NJDEP - NJGWS - Geologic Map Series GMS 12

Transcription

20
30
40
MIS 2
MIS 4
MIS 3 ecbr
Figure 3. Marine Isotope Stage (MIS) curve (modified
from SPECMAP curve, in Carey and others, 1998, after
Imbrie and others, 1984) showing the marine oxygenisotope curve for the last 150,000 years and the marine
isotope stages (MIS) which are referenced on the map
and in the text.
25
19.9 m (65.2 ft)
30
24.3 m (79.6 ft)
MIS 3 barrier sands
MIS 2
28.7 m (94 ft)
40
33.1 m (108.5 ft)
-80
pr
LEGEND
SF
MIS
VE
BP
ms
TWTT
328
ox
RES3
.2
22
0o
Seafloor
Marine Isotope Stage
Vertical exaggeration
Before present (1950 A.D.)
Miliseconds seismic velocity
Two-way travel time
Wellner and others (1993) shotpoint
mi
MIS 5 channels incising
MIS 5 bay facies
0
-50
Salt-marsh and estuarine deposits
Holocene
Qtl
Lower stream terrace deposits
late Pleistocene, late Wisconsinan
1
0
Seismic profile line
Bathymetric contour (in feet),
blue at -30’ elevation, all
others gray. Contour interval
10 feet
Point along Cross Section
Line CC’
NJGWS vibracore
Qcm2
Cape May Formation, Unit 2
late Pleistocene
Qtu
Upper stream terrace deposits
middle to late Pleistocene
Qcu
Upper colluvium
middle Pleistocene
Qcm1
Cape May Formation, Unit 1
early (?) to middle Pleistocene
TQg
Upland gravel, lower phase
late Pliocene to middle Pleistocene
Tg
Upland gravel
late Miocene to Pliocene
Tch
Cohansey Formation
late middle Miocene
Wellner and others (1993)
vibracore
Snedden and others (1994)
vibracore
Wellner and others (1993)
seismic shotpoint
1
2
3
3
4
4
5 km
scale: 1:80000
SEISMIC PROFILE
Jane Uptegrove1, Jeffrey S. Waldner1, Scott D. Stanford1, Don H. Monteverde1,
Robert E. Sheridan2, and David W. Hall1
Qal
Qcm1
UNDIFFERENTIATED SEDIMENTS (pre-Sangamonian) -- Contains 1)
unsampled material as much as 10 ft thick underlying the MIS 5 sediments, and 2)
southeast-dipping (Miocene) Coastal Plain deposits. These sediments are beyond
NJGWS vibracore sampling depth throughtout the map area and are identified
solely by stratigraphic relationship to overlying deposits.
TQg
DESCRIPTION OF ONSHORE MAP UNITS
Tg
ALLUVIUM (late Pleistocene and Holocene) – Sand, gravel, silt, minor clay and
peat; yellowish brown, brown, gray. Contains variable amounts of organic matter.
Deposited in modern floodplains and channels. As much as 20 feet thick.
Tch
Qs
FRESHWATER WETLAND DEPOSITS (late Pleistocene and Holocene) – Peat
and organic clay, silt, and sand. As much as 10 feet thick. Deposited in modern
freshwater wetlands.
SALT-MARSH AND ESTUARINE DEPOSITS (Holocene) – Silt, sand, peat, clay,
minor pebble gravel; brown, dark-brown, gray, black. Contains abundant organic
matter. As much as 40 feet thick. Deposited in salt marshes, estuaries, and tidal
channels during Holocene sea-level rise.
LOWER STREAM TERRACE DEPOSITS (late Pleistocene, late Wisconsinan)
— Sand, pebble gravel, minor silt; yellow, white, light gray. As much as 25 feet thick.
Form terraces and fans with surfaces 5 to 10 feet above modern flood plains and
wetlands. Laid down chiefly during the late Wisconsinan glacial maximum, between
about 25 and 15 ka.
Two-way travel time (TWTT)
below sea floor (ms)
SF
20
Core 12
MIS 2
25
MIS 4
10
30
35
MIS 6
15
40
CAPE MAY FORMATION, UNIT 2 (late Pleistocene) – Sand, pebble gravel, minor
silt, clay, peat, and cobble gravel; very pale brown, yellow, white, gray. As much as
25 feet thick. Forms a marine terrace with surface altitude up to 30 feet.
CAPE MAY FORMATION, UNIT 1 (early (?) to middle Pleistocene) – Sand, and
pebble gravel, minor silt, clay; very pale brown, yellow, reddish yellow. As much as
30 feet thick. Forms a marine terrace with surface altitude up to 65 feet.
UPLAND GRAVEL, LOWER PHASE (late Pliocene - middle Pleistocene) –
Sand, clayey sand, and pebble gravel, minor silt; yellow to reddish yellow. As much
as 20 feet thick. Includes fluvial and minor colluvial deposits in erosional remnants
capping lower uplands and interfluves. Grades in places to the Cape May Formation, unit 1.
UPLAND GRAVEL (late Miocene - Pliocene) – Sand, clayey sand, pebble gravel,
minor cobble gravel; yellow to reddish yellow. Locally iron-cemented. As much as
20 feet thick. Includes fluvial and minor colluvial deposits in erosional remnants
capping hilltops and interfluves.
COHANSEY FORMATION (late middle Miocene) – Quartz sand, white, yellow,
very pale brown; minor white, red, yellow clay. Includes thin, patchy alluvium and
colluvium, and pebbles left from erosion of surficial deposits.
New Jersey Geological and Water Survey
Department of Earth and Planetary Studies, Rutgers University
27
522
27a
24a
26
26a
Miocene
late Pleistocene
MIS 5 bay facies
MIS 5 cbms MIS 5 Channel and baymouth sand
deposits
late Pleistocene
~
> MIS 6 u
>MIS 6 undifferentiated sediments
Miocene to middle Pleistocene;
units older than MIS 6, including
undifferentiated coastal plain
units
~
>MIS 6 u
>MIS 6 undifferentiated sediments; coastal
plain units not in outcrop in offshore map
area; imaged at depth but not differentiated
on seismic profiles; Kirkwood Formation
penetrated at 78 ft depth in the Island Beach
Borehole (C11 on cross-section CC',
Permit # 33-31139)
Miocene to middle Pleistocene;
units older than MIS 6, including
undifferentiated coastal plain
units
> MIS 6 u
MIS 5 cbms
ap
pro
x.
