/m4
RE(b)3 + SN(b)3/u2
RI4/u3
RI6 + GG6/u2
RI2/u3
RS(b)4/u3
RS(b)4 + RE(b)4/u3
RS(b)4/u2-3
RS(b)6/u2
SB(b)5 + SN(b)4/u3
SB(b)4/u3
SB(b)4 + SN(b)2/u3
SB(b)5/u2
SB(b)5/u3
SB(b)4 + RE(b)4/u3
SB(b)2 + SN(b)2/u3
SB(b)2 + RE(b)2/u3
SB(v)2/s5-6
SB(b)3/u3
SB(v)2 + SN(v)1/u3
SB(b)2/u3
SB(b)2 + RE(b)2 + SN(v)2/m5
SB(b)2/u2-3
SB6/u2 + AS
SB(b)6/u3
SB(b)6 + RE(b)5/u2
SB(b)6 + BB(b)5/u3
SB(b)6/u2 + AS
SB(b)6/u2
SB(b)7/u2 + AS
SB(b)7 + BB(b)7/u2
SD
SM
SM + BB7/l1
No. of
polygons
4
1
1
1
2
1
1
1
1
1
1
2
9
1
1
5
1
1
1
2
1
1
5
1
1
1
1
2
1
3
1
1
1
2
3
1
Area
(ha)
21731
4174
24042
253
670
4110
1622
125
3040
443
590
7821
27214
12580
2436
18231
7810
5863
172
3208
1422
692
4274
3511
2348
1002
2385
4942
2708
38043
2733
6531
1837
102
378
214
Dominant
soil
RE
RE
RE
RE
RI
RI
RI
RS
RS
RS
RS
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SB
SD
SM
SM
Depth to
bedrock
(m)
1-2
<1
1-2
1-2
>2
>2
>2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
<1
1-2
<1
1-2
1-2
1-2
>2
1-2
1-2
1-2
1-2
1-2
1-2
1-2
>2
>2
>2
Depth to
compact
(cm)
50
50
50
50
100
100
100
45
45
45
45
40
40
40
40
40
40
40
40
40
40
40
40
40
40
40
40
40
40
40
40
40
40
n/a
n/a
n/a
Drainage
W
W
W
W
I
P
R
I
I
I
P
I
I
I
I
I
I
MW
MW
MW
MW
MW
MW
MW
MW
P
P
P
P
P
P
VP
VP
n/a
n/a
n/a
StonFertility Flooding iness
m
N
S2
m
N
S2
m
N
S2
m
N
S2
l
N
S0
l
N
S0
l
N
S0
m
N
S2
m
N
S2
m
N
S2
m
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
l
N
S2
n/a
n/a
n/a
n/a
n/a
n/a
n/a
n/a
n/a
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
Average
Slope
(%)
3.5
1.25
7
1.25
3.5
1.25
3.5
3.5
3.5
2.75
1.25
3.5
3.5
3.5
1.25
3.5
3.5
3.5
3.5
19.5
3.5
3.5
3.5
12
2.75
1.25
3.5
1.25
3.5
1.25
1.25
1.25
1.25
n/a
n/a
n/a
Surface
soil
texture
sl
sl
sl
sl
sl
sl
sl
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
n/a
n/a
n/a
Parent
material
texture
l
l
l
l
s
s
s
l
l
l
l
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
cl
n/a
n/a
n/a
CLI
Agriculture
3D
3RD
3TD
3D
3WF
4W
3MF
4WD
4WD
4WD
5WD
4DW
4DW
4DW
4DW
4DW
4DW
3D
3D
5T
3D
3DR
3D
4T
3D
5WD
5WD
5WD
5WD
5WD
5WD
7W
7W
-
CLI
Forestry
4Dbs
4Dbs
4Dbs
4Dbs
4Fjp
6Wbs
4MFjp
4DWbs
4DWbs
4DWbs
5WDbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DWbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
6Wbs
6Wbs
-
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
SM + SD
SN(v)1 + RE(b)2/s4-5
SN(v)1/s4-5
SN(v)2/u2
SN(v)2 + RE(b)4/u2-3
SN(v)1/s5
SN(v)1/s4
SN(b)3 + SB(b)3/u3
SN(b)2/u3
SN2 + RE2/u3
SN(v)2 + RE(b)2/u3
SN(b)2 + RE(b)3/u3
SN(b)2/u2
SN(v)1 + RE(b)2/s6
SN(v)2/u3
SN(b)2 + RE(b)2/u3
SN(v)2 + RE(b)2/s4-5
SQ
TC6 + BB6/u2
TC6/u3
TC(b)6 + RB(b)6/u2
TC(b)6 + SB(b)5/u2
TC6 + BR4/u2-3
TC(b)6 + BB(b)6/u2
TC7 + RB6/l2
TC7/u2
TC7/u2 + SM
TF4 + TT5 + PD5/u3
TF(v)1 + JU(v)1/y6 R1
TF(v)1 + JR(v)1 + PD(b)2/y6-7
TF(b)2 + TT(b)2 + PD(b)2/m4
TF(v)1 + TT(v)2/r5-6
TF(b)3 + NR(v)3 + JR3(b)/h4-5
TF(v)2 + LL(v)2 + TH(v)1/m5-4
TF(v)2 + MG(v)2/h5-6
TF(v)1 + NR(v)1/y5
No. of
polygons
1
1
1
1
3
1
1
1
1
1
1
1
1
1
1
2
3
7
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
Area
(ha)
127
6303
1725
1095
13888
1057
708
1725
1020
3900
1352
1668
1651
785
2528
1919
2434
1111
153
2662
739
816
2026
337
1511
323
174
3110
7293
3439
15088
2618
10446
2002
788
1887
Dominant
soil
SM
SN
SN
SN
SN
SN
SN
SN
SN
SN
SN
SN
SN
SN
SN
SN
SN
SQ
TC
TC
TC
TC
TC
TC
TC
TC
TC
TF
TF
TF
TF
TF
TF
TF
TF
TF
Depth to
bedrock
(m)
>2
<1
<1
<1
<1
<1
<1
1-2
1-2
>2
<1
1-2
1-2
<1
<1
1-2
<1
>2
>2
>2
1-2
1-2
>2
1-2
>2
>2
>2
>2
<1
<1
1-2
<1
1-2
<1
<1
<1
Depth to
compact
(cm)
n/a
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
150
30
30
30
30
30
30
30
30
30
100
100
100
100
100
100
100
100
100
Drainage
n/a
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
VP
P
P
P
P
P
P
VP
VP
VP
I
W
W
W
W
W
W
W
W
StonFertility Flooding iness
n/a
n/a
n/a
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
h
N
S0
h
N
S0
h
N
S0
h
N
S0
h
N
S0
h
N
S0
h
N
S0
h
N
S0
h
N
S0
h
N
S0
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
m
N
S3
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
Average
Slope
(%)
n/a
10
10
1.25
2.75
12
7
3.5
3.5
3.5
3.5
3.5
1.25
22.5
3.5
3.5
10
0.25
1.25
3.5
1.25
1.25
2.75
1.25
1.25
1.25
1.25
3.5
22.5
30
7
19.5
10
10
19.5
12
Surface
soil
texture
n/a
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
n/a
sicl
sicl
sicl
sicl
sicl
sicl
sicl
sicl
sicl
l
l
l
l
l
l
l
l
l
Parent
material
texture
n/a
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
sl
n/a
sic
sic
sic
sic
sic
sic
sic
sic
sic
l
l
l
l
l
l
l
l
l
CLI
Agriculture
4TR
4TR
3RPM
3RPM
4TR
3RPM
3PM
3PM
3PM
3RPM
3PM
4PM
5T
3RPM
3PM
4TR
O
5WD
5WD
5WD
5WD
5WD
5WD
7W
7W
7W
3P
5TR
5T
3P
5T
4T
4TR
5T
4TR
CLI
Forestry
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
4FMjp
6Wbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
5WDbs
6Wbs
6Wbs
6Wbs
3Fbs
4RFbs
3Fbs
3Fbs
3Fbs
3Fbs
3Fbs
3Fbs
3Fbs
Tab le 5. Selected interp retations of soil map units cont’d
No. of
Map Unit Symbol
polygons
TF(v)1 + TT(v)2 + BO(v)2/r6-8
1
TF(b-v)2 + JU(v)1 + CT(b)2/y6-5
1
TH(b)4 + CB(b)4/u3
1
TH(v)1/m6 R1 + HM(v)3/m5 R1
1
TH(v)1/m6 R1
1
TH(v)1 + CB(v)2/s6-7 R1
1
TH(v)1 + CR(b)2/s6
1
TH(v)1 + CR(b)2/s7
1
TH(v)1 + JR(v)1 + TF(v)1/s8 R1
1
TH(b)3 + MG(v)2/u3
1
TH(b)3 + CB(v)2/u3
1
TH(b)2 + MG(b)2/m5
1
TH(v)1/s-y9-7 R1
1
TH(b)2/m5
1
TH(v)2 + CR(b)2 + LL(b)2/m5-4
1
TH(v)2 + CR(b)2 + NR(b)2/m4
1
TH(v)1 + CR(b)2 + VO(b)2/y7-8
1
TH(v)1 + MG(v)1 + CB(v)2/s6-8 R1 1
TH(v)1 + CB(v)2/s8 R1
1
TH(v)2 + CR(v)3/r4-5
1
TU(b)5 + LL(b)5/u3
1
TU(b)6 + JU(b)5/u3
1
TU(b)2 + JU(b)1 + BM(v)1/y6-7
1
TU(b)2 + JU(b)1/y5
1
TU(b)3 + CT(b)3/m4
1
TU(b)2 + JU(v)3/m5
1
TU2 + JU2/m5
1
TU(b)3 + JU(b)3/m5
1
TU(v)2/m5-4
1
TU(b)2 + JU(b)3/m4-5
1
TU(b)3 + JU(b)3/m6
2
TU(b)2 + JU(b)2/m5-6
1
TU(v)1/y5-7
1
TU(b)2 + JU(b)1/m6
2
TU(b)3 + JU(b)3/m3-4
1
TU(b)2 + JU(v)1/y6
1
Area
(ha)
2109
6949
3067
15398
3048
1047
1178
889
12792
2260
9079
10060
14663
3337
9978
2674
380
16047
4100
17982
2464
579
1227
6655
3861
1596
2770
3927
15176
3074
3567
3867
343
8625
2852
2136
Dominant
soil
TF
TF
TH
TH
TH
TH
TH
TH
TH
TH
TH
TH
TH
TH
TH
TH
TH
TH
TH
TH
TU
TU
TU
TU
TU
TU
TU
TU
TU
TU
TU
TU
TU
TU
TU
TU
Depth to
bedrock
(m)
<1
1-2
1-2
<1
<1
<1
<1
<1
<1
1-2
1-2
1-2
<1
1-2
<1
<1
<1
<1
<1
<1
1-2
1-2
1-2
1-2
1-2
1-2
>2
1-2
<1
1-2
1-2
1-2
<1
1-2
1-2
1-2
Depth to
compact
(cm)
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