MIS 4
8.8
21 mi (
14
5o
.1
km
Core 16
)
Corrected Water Depth
of Core 16 = 61 ft (18.6 m)
MIS 6
GRAIN SIZE CURVE
median grain size (phi)
5 4 3 2 1 0 -1
0.0
5.7
6.0
phi
mm
-2
-1
0
1
2
3
4
5
4.0
2.0
1.0
0.5
0.250
0.125
0.062
0.031
0.3
1.2
1
AAR age:
OIS 5c-5e
1.5
AMS C-14:
44,210 =/1080 BP
2.1
2
3
1.8
2.4
2.7
3.0
3.3
3.6
3.9
4.2
4.5
4
5.1
AMS C-14:
>49,870 BP
5.4
AAR age:
OIS 3c
5
median grain size (mm)
air pocket
6
depth
6.04 m
MEDIAN
GRAIN SIZE
ID-depth phi
12000
12030
12060
12090
12120
12150
12180
12210
12240
12270
12300
12330
12360
12390
12420
12450
12480
12510
12540
12570
12600
4.8
EXPLANATION
GRAIN SIZE
LITHOLOGY
gravel
CL clay
ST silt
pea gravel
VF very fine sand
coarse sand
F fine sand
medium sand
M medium sand
fine sand/silt
C coarse sand
clay
VC very coarse sand
clay clast
G gravel
shells/
shell fragments
burrows
charcoal or lignite
roots or twigs
ST F C G
CL VF M VC
-0.32
0.30
0.41
0.80
0.82
1.20
1.27
1.30
1.51
1.17
1.96
1.90
1.52
1.51
1.65
1.62
1.49
1.55
1.51
1.51
1.51
Depth in
core (m)
Core #
Material
Lab #
Dating Method
Age
15
4
charcoal
GX-27722
conventional radiocarbon
31,600 +9760/-4280 BP
12
4.18
charcoal
GX-27719-AMS
AMS
>49,870
12
4.95
Spisula
JW2000-057
AAR
MIS 3
17a
3.85
Spisula
JW2000-040
AAR
MIS 3
18
6
peat
GX-27721-AMS
AMS
48,890 +/-3360 BP
18
5.85
Spisula
JW2000-043
AAR
MIS 5
MIS 5 bay facies
>MIS 3 ecbr
Table 2. Five dated samples from the two deeper stratigraphic units. AMS - accelerator mass
spectrometry due to small size of sample; AAR - amino acid racemization.
Crosssection #
Well Name
Well
permit #
Topo ID
Date of
drilling
Reported elevation Depth of
of well (ft)
core (ft)
Geophysical
logs
Dated
material
Reference
(on file at NJGWS)
C1
Ship Bottom
53-00052
Ship Bottom
1973
7
992
g, sp, r
no
C2
Stafford MUA
33-10547
Ship Bottom
1982
10
521
g
no
C3
Surf City
33-25686
Ship Bottom
1989
~10
574
g,r
no
Layne New York
C4
Surf City
33-1091
Ship Bottom
1964
<10
557
g
no
Murtha, well permit
C5
Surf City
33-1268
Ship Bottom
1970
<10
564
g, sp, r
no
Shultes, well permit
C6
AT and T long lines
33-967
Ship Bottom
1961
~10 (spudded in fill?)
460
g, sp, r
no
C7
Ship Bottom #1
NA
Ship Bottom
NA
20
96
no
2 radiocarbon
Newell et al., 1995
C8
Boro of Barnegat Light
33-6678
Long Beach
1979
<10
641
g, sp, r
no
Shultes, well permit
C9
Boro of Barnegat Light
33-7876
Long Beach
1980
5.5+
658
g, sp, r
no
USGS well logs
C10
Core 3, Wellner and others, 1993
NA
NA
1988
-30.8
1 radiocarbon
C11
Island Beach Core hole
ODP Leg 150X
33-31139
Barnegat Light
1993
12
2 radiocarbon
in this section
8.5
1223
g, dens, neutron,
caliper, etc.
B’
USGS well logs
SW
MIS 5 bay facies
GRAIN SIZE CURVE
5 4 3 2 1 0 -1 -2
0
20
SF
5
10
MIS 2
MIS 4
20
25
30
35
15
MIS 6
EXPLANATION
GRAIN SIZE
LITHOLOGY
gravel
CL clay
ST silt
pea gravel
VF very fine sand
coarse sand
F fine sand
medium sand
M medium sand
fine sand/silt
C coarse sand
clay
VC very coarse sand
clay clast
G gravel
shells/
shell fragments
burrows
charcoal or lignite
roots or twigs
5.1
5.4
phi
mm
5.7
-2
-1
0
1
2
3
4
5
4.0
2.0
1.0
0.5
0.250
0.125
0.062
0.031
0.3
Core 13
40
0.6
0.9
1
1.2
1.5
1.8
2
MIS 2
reflector
3
2.1
2.4
2.7
3.0
3.3
3.6
3.9
4.2
4.5
4
4.8
6.0
5
AAR date:
OIS 5c-5e
6
depth
5.9 m
-1.01
-1.19
-1.3
-0.96
-1.2
4.4
0.13
4.25
4.34
4.2
-0.62
-0.12
0.59
0.5
0.7
0.7
0.62
0.63
0.18
0.88
13000
13030
13060
13090
13120
13150
13180
13210
13240
13270
13300
13330
13360
13390
13420
13450
13480
13510
13540
13570
0.0
SEISMIC PROFILE
MEDIAN
GRAIN SIZE
ID-depth phi
median grain size (mm)
ST F C G
CL VF M VC
Figure 5. Core 13 Composite. Driller’s water depth (corrected): 15.5 m (50.7 ft). Five-digit numbers in the left-hand column of the
Median Grain Size table are sample ID-depth numbers. The first two digits are the Core ID number (13); the last three digits are the
sample depth in centimeters (0 - 570). Lithology colors represent observed colors at time of core processing. Color differences
among units are accentuated to distinguish lithologies.
C
C1
0
C2
H2O
Qs
100
Qmm~MIS 1be
possible MIS 3
bay sediments
18
59
128
SECTION
AA'
C6
H2O
C7
Qs
Qs
C8,C9
H2O
Qbs~MIS 1brs
C’
C10
Qmm~MIS 1be
H2O
C11
Qmm~MIS 1be
34,890+/-960
4532+/-58
Qcm2~MIS 5
Qmm~MIS 1be
Qmm~MIS 1be
8810+/-170
Qmm~MIS 1be
10
5625+/-200
Qcm2~MIS 5
>MIS 6
possible MIS bay sediments
20
The views and conclusions contained in this document are those of the authors and
should not be interpreted as necessarily representing the official policies, either
expressed or implied, of the U. S. Government.
50
>MIS 6
30
0
0
0
Qbs~MIS 1brs
Qbs~MIS 1brs
>MIS 6
Research supported by the U. S. Geological Survey, National Cooperative Geologic
Mapping Program, under USGS award number G09AC00185.
Explanatory pamphlet accompanies map
GIS/Cartography by Z. Allen-Lafayette
24 SF
39
0
Offshore bathymetry for figure 1 modified from National Oceanic and Atmospheric
Administration NJGWS Coastal Relief Model Development digital file.
39
48
Section CC’, correlation of gamma logs and lithologic logs, from the upper sections of onshore wells and boreholes and inlet vibracore, extending
from Ship Bottom on Long Beach Island to the Island Beach corehole. Red lines show gamma response, with intensity increasing to the right.
Onshore base map for figure 1 from USGS topographic quadrangles: Forked River,
1989; NJ, Long Beach, NJ, 1951, photorevised 1972; Ship Bottom, NJ, 1952,
photorevised 1972; Beach Haven, NJ, 1951, photorevised 1972; and Barnegat
Light, NJ, 1989.