100
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
50
Drainage
W
W
I
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
W
I
P
W
W
W
W
W
W
W
W
W
W
W
W
W
W
StonFertility Flooding iness
m
N
S3
m
N
S3
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
h
N
S2
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
l
N
S3
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R0
B0
R1
B0
R1
B0
R1
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R1
B0
R1
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
Average
Slope
(%)
42.5
19.5
3.5
22.5
22.5
30
22.5
37.5
57.5
3.5
3.5
12
65
12
10
7
50
42.5
57.5
10
3.5
3.5
30
12
7
12
12
12
10
10
22.5
19.5
27
22.5
5.5
22.5
Surface
soil
texture
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
Parent
material
texture
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
l
CLI
Agriculture
6T
5T
3W
5TR
5TR
5TR
5T
6T
6T
2C
2C
4T
7T
4T
4TR
3TR
6T
6T
6T
4TR
4WD
5WD
5T
4T
3P
4T
4T
4T
4TR
4T
5T
5T
5T
5T
3P
5T
CLI
Forestry
3Fbs
3Fbs
3Fbs
4Rbs
4Rbs
4Rbs
3Fbs
3Fbs
5Rbs
3Fbs
3Fbs
3Fbs
5Rbs
3Fbs
3Fbs
3Fbs
5Rbs
4Rbs
5Rbs
3Fbs
4DWFbs
5WDbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
4DFbs
Tab le 5. Selected interp retations of soil map units cont’d
Map Unit Symbol
TU(v)2 + LL(v)2/m5
TU(b)2 +JU(b)2/m5
TU(b)2 + JU(b)2/m5-4
VO(b)5 + CT(b)5 + TT(v)5/u3
VO(v)4 + LL(v)4 + MG(b)2/u3
VO(v)3 + CR(v)3/m4
VO(v)2 + BO(v)1/y6-7
VO(b)3 + CR(b)3 + TH(b)2/m4
VO(v)3 + LL(v)3 + MG(v)3/s6
WA
No. of
polygons
1
1
1
1
1
1
1
1
1
44
Area
(ha)
8353
2489
2017
6267
4107
2228
805
10742
5619
5581
Dominant
soil
TU
TU
TU
VO
VO
VO
VO
VO
VO
WA
Depth to
bedrock
(m)
<1
1-2
1-2
1-2
<1
<1
<1
1-2
<1
>2
Depth to
compact
(cm)
50
50
50
40
40
40
40
40
40
n/a
Drainage
W
W
W
I
I
MW
MW
MW
MW
n/a
StonFertility Flooding iness
l
N
S3
l
N
S3
l
N
S3
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
m
N
S2
n/a
n/a
n/a
Notes: The depth recorded under “Depth to Compact” assumes that bedrock does not occur within the profile.
Boulder- Rockiness
iness
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
B0
R0
Average
Slope
(%)
12
12
10
3.5
3.5
7
30
7
22.5
n/a
Surface
soil
texture
l
l
l
l
l
l
l
l
l
n/a
Parent
material
texture
l
l
l
l
l
l
l
l
l
n/a
CLI
Agriculture
4TR
4T
4T
4DW
4DW
3DR
5T
3D
5T
-
CLI
Forestry
4DFbs
4DFbs
4DFbs
4DWbs
4DWbs
4Dbs
4Dbs
4Dbs
4Dbs
-
127
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Canadian Forestry Service, Maritime Forest Research
Centre, Fredericton, N.B.
Wang, C, Ross, G. J. and Rees, H. W. 1981.
Characteristics of residual and colluvial soils developed
on granite and of the associated pre-Wisconsin landforms
in north-central New Brunswick. Can. J. Earth Sci.
18(3):487-494.
W ang, C. and Rees, H. W . 1983. Soils of the
Rogersville-Richib ucto R egion of New B runswick. Ninth
Report of the New Brunswick Soil Survey. Research
Branch, Agriculture Canada and New Brunswick
Departm ent of A griculture and Rural Development,
Fredericton, New Brunswick. 239 pp.
Weeks, L. J. 1957. The Appalachian region. Pages 123205 in C. H . Stock well, editor. Geology and econ omic
minerals of Canad a, 4 th edition. Geol. Surv. Can. Econ.
Ser. No. 1.
W ein, R. W. and M oore, J. M. 197 7. Fire history and
rotations in the New Brunswick Acadian forest. Can. J.
For. Res. 7(2):285-294.
129
GLOSSARY - GENERAL TERMS*
ablation till A surfac e of loo se, permea ble somewhat,
stratified sandy and stony till usually overlying denser till.
chroma, color The relative purity, strength, or saturation
of a color (related to grayness).
acid soil A soil having a pH of 5.5 or lower (generally pH
4.0 to 5.5).
classification The systematic arrangement of soils into
categories on the basis of their characteristics.
alluvium
Material such as clay, silt, sand and gravel
depo sited by mod ern rivers and stream s.
clay As a soil separate, the mineral soil particles less than
0.002 mm in diameter: usually consisting largely of clay
minerals.
association, soil A natural grouping of soil or landscape
segments based on similarities in climatic o r physio graphic
factors and soil parent materials.
available rooting zone That depth of soil material which
is suitable for root growth and pene tration. Soil matrix bulk
densities of greater than 1.60 g/cm3 are considered a serious
limitation to root growth.
clay films (skins)
Coatings of oriented clays on the
surfaces of soil peds (natural unit of soil structure) and
mineral grains, and in so il pores.
coarse fragments Roc k fragm ents greater than 2 mm in
diameter, including gravels, cobb les, stones and bo ulders.
cobb les Rock fragments 7.5 to 25 cm in diameter.
ava ilable water The portion of water in a soil that can be
readily abso rbed by plant roots. It is the wate r held in the
soil against a pressure of 33 kPa to 1500 kPa, expressed in
centimetres of water per centimetre of soil, and reported on
a whole soil basis (soil <2 mm diameter, plus co arse
fragments).
complex, soil A mapping unit used in soil surveys where
two or more so il associations are so intima tely intermixed in
an area that it is impractical to separate them at the scale of
mapping used.
bedrock exposure
W hen the solid ro ck that usually
underlies soil is exposed at the surface or is covered by less
than 10 cm of unconso lidated material.
compact
Said o f any soil that has a firm or dense
consistence and whose particles are closely packed with very
little intervening space. Compact soils typically have a
matrix bulk density (particles less than 2 mm diameter) of
greater than 1.60 g/cm3.
bisequal Two sequa in one soil; that is, two sequences of
an eluvial horizon and its related illuvial horizon.
bog
Spha gnum or fore st peat m aterials formed in an
ombrotrophic environment due to the slightly elevated
nature of the bog tending to be disassociated from nutrientrich ground water or surrou nding minera l soils.
boulders Rock fragments greater than 100 cm in diameter.
bulk density The m ass of dry soil per unit bulk volume,
often expressed in g/cm3. In this report, the bulk density is
reported for the material <2 mm d iameter.
calcareous
A material containing sufficient calcium
carbonate, often with magnesium carbonate, to effervesce
visibly when treated with cold 0.1 N hydrochloric acid.
catena A nontaxonomic grouping of a sequence of soils of
about the same age, d erived from similar parent materials,
and occu rring under sim ilar climatic conditions, but having
unlike characteristics becau se of variations in relief and
drainage.
compaction (soil) Any process (such as by weight of
overburden or dessication) by which a soil mass loses pore
space and achiev es a higher density.
consistence The resistance of a material to deformation or
rupture. The degree of cohesion or adhesion o f the soil
mass. Terms used for describing consistence are for spe cific
soil moisture contents, i.e. moist soil: loose, very friable,
friable, firm, very firm.
control section The vertical section of soil upon which
classification is based. Typically 1 m in mineral soils and
1.6 m in organic soils, but less in cases o f shallow to
bedrock, and in the case of organic soils, shallow to a
mineral soil.
coprogenous earth A material in some organic soils that
contains at least 50% by volum e of feca l pellets less than 0.5
mm in diameter.
core zone The central regions of raised and blanket bogs.
* Source of most entries in Glossary - General Terms: Airphoto Analysis Associates Consultants Ltd. (1975); Research Branch, Canada Dept
of Agriculture (1976); and Soil Science Society of America (1978).
130
deglaciation The uncovering of a land area fro m be neath
a glacier or ice sh eet by the withdrawal of ice due to
shrinkage by melting.
deposit
Material left in a new position by a natural
transporting agent suc h as water, wind, ice or gravity.
drainage (soil) The frequency and duration of periods
when the soil is free of saturation.
eluviation The transportation of soil material in suspension
or in solution within the soil by the downward or lateral
movement of water.
ericaceous Pertaining to or like heath plants; belonging to
the heath family of plants.
esker A winding ridge o f irregularly stratified san d, gravel,
and cobbles deposited under the ice by rapidly flowing
glacial streams.
eutroph ic Said of an environment characterized by an
abundance of dissolved plant nutrients such as nitrogen,
potassium, phosphorus and calcium.
evapotranspiration The loss of water by evaporation from
the soil and by transpiration from plants.
fen Sedge p eat materials derived primarily from sedges
with inclusions of partially decayed stems of shrubs formed
in a eutrophic environment due to the clo se association of
the material with mineral-rich waters.
fibric Said of an organic soil material containing large
amo unts of weakly decomposed fiber whose botanical o rigin
is readily identifiable.
flaggs
shale.