12
Miller and others, 1994
Island Beach Site Report
ODP, Vol 150X
possible MIS 3
bay sediments
30
16
105
Qcm2~MIS 5
>MIS 6
20
32
>39,000
Qcm2~MIS 5
20
6
40
C3 C4 C5
Qmm~MIS 1be
8
Wellner and others, 1993
Qtl
Qbs~MIS 1brs
50
Qbs~MIS 1brs
0
82
Qtl
0
10
Qs
H2O
0
25
Figure 4. Core 12 Composite. Driller’s water depth (corrected): 20.6 m (67.4 ft). Five-digit numbers in the left-hand column of the
Median Grain Size Table are sample ID-depth numbers. The first two digits are the Core ID number (12); the last three digits are the
sample depth in centimeters (0 - 600). Lithology colors represent observed colors at time of core processing. Color differences
LITHOLOGY
CL VF M VC
ST F C G
0
32
Table 3. Identification of wells in Section CC’.
UPPER COLLUVIUM (middle Pleistocene) – Sand, and pebble gravel; pale
brown, yellow, reddish yellow. As much as 20 feet thick. Forms aprons graded to
upper terraces.
2
MIS 3 Estuarine, channel and barrier sand
deposits
~
15
5
UPPER STREAM TERRACE DEPOSITS (middle to late Pleistocene) – Sand
and pebble gravel; yellow, reddish yellow, yellowish brown. As much as 20 feet
thick. Forms stream terraces with surfaces 20 to 50 feet above the modern floodplain. Terraces grade to, or are onlapped by, the Cape May Formation, unit 2
1
Tch
Depth (ft)
>MIS 6 u
CHANNEL AND BAYMOUTH DEPOSITS (Sangamonian) – Sand is coarse to very
fine, dark, yellowish-brown to brown, compacted. Sparse shell fragments are
stained light-brown to brown. Silt and clay are minor constituents. This unmapped
subcrop underlies MIS 3 sediments. It is as much as 60 ft thick, in water depths of
70 to 130 ft. Correlates with the onshore Qcm2.
BEACH AND NEARSHORE MARINE SAND (Holocene) – Sand and shell
fragments, minor pebble gravel, very pale brown to light gray. As much as 30 feet
thick. Deposited during Holocene sea-level rise.
CAPE MAY FORMATION (Salisbury and Knapp, 1917) – Estuarine, beach, and
nearshore marine deposits laid down during two or more sea-level highstands in
the Pleistocene. Divided into three units based on marine-terrace elevation. Two of
these units are mapped in this area.
Qcm2
Pliocene
Chart 1. Correlation of map units
15
Qcu
>MIS 6 u
Tg
Depth (m)
MIS 5 cbms
ESTUARINE, CHANNEL, AND BARRIER DEPOSITS (Wisconsinan) -- Sand,
gravel, and compacted clay. Sand is medium to coarse. Horizontally-bedded gravel
and clay are erosion-resistant. Locally, where capped by younger MIS 2/1 sand,
MIS 3 sand is preserved between the younger sand and the underlying gravel/clay
units. Sand and gravel are light- brown or gray to yellowish-brown to dark-orange
(typically oxidized). In many of the NJGWS vibracores that penetrate this unit, a
gravel sub-unit about 1.5 ft thick caps the unit as a whole, and forms the basal
surface on which the MIS 2/1 interbedded unit is deposited. Shell fragments occur
in small amounts, typically clustered in thin layers (~1 to 3 inches). Shells may be
stained by oxidation. Compacted clay layers may also contain shell hash layers.
Unit is as much as 40 ft thick, in water depths of 30 to 95 ft.
Qtu
Holocene
0.9
from sea surface (ms)
MIS 3 ecbr
BAY/ESTUARINE DEPOSITS (Holocene) -- Interbedded sand, silt, and clay; silt is
dark-gray, grayish-brown; clay is greenish-gray to very dark gray/black. Organic
material is in some of the clays, typically as isolated stems, leaves or peat fibers. In
rare cases, this organic material is suitable for radiocarbon dating (see text and
figures). This unit typically is 6 to 8 ft thick and underlies the MIS 1 brs unit, in water
depths of 40 to 75 ft. The interbedded unit may contain burrows. The clay interbeds
may contain shell fragments and or shell hash. Correlates with the onshore Qmm.
early Pleistocene
Depth (ft)
MIS 1 be
Qtl
520
Qcm1
>MIS 6 u
Depth (m)
EXPLANATION
BARRIER/SHOAL DEPOSITS (Holocene) -- Sand, light-gray to brownish-gray,
predominantly medium- to fine-grained, with small amounts coarse sand and pea
gravel. Shells are common to abundant and are distributed in the upper sand unit
as whole shells or as fragments. Total thickness of the unit is as much as 20 feet
(ft), in water depths of 40 to 75 ft. Correlates with the onshore Qbs.
middle Pleistocene
TWTT (ms)
2012
MIS 1 brs
MIS 1 Bay/estuarine deposits
0.6
20
Qmm
MIS 1 be
0
by
Listed are descriptions of all units that crop out on the seafloor and/or are shown on
cross sections; interpreted from sediment-core analysis, sample dating, and
seismic stratigraphic relationships.
Holocene
LITHOLOGY
CL VF M VC
ST F C G
GEOLOGY OF THE NEW JERSEY OFFSHORE IN THE VICINITY OF
BARNEGAT INLET AND LONG BEACH ISLAND
Qbs
26b
4.0
mi
150 o (6.4 km
5 mi
Figure 1. Geology of the New Jersey offshore and contiguous upland areas in the vicinity of Barnegat Inlet and Long Beach Island.
DESCRIPTION OF OFFSHORE UNITS
Qtu
Sangamonian
MIS 5 cbms
Qcu
>MIS 5 cbms
Age of unit
MIS 1 Barrier/shoal sand
0.031
0.062
0.125
0.250
0.5
1.0
2.0
4.0
26
7
late Pleistocene
Quaternary
Table 1. Correlation of onshore surficial units and offshore units.
74o00’00”
74o07’30”
Wisconsinan
21
39o30’00”
-7
0
Area of
detail
2
Holocene
TQg
MIS 1 brs
MIS 3 ecbr
vertical scale (meters)
MIS 1 brs
26
6
-60
26
5
26
4
26
8
~
~
-5
0
113
Holocene
Qmm
0
-8
26
9
0
-3
SP327
Beach and nearshore marine sand
Period
Neogene
-80
27
0
Qbs
123.0
20
N
late Pleistocene and Holocene
37.5
Qal
BEND IN SECTION
B’
MIS 1 be
Qcm2
BEND IN SECTION
-6
0
43
Freshwater wetland deposits
0
Geologic contact, solid where
-8
known, dashed where inferred
Cross section line
-70
18
27
6
-60
19
97
Qmm
Epoch
MIS 3 ecbr
BEND IN SECTION
MIS 1 be
MIS 1 brs
North American
Stages
Qtl
SLIGHT BEND IN SECTION
BEND IN SECTION
-8
0
2
112
99
Qbs
8
Corrected Water Depth
of Core 18 = 61.1 ft (18.6 m)
MIS 6
BEND IN SECTION
54
6
39o30’00”
16
20
3
98
e1
Offshore
Units
MIS 4
Manahawkin Bay
20
-60
Qs
0.031
0.062
0.125
0.250
0.5
1.0
2.0
0
-3
Lin
Core 18
BEND IN SECTION
27
5
20
5
C6
26c
Qs
Manahawkin Bay
20
6
-40
-30
BEND IN SECTION
SE
.9k
NE
Depth (m)
25
21
late Pleistocene and Holocene
sample depth (meters)
20
7
26
8
A
20
-60
1
27
26
9
Onshore
Surficial
Units
m)
Offshore units
Name
Abbrev.