Thin fragments of sandstone, limestone, slate or
flark zone Found in organic soils, it borders the core zone,
or central regions of raised and blanket bogs. The flark zone
is characterized by large parallel embankments formed by
rows of hummocks that surround the peat bog in a step-like
manner. Flashets (ponds) occur between the hummocks
oriented at right angles to the direction of the slope.
floodpla in Land bordering a stream, built up of sediments
from overflow of the stream and subject to inundation when
the stream is at flood stage.
fluvial depo sits All sediments, past and present, deposited
by flowing water, including glacio fluvial deposits.
fragipan A natural subsurface horizon having a higher
bulk density than the solum above; seemingly cemented
when dry, but showing moderate to weak brittleness when
moist.
geo mor phic Pertaining to the form of the Earth or o f its
surface features.
glacial drift A general term applied to all rock material
(clay, silt, sand, gra vel, cobbles, boulders) transported by a
glacier and deposited d irectly by or from the ice, or by
running water emanating from the glacier.
glaciation The alteration of a land surface by the massive
movement over it of glacier ice.
glacier A body of ice, consisting mainly of recrystallized
snow, flowing on a land surface.
glaciofluvial depo sits Material moved by glaciers and
subsequently sorted and deposited by streams flowing from
the melting ice.
glaciolacustrine Sediment generally consisting of stratified
fine sand, silt, and clay deposited on a lake bed. Glacial ice
exerted a strong but secondary control upon the mode of
origin in that glacier ice was close to the site of deposition.
glaciomarine Unconsolidated sorted and stratified depo sits
of clay, silt, sand , or gravel that have settled from
suspension in salt or brackish water bodies. Glacial ice
exerted a strong but secondary control upon the mode of
origin in that glacier ice was close to the site of deposition.
gleysation A soil-forming process, operating under poor
drainage conditions, which results in the reduction of iron
and other elements and in gray colors, and m ottles.
gra vel Rock fragments 2 mm to 7.5 cm in diameter.
groundw ater Water beneath the soil surface, usually under
conditions where the voids are completely filled with water
(saturation).
grus An accumulation of waste consisting of angular,
coarse-grained fragments resulting from the granular
disintegration of crystalline rocks (esp. granite).
horizon, soil A layer in the soil pro file approxim ately
parallel to the land surface with m ore o r less well-defined
characteristics that have been produced through the
operation of soil forming pro cesses.
hum ic Said of an organic soil material containing large
amo unts of highly decomposed organic materials with little
identifiable fiber.
hummo cky A very complex sequence of slopes extending
from somewhat rounded depressions or kettles of various
sizes to irregular to conica l knolls and knobs.
illuviation The process of depositing soil material removed
from one horizon in the soil to another, usually from an
131
upper to a lower horizon in the soil profile. Illuviated
substances include silicate clay, hydrous oxides of iron and
aluminum, and organic matter.
impeded drainage A condition that hinders the movement
of water by gravity through so ils.
inclusion A soil type found within a mapping unit that is
not extensive enoug h to be map ped separately or as part of
a complex.
kame An irregular rid ge or hill of stratified glacial drift
deposited by glacial meltwater.
lacustrine
Material deposited in lake water and later
exposed by either lowering of the water level or by uplifting
of the land. These sediments range in texture from sands to
clays.
lagg The areas at bog edge s adja cent to mineral soil where
waters flow or stagnate.
land type Natural and man-made units in the landscape
that are either highly variable in content, have little or no
natural soil, or are excessively wet.
landform The various shapes of the land surface resulting
from a variety of actions such as deposition or
sedimentation, erosion, and earth crust movements.
lithology The description of rock fragments on the basis of
such characteristics as color, structure, mineralogic
composition and grain size.
lodgment till
Material deposited from rock debris in
transport in the base of a glacier. As it is “plastered” into
place, this till is compact and not sorted.
mineral soil
A soil consisting predominantly of, and
having its properties determined pred ominantly by, mineral
matter. It contains less than 30% organic matter (17%
organic carbon), except for an organic surface layer that may
be up to 60 cm thick.
mode of deposition
The method whereby soil parent
material has be en left in a ne w po sition b y a natural
transporting agent such as water or ice.
moder A forest humus form (litter layer), especially under
northern hardwoo ds, where the mixing of organic and
mineral particles is purely mechanical with no formation of
true organo mineral com plexes. The mixing is due to
micro arthropod activity.
mor A type of forest humus (litter layer) in which the
organic forest floor layer is present and there is prac tically
no mixing of the surface organic matter with mineral so il.
The transition from organic to m ineral ho rizon is abrupt.
moraine A mound, ridge or other distinct accumulation of
unsorted, unstratified glacial drift, predo minan tly till,
deposited chiefly by direct action of glacier ice in a variety
of topographic landforms that are independent of control by
the surface on which the drift lies.
mottles Irregularly marked spots or streaks, usually yellow
or orange but sometimes blue, that indicate poor aeration
and lack of good drainage. They are described in terms of
abundance, size and contrast.
mull
A humus form in which there is extensive
decomposition of forest litter and intimate association of
colloidal organic matter with mineral soil. A forest mull
implies a stead y state of faunal activity with regular passage
of organic matter and mineral particles through the guts of
earthworms. Diag nostic o rganic layers are lacking.
neutral soil A soil wh ich is neithe r acid or alka line in
reaction, typically considered pH 5.5 to 7.5.
non soil The collection of soil material or soil-like material
that does not meet the definition of soil. Nonsoil includes
soil displaced by unnatural processes, unconsolidated
material unaffe c te d by s oil-forming p rocesses,
unconsolidated mineral or organic material thinner than 10
cm overlying bedrock, and soils covered by more than 60
cm of water.
omb rotroph ic Said of an environment characterized by a
shortage of plant nutrients due to a disassociation from
nutrient-rich waters.
organic matter The organic fraction of the soil; includes
plant and animal residues at various stages of
decomp osition, cells and tissues of soil organisms, and
substances synthesized by the soil population.
org anic soil
Organic so ils consist o f peat d epo sits
containing more than 30% organic ma tter by weight (17%
organic carbon) and are usually greater than 40 to 60 cm
thick.
outw ash Sediments washed out by flowing water beyond
the glacier and laid dow n as stratified beds with particle
sizes ranging from bo ulders to silt.
overburden
The loose soil or o ther unconsolidated
material overlying bedrock.
paludification The process of peat formation.
parent material The unconsolida ted and m ore or less
chem ically weathe red m ineral or orga nic matter from which
the solum of a soil has develop ed by soil forming processes.
par ticle size class Refers to the grain size distribution of
the whole soil including the coarse fraction. It differs from
132
texture, which refers to the fine earth (<2 mm) fraction only.
In addition, textural classes are usu ally assigned to sp ecific
horizons whereas particle-size classes indicate a compo site
particle size of all or a part of the control section. See
particle size classes triangle below.
polygon Any delineated area shown on a soil m ap that is
identified by a symbol.
pores, macro Soil voids that are readily drained of free
water, based on water retention at 100 cm of water suction.
Herein considered on a whole soil basis (soil <2 mm
diameter, plus coarse fragments).
pores, micro Soil voids that are not readily drained of free
water, based on water retention at 100 cm of water suction.
Herein considered on a whole soil basis (soil <2 mm
diameter, plus coarse fragments).
porosity, total The total spa ce no t occupied by solid
particles in a bulk volume of soil. Herein considered on a
whole soil basis (soil <2 mm diameter, plus coarse
fragments).
post glacial Pertaining to the time interval since the total
disappearance o f continental glaciers.
profile, soil A vertical section of the soil through all its
horizons and extending into the parent material.
peat Unconsolidated soil material consisting largely of
organic matter.
reaction, soil The degree of acidity or alkalinity of a soil,
usually expressed as a pH value.
pedoge nic Pertaining to soil formation.
regolith The unconsolidated mantle of weathered rock and
soil material overlying solid rock.
pedology The aspects of soil science dealing with the
origin, morpho logy, genesis, distribution, mapping, and
taxonomy of soils, and classification in terms of their use.
reworked
Descriptive of material modified after its
preliminary deposition, commonly by water.
perhum id A soil moisture regime that experiences no
significant water d eficits in the growing season. Water
deficits are less than 2.5 cm.
permeability, soil The e ase with which gases and liquids
penetrate or pass through a bulk mass of soil or a layer of
soil.
rockiness Defined on the basis of the percentage of the
land surface occupied by bedrock exp osures.
sand A soil particle between 0.05 and 2.0 mm in diameter.
saturated hydraulic conductivity
The effective flow
veloc ity or discharge velocity in saturated soil at a unit
hydraulic gradient. An approximation of the permeability of
the soil, expressed in centimetres per hour.
perviousness See: perme ability.
petrology Deals with the origin, occurrence, structure and
history of rocks.
seepage The down-slope horizontal movement of water
within the soil profile on top of a layer of restricted
perm eability.
pH, soil
The negative logarithm of the hydrogen-ion
activity of a soil. The degree of acidity or alkalinity of so il
expressed in terms of the pH scale.
series, soil The basic unit of soil classification consisting
of soils that are essen tially alike in all major profile
characteristics except surface texture.
phase, soil A subdivision of a soil association or other unit
of classification having characteristics that affect the use and
management of the soil, but that do not vary sufficiently to
differentiate it as a separate association.
silt A soil separate consisting of particles between 0.05 and
0.002 mm in diameter.
physiography The physical geography of an area dealing
with the nature and o rigin of topographic features.
soil The unconsolidated material on the immediate surface
of the earth that serves as a natural me dium for the growth
of land plants and that has been influenced by soil forming
factors.
133
soil-forming factors Natural agenc ies that are respo nsible
for the formation of soil: parent rock, climate, organisms,
relief (drainage) and time.
terric Refers to a mineral layer und erlying an organic soil.
The mineral layer occurs within a depth of 160 cm from the
surface.
soil map A map showing the distribution of soil types or
other soil mapping units in relation to the prominent
physical and cultural features of the earth’s surface.
texture, soil The relative propo rtions of the vario us soil
separates (sand, silt and clay) in a soil. See texture classes
triangle below.
soil survey The whole proce dure involved in making a soil
resource inventory.