-2
0
EXPLANATION
16
27
0
Correlation
Age of unit
Alluvium
106.6
22
-8
0
-80
22
-30
517
(1
Location and ID of seismic cross-tie
Depth (ft)
Lo
ng
Beach
Haven
530
RES12
RES10
BEND IN SECTION
RES5
RES6
5292
RES8
MIS 3 ecbr
.1
)
Qal
32.5
CORRELATION OF MAP UNITS
533, 276, 522
27
6
>MIS 6 u
ap
0
-6
-30
90.2
Section AA’, from Barnegat Inlet seismic profile (reinterpreted from Wellner and others ,1993) to NJGWS Line 25a. Perspective is from the southwest. Depth scale is two-way travel time (TWTT) of
the seismic signal in miliseconds (ms) converted to meters (m) and feet (ft), based on acoustic velocities of water and the sediments. Seismic reflectors were correlated betweeen all the seismic tie
lines marked on the profiles.
MIS 5 cbms
Onshore surficial units
Name
27.5
130o
rox.
Abbrev.
SF
73.8 ft
MIS 6
MIS 5 channel incising bay facies
Location and ID of seismic cross-tie
app
MIS 3 ecbr
65.6
approx. 6.1 mi (9.8 km)
23a,19
-80
19
-6
0
-50
MIS 1 brs
21
MIS 5 channels incising bay facies
49.2
SF
2.5 m
40
> MIS 6 u
MIS 1 be
Scale: 16 m/inch, vertical; 800 m/inch horizontal; vertical exaggeration (VE) = 50x. The crosssection is scaled uniformly through all the profiles, including the gap in the record between the
Wellner and others (1993) profile and Line 25a.
53
3
2
53
-40
22
0
-7
b
24
Be
ach
Snedden and others, 1994
Peahala Ridge area
-30
-1
-20 0
A’
23a
27
32.8
20
MIS 4
MIS 5 cbms
MIS 5 channels incising bay facies
Section BB’, extending from Wellner and others (1993) offshore profile to NJGWS Line 18.
Perspective is from the southwest. Depth scale is two-way travel time (TWTT) of the seismic
signal in miliseconds (ms) converted to meters (m) and feet (ft), based on acoustic velocities
of water and the sediments. Lines 25a, 27a and 24b are 100-ms records. Line 18 is an 80-ms
record. The zero ms depth is recorded lower on the 80-ms record. Thus, there is a step-down
in the scale for Line 18. Seismic reflectors were correlated betweeen all the seismic tie lines
marked on the profiles.
23
f
18
25g2
Corrected Water Depth of
Core 13 = 51.7 ft (15.8m)
130o
-8
0
C
Marshelder
Islands
43
61
62
60
D
Qbs
42
41
RES3
Core 13
Wellner and others, 1993,
seismic profile and shotpoints
-8
80
10
24b
-80
40
59
-80
A
Ham
Island
26
Brighton Beach
B’
-50
29 30
Outline of
contoured
-80 in
area
figs. 10-12
MIS 3 ecbr
MIS 5 channel
18
48
49
28
522
Beach Haven
Crest
26
-60
Qmm
-6
0
45
44
47
46
39o37’30”
23
b
-50
54
Sand
Island
Little Egg
Harbor
-60
Line
MIS 3 ecbr
MIS 6
> MIS 6 u
-80
16.4
15
30
0.5 mi (0.8 km)
-6
0
High
Island
VE
5
MIS 5 cbms
RES10
C’
50 D’
55
51
52 53
B 56
57
58
39o37’30”
27
a
MIS 1 be
BEND IN SECTION
NW
MIS 4
130o
b
25
Flat
Island
MIS
MIS 1 be
MIS 2
Seafloor
Marine Isotope Stage
Vertical exaggeration
Before present (1950 A.D.)
Miliseconds seismic velocity
Two-way travel time
Wellner and others (1993) shotpoint
0
Scale: 16 m/inch, vertical; 800 m/inch horizontal; VE = 50x
MIS 1 be
MIS 3 ecbr
35
SW
MIS 1 brs
VE = approx. 50x
Egg
Island
C10 of CC’
MIS 1 brs
38.7
A’
15.5 m (50.8 ft)
20
Barnegat Bay
24
11.3 m (37 ft)
MIS 3
barrier sands
MIS 6
)
Little Beach
-70
25
a
> MIS 6 u
7a
km
0
10
MIS 3
barrier sands
> MIS 6 u
LEGEND
SF
164
e2
06
190 o mi (6
.5
MIS 1 brs
ms
Lin
MIS 4
. 4.
0
SE
MIS 5 cbms
BP
NE
MIS 5 cbms
MIS 5
barrier sands
2.0
2.5
7.5 m (24.6 ft)
10
sandy peat layer 14C date
sample depth in core = 2.2 m (7.2 ft)
total depth of sample = 11.6 m (38.1 ft)
radiocarbon age (years BP) = 8810 +/- 170
estuarine/lagoonal muds
sub-bottom depth of core = 2.6 m (8.5 ft)
total depth of core = 12 m (39.4 ft)
(from Wellner, 1990)
SE
3.8 m (12.3 ft)
5
1.5
RES10
-60
17a
Line 25a
ravinement surface
TWTT
NW
15
SF
12m (39.4 ft)
20
22.7
30.7
25g2
Depth (ft)
50 mi
rox
A’
NW
BEND IN SECTION
10
app
1.0
MIS 2
23f
25
c
518, 25, 26f
h
on
ny
Ca
e
or
Ba
14.7
MIS 6
-5
0
ek
Cre
ill
M
26
c
MIS 1 brs
SF
-50
MIS 1 brs
Ship
Bottom
Illinoian
MIS 5 channels
incising bay facies
Line 25a
27
MIS 3 ecbr
Pleistocene
-70
ug
-5
0
-5
0
12
0
6.7
-6
0
13
326
0
SE
53
0
-5
0
26
d
53
3
327
MIS 1 be
24
a
0
-5
B 328
14
-40
C
Thorofare
Island
Oyster
Point
-1
0
-20
-3
0
C1
72
-40
MIS 6
Figure 2. Map of the continental shelf offshore New Jersey, showing the map area, location
of the Baltimore Canyon Trough hinge line of Grow and others (1968) and Owens and
others (1996). The map area is located northwest of the hinge line. ECMA = East Coast
Magnetic Anomaly. The 200-m isobath, shown as a blue line, indicates the approximate
location of the Continental Shelf edge. Figure modified from Carey and others (1998).