The systematic examination,
description, classification, map ping and interpreting of soils
and soils data within an area.
solum The upper horizons of a soil in which the parent
material has been modified and in which m ost plant roots are
contained. It usually consists of the A and B horizons.
sorted Said of an unconsolidated sediment consisting of
particles of essen tially uniform size or of particles lying
within the limits of a single grade or class.
stones Rock fragments greater than 25 cm in diameter.
stoniness, surface Defined on the basis of the percentage
of the land surface occupied by fragments coarser than 25
cm in diameter.
stratified materials Unconsolidated sand, silt and clay
arranged in “strata” or layers.
structure, soil The combination or arrangement of primary
soil particles into second ary particles, units or peds. These
peds are characterized and classified on the basis of size,
shape and degre e of distinctness.
surface expression The form (assemblage of slopes) and
pattern of forms in a landscape.
swamp A peat-covered or pe at-filled area with the water
table at or above the peat surface. The dominant peat
materials are mesic to humic forest a nd fen peat fo rmed in
a eutrophic environment resulting from strong water
movement from the m argins or other m ineral sources.
till Unstratified glacial material deposited directly by the
ice and consisting of clay, sand, gravel and boulders
intermingled in any proportion.
value, color The relative lightness or intensity of color.
veneer A thin layer of soil material from 10 cm to 1 m in
thickness which does not mask minor irregularities in the
underlying unit’s surface, which is often bedrock.
134
135
GLOSSARY - ROCK TYPES*
argillite A compact rock de rived from either mudstone
(claystone or siltstone) or shale, that has undergone a
somewhat higher degree of induration than is present in
mudstone or shale but that is less clearly laminated than, and
without the fissility (either parallel to bedding or otherwise)
of shale, or that lacks a cleavage distinctive of slate.
arkose A feldspar-rich, typically coarse-grained sandstone,
com mon ly pink or red dish to pale gray or b uff, composed of
angular to subangular grains that may be either poorly or
moderately well sorted , usually de rived from the rapid
disintegration of granite or granitic rocks.
basa lt
A dark- to medium-dark colored, comm only
extrusive, mafic igneous rock composed chiefly of calcic
plagioclase and clinopyroxene in a glassy or fine-grained
groundmass (the extrusive equivalent of gabbro)
basic Said of an igneous rock having a relatively low silica
content, sometimes delimited arbitrarily as less than 54%,
e.g. gab bro, basalt
calcareous
Said of a substance that contains calcium
carbonate (CaCO 3). When applied to a rock name it implies
that a considerable percen tage (up to 5 0% ) of the ro ck is
calcium carbonate
calcite A common rock-forming mineral: CaCO 3; usually
white, colorless or pale shades of gray, yellow or blue
conglomera te A coarse-grained clastic sedimentary rock
composed of rounded (to subangular) fragments larger than
2 mm in diameter (granules, pebb les, cobbles, boulders) set
in a fine-grained m atrix of sand, silt or any of the common
natural cementing materials (such as calcium carbonate, iron
oxide, silica, or hardened clay) (the consolidated equivalent
of gravel).
diorites
A group of plutonic rocks intermed iate in
com pos iti o n betwe en ac idic an d ba sic rocks,
chara cteristically com posed of dark-colored amphibole (esp.
hornblende), acid plagioclase, pyroxene and sometimes a
small amount of quartz.
felsic Applied to an igneous rock having light-colored
minerals in its mode. It is the opposite of mafic.
gabbro A group of dark-colo red, basis intrusive igneous
rocks com posed principa lly of basic plagio clase and
clinopyroxene
gneiss A foliated rock formed b y regional metam orphism
in which b ands or lenticles or granular minerals alternate
with bands and lenticles in which min erals having flaky or
elongate prismatic habits predominate.
granites
A term loosely applied to any light-colored
coarse-grained plutonic rock (pertaining to igneous rocks
formed at great depth) containing quartz as an essential
com pon ent, along with feldsp ar (usually white of nearly
white and clear and translucent) and mafic (dark-colored
minerals) minerals
granite gneiss A gneiss derived from a sedimentary or
igneous rock and having a granite mineralogy.
granodiorites A gro up of coarse-grained plutonic rocks
intermediate in composition between quartz diorite and
quartz monzonite.
greyw acke
A dark (usually gray o r greenish gray,
sometimes black) and very hard, tough and firmly indurated,
coarse-grained sandstone that has a subconchoidal fracture
and consists of poorly sorted and extremely angular to
subangular grains of quartz and feldspar with an abundant
variety of small, dark rock and mineral fragments embedded
in a preponderant and compact, partly metamorphosed
clayey matrix having the general composition of slate and
containing an abundance o f very fine-grained micaceous and
chloritic minerals.
igneous Rock form ed fro m the cooling and solidification
of magma, and that has not been changed appreciably since
its formation
limestone A sedimentary rock consisting chiefly (more
than 50% by weight or by areal percentage under the
microscope) of calcium carbonate, primarily in the form of
mineral calcite, with or without magnesium carbonate.
mafic Said of an igneous rock composed chiefly of one or
more ferromagnesium, dark-colored minerals in its mode.