52
9
25
C3
Cedar
Bonnet
Islands
Drum
Point
C5
C4
Surf City
Bonnet
Island
23
a MIS 3 ecbr
26
f
Manahawkin
Bay Side
Bay
26
b
-5
0
Lo
ng
k
Cedar C
re
e
Beach Haven West
SW
150
NW
24
-50
Main
Point
Qs
Qs
Tro
75
76
11
Be
Long Beach
upper Holocene sands
23b
23 23b
f
Qtl C2
72
MIS 1 be
Sangamonian
BEND IN SECTION
Carvel
Island
24a
-50
Log Creek
Pond
518
52
8
g
25
nC
ree
k
24
b
h
ki
Qtl
ơ
-4
0
180
an
ah
aw
25
b
West
Carvel
Island
ac
M
ltim
15
Harvey
Sedges
North
Pond
a
26
MIS 1 ecbr
24
MIS 3
ecbr
MIS 1 brs
Wellner and others, 1993, Core 3, C10 above
25b
-3
0
2
53
Qtl
Wellner and others, 1993, seismic profile and cores
5 km
5 mi
100
Depth (ft)
25a
Big
Fla
tC
re
ek
approx. 130o
Depth (m)
C6
r e ek
Harvey
Cedars
0.0
10 20 30 40 50 km
MD
0
11a
0
-5
VE = 50x
0.5
0
517
> MIS 6 u
Core depth below sea level = 9.4 m, 30.8 ft.
5e
125
ebb tidal delta sands
MIS 4
MIS 5 cbms
MIS 1 be
5d
Spencer Canyon
ey
MIS 3 ecbr
C-14: 8810
+/- 170 BP
TWTT in ms
SP326
Sandy
Island
Marshelder
Island
Cedar
C
518
25
lf V
al l
MIS 1 brs
MIS 6
sub-bottom depth (m)
South
Point
Qs
DE
Sh
e
Lindenkohl Canyon
Lin
e7
6
MIS 2
BEND IN SECTION
SP327
h
res
c
26
26
F
B
Qbs
MIS 1 be
25
c
De
law
are
NE
Core 2
ebb tidal
delta sands
lagoonal mud
18
5c
MIS 5
100
ECMA
MIS 1 be
30
98.4
160
12
24
26
26a
River
C reek
Wellner and others,1993
seismic section, shot
points SP328 - 326
0
SP328
-3
5a
5b
24a
Qcm2
G un
n i ng
Loveladies
Whalebone
Point
AMCOR
6011
-50
Beach View
-4
0
Qcu
Table 5 &
fig. 16
26f
0
-4
Cape May
516
75
520
Sloop
Sledge
South Tom's Canyon
59
78.7
MIS 4
26b
517
9
-60
MIS 1 be
3b
39.4
3a
3c
26c
h
Map
Area
26f
-10
-20
53
0
-30
Qtl
50
Barnegat
Gulf Point
Delaware
Bay
MIS 2
MIS 3
-2
00
m
Qbs
Qs
Va
lle
y
eo
f
C8, C9
Conklin
Island
Double
Creek
39o45’00”
Holocene
50
L in
50
Qtl
MIS 1
161
Core 3
barrier sand
Hudson Canyon
Hi n g e
Qal
Atlantic
City
-7
0
Qtl
25g
39o45’00”
TQg
Qcu
Qcm1
Friends
Meeting
Cemetery
10
50
High Bar
Island
RES 2
RES 4
1
RES 6
RES 8
RES 12
516
RES 10
52
9
-80
Qcm1
2
Barnegat
Light
High Bar
52
8
162
SE
0
Sh
elf
163
SF 6
19.6
2
1
25
-70
Qcm2
0
10
C7
3
27
Pebble Beach
C10
27
a
Barnegat
A
Clam Island
10
Qtl
Tg
Tch
-60
7
0
-1
Wisconsinan
-60
50
Qal
Barnegat
Inlet
-60
Tidal Flat
Hu
ds
on
164
Core 7
Late
76
10
523
TQg
Wellner and others, 1993. Seismic profile
and cores 1,2, 3, and 7
Qtl
-2
GEOLOGY OF THE NEW JERSEY OFFSHORE IN THE
VICINITY OF BARNEGAT INLET AND LONG BEACH ISLAND (SHEET 1 OF 2)
GEOLOGIC MAP SERIES GMS 12-3
NW
more ice
-60
Tg
Qbs
Barnegat Beach
Cr
ee
k
-70
el
Tch
-4
0
100
Sedge Islands
10
9
50
L o ch i
Manasquan
Tidal Flat
0
0
less ice
PA
y
all e
on V
ud s
Tg
100
Barnegat Bay
Qcm2
RES 3
RES 5
RES 7
RES 9
TQg
Qal
o
O( /oo)
New Jersey
513
-60
A
G18
H
eoP al
TQg Qcm1
t
Atlan
MIS 3 ecbr
Sedge
Islands
Waretown
Qcm2
50
50
TQg
Qmm
Qs
ow n
Waret
ean
ic Oc
Sandy Hook
10
Creek
-4
0
Tch
-40
50
Depth (m)
Tidal Flat
Mid
75
513
558
-70
Early
522
MIS 1 be
AGE (ka)
C11
Qcm1
Qtu
MIS 1 brs
76
C’
Qcm2
TWTT (ms)
ter
ys
Qtl
NY
74o00’00”
-60
35
-50
74o07’30”
Qs
523
O
Oyster Cre
ek
k
ree
10
Tch
Forked River
Beach
520
C
Qtu
558
0
-3
10
Qcm2
Qs
-40
r
ked Rive
nch For
Bra
Garde
n State
Parkw
ay
h
BEND IN SECTION
Prepared in cooperation with the
U.S. GEOLOGICAL SURVEY
NATIONAL GEOLOGIC MAPPING PROGRAM
DEPARTMENT OF ENVIRONMENTAL PROTECTION
WATER RESOURCES MANAGEMENT
NEW JERSEY GEOLOGICAL AND WATER SURVEY
Prepared in cooperation with the
U.S. GEOLOGICAL SURVEY
NATIONAL GEOLOGIC MAPPING PROGRAM
DEPARTMENT OF ENVIRONMENTAL PROTECTION
WATER RESOURCES MANAGEMENT
VICINITY OF BARNEGAT INLET AND LONG BEACH ISLAND (SHEET 2 OF 2)
35
10
40
15
MIS 6
20
45
3.0
3.3
3.6
3.9
4.2
3
3
2.7
4.5
CL VF M VC
ST F C G
4.8
5.1
5.4
5.7
4
4
6.0
6.2
EXPLANATION
GRAIN SIZE
LITHOLOGY
gravel
CL clay
ST silt
pea gravel
VF very fine sand
coarse sand
F fine sand
medium sand
M medium sand
fine sand/silt
C coarse sand
clay
VC very coarse sand
clay clast
G gravel
shells/
shell fragments
burrows
charcoal or lignite
roots or twigs
Esker, D., Sheridan, R.E., Ashley, G.M., Waldner, J.S., and Hall, D.W., 1996, Synthetic seismograms from vibracores: a
case study in correlating the late Quaternary seismic stratigraphy of the New Jersey Inner Continental Shelf:
Journal of Sedimentary Research, v. 66, no. 6, p. 1156-1168.
Figueiredo, A.G., 1984, Submarine sand ridges: geology and development, New Jersey, USA: unpublished Ph.D. thesis:
University of Miami, 408 p.
Folk, R.L., 1980, Petrology of Sedimentary Rocks: Hemphill Publishing Co., Austin, TX, 185 p.
Grow, J.A., Klitgord, K.D., and Schlee, J.S., 1988, Structure and evolution of the Baltimore Canyon Trough, in R.E. Sheridan and J.A. Grow, eds., The Atlantic continental margin: U.S.: Geological Society of America, The Geology of
North America, v. 1-2, p. 269-290.
median grain size
(mm)
5
5
Grain size samples
with (*) are averaged
from the overlapped
samples of vibracores
Run #1 and #2.
ST F C G
CL VF M VC
end of 17aR1
at 4.93 m
MIS 4
reflector
6
6
phi
mm
-2
-1
0
1
2
3
4
5
4.0
2.0
1.0
0.5
0.250
0.125
0.062
0.031
5.4
5.7
phi
mm
6.0
-2
-1
0
1
2
3
4
5
4.0
2.0
1.0
0.5
0.250
0.125
0.062
0.031
0.9
SEISMIC PROFILE
1
1.2
15
Core 18
20
MIS 4
SF
25
5
30
10
35
15
40
MIS 6
1.5
1.8
2
20
3
2.1
2.4
2.7
3.0
3.3
3.6
3.9
4.2
4.5
4.8
4
5.1
EXPLANATION
GRAIN SIZE
LITHOLOGY
gravel
CL clay
ST silt
pea gravel
VF very fine sand
coarse sand
F fine sand
medium sand
M medium sand
fine sand/silt
C coarse sand
clay
VC very coarse sand
clay clast
G gravel
shells/
shell fragments
burrows
charcoal or lignite
roots or twigs
ST F C G
CL VF M VC
end of 17aR2
at 6.23 m
Figure 6. Core 17a Composite. Driller’s Water Depth (corrected): 19.6 m (64.3 ft). Five-digit numbers in the left-hand column of the Median Grain
Size Table are sample ID-depth numbers. The first two digits are the Core ID number (17a); the last three digits are the sample depth in centimeters (0 - 600R2). R2 indicates samples from Run #2. Lithology colors represent observed colors at time of core processing. Color differences
MIS 4
reflector
5
6.2
AAR age:
OIS 5c-5e
AMS C-14:
48,890 +/3360 BP
depth 6
6.21 m
median grain size
(mm)
0.400
MIS 5
0.300
49.2
SF
55.8
70.5
15.0
SF
17 m
21.5
85.3
100.0
114.8
129.6
Line 25b
15
20
25
30
26.0
35
30.5
40
35.0
45
39.5
50
44.0
144.3
MIS 3
0.200
P
0.100
2.1 miles
18
13 12b
12a 17a
0.000
0.200
0.250
0.300
0.350
D/L Alanine
0.400
0.450
0.500
Depth of sample in Total depth of
Total depth of
AAR
Attributed
core (meters below sample (meters sample (feet below
sample ID
MIS
sea floor)
below sea level)
sea level)
ST F C G
CL VF M VC
SE
NW
12a
3
4.2
-24.8
-81.344
17
3
1.25
-20.85
-68.388
P
5
outcrop
beach outcrop
beach outcrop
13
5
5.83
-21.33
-69.9624
12b
5
1.25
-21.85
-71.668
18
5
5.85
-24.45
-80.196
37.0
11.3
49.2
SF
55.8
70.5
15.0
SF
17 m
21.5
85.3
100.0
114.8
129.6
Line 25b
15
MIS 1be
Core 17a
20
seafloor
MIS 2
25
MIS 4
26.0
MIS 3
MIS 5
30.5
35.0
35
40
MIS 6
45
39.5
> MIS 6
50
clinoform
structures
44.0
144.3
30
Duncan, C.S., Goff, J.A., Austin, J.A., and Fulthorpe, C.S., 2000, Tracking the last sea-level cycle: seafloor morphology
and shallow stratigraphy of the latest Quaternary New Jersey middle continental shelf: Marine Geology, v. 170, p.
395-421.
0.6
EXPLANATION
Valine
Leucine
Aspartic
Phenyl
Glumatic
11.3
Depth (meters)
30
MIS 4
2
2
2.4
0.3
0.500
37.0
Depth (meters)
5
25
SF
2.1
4.48
4.24
1.15
4.30
0.22
0.06
0.19
0.29
0.24
-1.17
-1.09
-0.69
-1.09
-1.16
-0.10
-1.08
1.40
-1.37
0.18
1.63
1.43
Depth (feet)
20
Core 17a
phi
18030
18060
18090
18120
18150
18180
18210
18240
18270
18300
18330
18360
18390
18420
18450
18450
18510
18540
18570
18600
18620
0.0
air pocket
1.8
ID-depth
SEISMIC PROFILE
0
SE
NW
Depth (feet)
1.5
0.600
D/L other aa
1
1
0.031
0.062
0.125
0.250
0.5
1.0
2.0
4.0
1.2
Spisula D/L vs D/L
MEDIAN
GRAIN SIZE
GRAIN SIZE CURVE
5 4 3 2 1 0 -1 -2
LITHOLOGY
CL VF M VC
ST F C G
0.9
Duane, D.B., Field, M.E., Meisburger, E.P., Swift, D.J.P., and Williams, S.J., 1972, Linear shoals on the Atlantic inner
continental shelf, Florida to Long Island, in Swift, D.J.P., and others, eds., Shelf sediment transport: process and
pattern: Stroudsburg, PA, Dowdan, Hutchinson and Ross, p. 447-498.
Hathaway, J.C., Schlee, J.S., Poag, C.W., Valentine, P.C., Weed, E.G.A., Bothner, M.H., Kohout, F.A., Manheim, F.T.,
Schoen, R., Miller, R.E., and Schultz, D.M., 1976, Preliminary Summary of the 1976 Atlantic margin Coring Project
of the U.S. Geological Survey, Open-File Report # 76-844: U.S. Geological Survey, Reston, VA, 217 p.