It is the opposite of felsic.
meta basalt Metamorposed mafic rock which has lost all
traces of original texture and mineralogy d ue to comp lete
recrystallization
metagabbro Metamo rphosed gabbro
metagreyw acke Metamo rphosed greywacke
* Source of most entries in Glossary - Rock Types: Gary, M., Mc Afee, R. and W olf, C. L. (eds) (197 2).
136
meta mor phic Rock derived from pre-existing rocks but that
differ from them in physical, chemical and mineralogical
properties as a result of natural geological pro cesses,
principally heat and pressure, originating within the earth.
The pre-existing rocks may have been igneous, sedimentary
or another form of metamorphic rock.
shales A fine-grained, indurated, detrital sedimentary rock
formed by the consolidation (as by compress ion or
cementation) of clay, silt or mud, and characterized by finely
stratified (Laminae 0.1-0.4 mm thick) structure and/or
fissility that is approximately parallel to the bedding (along
which the rock breaks readily into thin layers)
quartzite A very hard but unmetamorphosed sandstone
consisting chiefly of sand grains that have b een comp letely
and solidly cemented with secondary silica that the rock
breaks across or through the individual grains rather than
around them
siltstone An ind urated or somewhat indurated silt having
the texture and composition, but lacking the fine lamination
or fissility, of slate; a massive mudstone in which the silt
predominates over clay (intermediate between sandstone and
shale)
rhy olite A gro up of extrusive igneous rocks, gene rally
porphyritic (large crystals) and exhibiting flow texture, with
phenocrysts of quartz and alkali feldspars (esp. orthoclase)
in a glassy to crypto crystalline groundma ss (the extrusive
equivalent of granite)
slate A compact fine-grained metamorphic rock formed
from such ro cks as shale and volcanic ash, which possesses
the property of fissility along planes independent of the
original bedding (slaty cleavage).
sandstone A medium-grained clastic sedimentary rock
composed of abundant and rounded or angular fragments of
sand size set in a fine-grained m atrix (silt or clay) and more
or less firmly united by a cementing material (commonly
silica, iron oxide or calcium carbonate); the consolidated
equivalent of sand, intermediate in texture between
conglomerate and shale.
schist
A strongly foliated crystalline rock formed by
dynamic metamorphism which can be read ily split into thin
flakes or slabs due to the well developed parallelism of more
than 50% of the minerals present, particularly those of
lamellar or elongate prismatic hab it, e.g., mica, hornblende
sedimentary Rock form ed fro m ma terials deposited from
suspension or precipitated from solution and usually being
more or less consolidated. The principal sedimentary rocks
are sandstone, shales, limestones and conglom erates.
trachyte A group of fine-grained, generally porphyritic,
extrusive rocks having alkali feldspar, minor mafic m inerals
(biotite, hornblend e or p yroxene) as the main com pon ents
tuff A compacted deposit of volcanic ash and dust that may
or may not contain up to 50% sediments such as sand or
clay.
volcanics A generally finely crystalline or glassy igneous
rock resulting from volcanic actio n at or near the Earth’s
surface, either ejected explosively or extruded as lava.
137
APPENDIX - COMMON AND SCIENTIFIC NAMES OF TREES
a ld e r , s p e c k l e d
a s h , b l a ck
a s h , m o u n ta in ( A m e ric a n )
a sh , w h ite
a s p e n , l a r g e - t o o th
a s p e n , tr e m b lin g
b e e c h , A m e r ic a n
birch , gray or w ire or fire
b i rc h , w h ite o r p a p e r
b ir c h , y e llo w
c e d a r , e a st e r n w h ite
c h e rry , p in
e lm , w h i t e
f ir , b a l sa m
he m lock , eastern
la r c h , A m e r ic a n
m a p l e , m o u n t a in
m aple, red
m a p l e , s tr ip e d
m aple, sugar
o a k , re d
p in e , e a st e r n w h ite
p i n e , ja c k
pine, red
p o p la r
p o p la r , b a l sa m
s p r u c e , b l a ck
spruce, red
sp ru c e , w h ite
ta m a r a c k
w illo w
`
Alnus rugosa ( D . R . ) S p r .
Fraxinus nigra M a rs h .
Sorbus americana M a rs h .
Fraxinus americana L .
Populu s grandid entata M ic h x .
Populus tremuloides M ic h x .
Fagus gran difolia E h r h .
Betu la po pulifolia M a rs h .
Betula papyrifera M a rs h .
Betu la alleg han iensis B ritt.
Thu ja occiden talis L .
Prunus pensylvanica L .
Ulmus americana L .
Abies balsamea (L .) M ill.
Tsug a canad ensis ( L . ) C a r r .
Larix laricina ( D u R o i) C . K o c h .
Acer spicatum L a m .
Acer rubrum L .
Acer pensylvanicum L .
Acer saccharum L .
Quercus rub ra L .
Pinus strobus L .
Pinus banksiana L a m b .
Pinus resinosa A it.
Populus L .
Populus balsamifera L .
Picea mariana ( M i ll .) B S P .
Picea rubens S a r g .
Picea glauca ( M o e n c h ) V o s s
Larix laricina ( D u R o i) C . K o c k .
Salix L .