0.30
0.05
0.60
-0.45
0.10
-0.35
0.72
0.48
-0.10
0.40
0.25
0.60
0.10
0.55
1.05
0.60
0.72
-0.65
0.32
0.75
0.15
0.38
0.30
0.60
0.60
0.75
0.6
Dillon, W.P., and Oldale, R.N., 1978, Late Quaternary sea-level curve: Reinterpretation based on glacio-tectonic influence:
Geology, v. 6, p. 56-60.
phi
17a000
17a030
17a060
17a090
17a120
17a150
17a180
17a210
17a240
17a270
17a300
17a330
17a360
17a390
17a420
17a450
17a480
17a360R2
17a390R2
17a420R2
17a450R2
17a480R2
17a510R2
17a540R2
17a570R2
17a600R2
0.3
Bishop, K.J., 2000, Assessment of offshore sediments in Area C from the New Jersey continental shelf for potential use in
beach replenishment: independent Bachelor of Science research, Rider University, Lawrenceville, NJ, 36 p.
Carey, J.S., Sheridan, R.E., and Ashley, G.M., 1998, Late Quaternary sequence stratigraphy of a slowly subsiding passive
margin, New Jersey continental shelf: American Association of Petroleum Geologists Bulletin, v. 82, no. 5A, p.
773-791.
ID-depth
0.0
Ashley, G.M., Wellner, R.W., Esker, D., and Sheridan, R.E., 1991, Clastic sequences developed during Late Quaternary
glacio-eustatic sea-level fluctuations on a passive continental margin: Example from the inner continental shelf near
Barnegat Inlet, New Jersey: Geological Society of America Bulletin, v. 103, p. 1607-1621.
Butman, B., Noble, M., and Folger, D.W., 1979, Long-term observations of bottom current and bottom sediment movement
on the mid-Atlantic shelf: Journal of Geophysical Research, v. 84, p. 1187-1205.
MEDIAN
GRAIN SIZE
0
0
GRAIN SIZE CURVE
5 4 3 2 1 0 -1 -2
LITHOLOGY
CL VF M VC
ST F C G
Ashley, G.M., and Sheridan, R.E., 1994, Depositional model for valley fills on a passive continental margin, in R.W.
Dalrymple, R. Boyd, and B.A. Zaitlin, eds., Incised-valley systems: origin and sedimentary sequences: SEPM
Special Publication 51, p. 285-301.
0.031
0.062
0.125
0.250
0.5
1.0
2.0
4.0
REFERENCES
2.1 miles
Figure 8. Graph of D/L Alanine vs. D/L other amino acids, showing the correspondence of D/L
ratios for the sample, and showing clustering of samples in two groups, interpreted as MIS 3
and MIS 5 in age. "P" is the North Parramore Island, VA Spisula shell from a MIS 5 outcrop
(Wehmiller, oral communication, 2002). Table shows total depth of samples, establishing that
the most shallow sample, attributed to MIS 3, is from 20.85 m below sea level. Graph courtesy
of John Wehmiller, University of Delaware.
Figure 7. Core 18 Composite. Driller’s Water Depth (corrected): 18.6 m (61.1 ft). Five-digit numbers in the left-hand column of the
Median Grain Size Table are sample ID-depth numbers. The first two digits are the Core ID number (18); the last three digits are the
sample depth in centimeters (0 - 620). Lithology colors represent observed colors at time of core processing. Color differences among
units are accentuated to distinguish lithologies.
Figure 9. Seismic section and interpreted profile, seaward end of line 25b. This section shows the extensive channeling in the MIS 5 sequence, interpreted as a bay-mouth
feature, with the major channel thalweg (heavy gray line) migrating shoreward (to the NW) over time. The migrating channel feature erodes faintly imaged sub-horizontal
bedding in the basal MIS 5 sediments. Note the depositional geometry of the MIS 3 sediments, i.e. horizontal bedding. Core 17a penetrates MIS 3 and MIS 5 sediments
(see Figure 6).
Imbrie, J., Shackleton, N.J., Pisias, N.G., Morley, J.J., Prell, W.L., Martinson, D.G., Hays, J.D., MacIntyre, A., and Mix, A.C.,
1984, The orbital theory of Pleistocene climate; support from a revised chronology of the marine į18O record, in
Berger, ed., Milankovitch and Climatee, Part 1: Reidel, Hingham, MA, p. 269 - 305.
Lacovara, K. J., 1997, Definition and evolution of the Cape May and Fishing Creek formations in the middle Atlantic coastal
plain of southern New Jersey: Ph. D. dissertation, University of Delaware, Newark, Delaware, 245 p.
McBride, R.A., and Moslow, T.F., 1991, Origin, evolution, and distribution of shoreface sand ridges, Atlantic inner shelf,
U.S.A.: Marine Geology, v. 97, p. 57-85.
Miller, K.G., Rufolo, S., Sugarman, P.J., Pekar, S.F., Browning, J.V., and Gwynn, D.W., 1997, Early to Middle Miocene
sequences, systems tracts, and benthic foraminiferal biofacies, New Jersey Coastal Plain, in Proceedings of the
Ocean Drilling Program, Scientific Results, Miller, K.G., and Snyder, S.W. (eds.), vol. 150X, p. 169-186.
Miller, K. G., Sugarman, P.J., Browning, J.V., Horton, B.P., Stanley, A., Kahn, A., Uptegrove, J., and Aucott, M., 2009,
Sea-level rise in New Jersey over the past 5000 years: Implications to anthropogenic changes: Global and
Planetary Change, v. 66, p. 10-18.
Miller, K. G., Sugarman, P.J., Van Fossen, M., Liu, C., Browning, J.V., Queen, D., Aubry, M.P., Burckle, L. D., Goss, M., and
Bukry, D., 1994, Island Beach Site Report: Proceedings of the Ocean Drilling Program, Initial Reports, v. 150X, p.
5-59.
New Jersey Geological Survey, 2007, Surficial Geology of New Jersey: New Jersey Geological Survey Digital Geodata
Series DGS 07-2, scale 1:100,000.
Newell, W.L., Powers, D.S., Owens, J.P., and Schindler, J.S., 1995, Surficial Geological Map of New Jersey; Southern
Sheet: U.S. Geological Survey Open-File Report 95-272, scale 1:100,000: 6 sheets.
320000
Harvey
Cedars
-70
-73
-76
-79
-82
-85
-88
-91
-94
-97
-100
-103
-106
-109
-112
-115
-118
-121
-124
-127
-130
310000
300000
290000
edge of
MIS 5 bay
280000
270000
Newell, W. L., Powars, D. S., Owens, J. P., Stanford, S. D., Stone, B. D., 2000, Surficial geologic map of central and
southern New Jersey: U. S. Geological Survey Miscellaneous Investigations Series Map I-2540-D, scale 1:100,000.
O’Neal, M. L., and McGeary, S., 2002, Late Quaternary stratigraphy and sea-level history of the northern Delaware Bay
margin, southern New Jersey, USA: a ground-penetrating radar analysis of composite Quaternary coastal terraces:
Quaternary Science Reviews, v. 21, p. 929-946.
260000
O'Neal, M. L., Wehmiller, J. F., and Newell, W. L., 2000, Amino acid geochronology of Quaternary coastal terraces on the
northern margin of Delaware Bay, southern New Jersey, U. S. A., in Goodfriend, G. A., Collins, M. J., Fogel, M. L.,
Macko, S. A., and Wehmiller, J. F., eds., Perspectives in amino acid and protein geochemistry: Oxford University
Press, p. 301-319.
250000
Owens, J.P., Sugarman, P.J., Sohl, N.F., Parker, R.A., Houghton, H.F., Volkert, R.A., Drake, A.A., Jr., and Orndorff, R.C.,
1998, Bedrock Geologic map of central and southern New Jersey: U.S. Geological Survey, Miscellaneous Investigations Series Map I-2540-B, scale 1:100,000, 4 sheets.
10A.
Psuty, N. P., 1986, Holocene sea level in New Jersey: Physical Geography, v. 36, p. 156-167.
Salisbury, R. D., and Knapp, G. N., 1917, The Quaternary formations of southern New Jersey: N. J. Geological Survey
Final Report, v. 8, 218 p.
320000
Harvey
Cedars
depth thickness
in feet in feet
54
320000
310000
Harvey
Cedars
-54
-56
-58
-60
-62
-64
-66
-68
-70
-72
-74
-76
-78
-80
-82
-84
-86
-88
-90
-92
-94
-96
310000
50
46
?
300000
42
300000
38
34
290000
290000
30
edge of
MIS 5 bay
26
280000
280000
22
18
270000
14
270000
10
6
260000
260000
2
edge of
MIS 5 bay
edge of
MIS 5 bay
250000
Harvey
Cedars
depth thickness
in feet in feet
?
trace of
MIS 3
barrier/
shoreface
320000
320000
Harvey
Cedars
?
33
310000
30
310000
300000
27
-38
27
-41
25
24
290000
MIS 3
inlet
perimeter of
shore-detached
27a
shoal sand
resource,
based on 10-ft
thickness contour
17
15
280000
-56
280000
12
270000
-65
7
-68
5
270000
9
260000
6
260000
3
1
-74
250000
250000
115
5.0
18.95
5.78
organic sediments,
1200
35
1133
124
5.0
6.95
2.12
4532
58
5209
233
14.0
12.7
3.87
5625
200
6415
468
14.0
46.1
14.05
39o 30' 36.51" N
74o19' 11.35" W
3
39o 48' 10" N
74o 05' 37" W
4
(Miller and others, 1994)
C11 - Island Beach
39o 48' 10" N
74o 05' 37" W
lignite
5
Great Bay
39o 33' 58.11" N
74o 21' 20.23" W
peat
500
70
494
140
9.8
6
(Psuty, 1986)
Great Bay
39o 33' 19.44" N
74o 20' 36.66" W
peat
3050
95
3210
190
9.8
24.6
7.5
7
(Psuty, 1986)
Great Bay
39o 32' 08.42" N
74o 19' 50.04" W
peat
4175
145
4760
290
9.8
27.7
8.44
8
(Psuty, 1986)
Great Bay
39o 32' 09.07" N
74o 19' 50.38" W
peat
4495
125
5204
250
9.8
27.1
8.26
9
(Psuty, 1986)
NJGS Core 127
39o 24' 59.36" N
74o 15' 19.94" W
peat
7130
100
7960
440
-51.5
52.71
16.07
10
NJGS Core 127
39o 24' 59.36" N
74o 15' 19.94" W
peat
7690
50
8486
200
-51.5
51.9
15.82
11
C10 - Barnegat Inlet Core 3
39o 45' 58.68" N
74o 05' 58.2" W
peat
8810
170
9890
+360/-400
-30.8
38
11.6
12
C7 - Ship Bottom #1
39o 43' 52.2" N
74o 14' 21.0" W
peaty clay silt
34,890
960
NA
NA
20
8
2.44
13
(Newell and others, 1995)
C7 - Ship Bottom #1
39o 43' 52.2" N
74o 14' 21.0" W
peaty clay silt (?)
>39,000
NA
NA
NA
20
38
11.59
14
(Newell and others, 1995)
Great Bay #2
39o 30' 36.51" N
74o 19' 11.35" W
organic sediments,
40,100
NA
NA
NA
5
46.5
14.2
primarily peats
250000
250000
0
1
2
3
4
0
1
statue miles
240000
600000
610000
620000
2
3
4
statue miles
630000
600000
10B.
610000
620000
0
240000
1
600000
11A.
Figure 10A. Depth of the MIS 6 reflector. 10B. Thickness of the overlying MIS 5 sediments. The landward and seaward edges of the MIS 5
bay feature, as interpreted from the prominent clinoforms and channel thalwegs seen in the seismic data, are indicated by heavy dashed lines.
Surfaces are contoured from approximately 2500 data points from the seismic lines shown and labeled on the figure. The contouring is limited
to the portion of the map area covered by this seismic grid. Map scale is in New Jersey state plane coordinates. Harvey Cedars is located
approximately 3 miles south of Barnegat Inlet on Long Beach Island. Vibracore locations are shown as pink triangles and labeled in bold text.
The location and extent of the contoured area is indicated on Figure 1.
3
4
0
1
statue miles
240000
630000
2
610000
620000
2
3
statue miles
630000
600000
11B.
610000
620000
0
4
4
240000
1
3
4
0
statue miles
240000
12A.
630000
2
600000
610000
1
2
3
4
statue miles
620000
630000
600000
12B.
610000
620000
primarily peats
630000
Scott, T.W., Swift, D.J.P., Whittecar, G.R., and Brook, G.A., 2010, Glacioisostatic influences on Virginia’s late Pleistocene
coastal plain deposits: Geomorphology, v. 116, p. 175-188.
39o37’30”
25
b
23
b
d
A
Be
ng
EXPLANATION
26c Seismic line
MIS 5 channel
0
18
Clinoforms on
seismic profiles
19
Inferred MIS 5 channel
0
70o07’30”
1
1
2
2
3 miles
3 kilometers
74o00’00”
Figure 13. MIS 5 channel features, as demarcated by the rose-shaded blocks on the seismic
profiles. The depth of the MIS 6 surface and thickness of the MIS 5 sediments also demarcate the
channel features (see Figure 10). Channel thalwegs indicate the dendritic paleochannel extent,
depth and southward direction of drainage (blue lines, dashed where inferred). The interpreted
edges of the MIS 5 bay are indicated with a bold dashed black line. The relatively steeply dipping
en echelon reflectors seen on Sections AA’ and BB’ and in Figure 9 also indicate the shoreward
migration of the channels.
charcoal, C-14:
31,600 + 9760 /
- 4280 BP
SAND; fine, slightly clayey; some
large shell fragments; several clay
layers and clay clasts; some large
rock fragments
depth 6
6.0 m
ST F C G
CL VF M VC
0
1
2
25
MIS 4
10
30
15
35
20
MIS 6
40
Core 11a location on seismic line 25g:
Lat: 39o 42.4036'
Lon: 74o 02.6232'
Water Depth (corrected): 15.1 m (49.4')
SAND; fine to very fine; some shell
fragments; small amount of rock fragments
SAND; fine to very fine; small amount
shell fragments; small amount rock
fragments; bands of clayey sand at
3.75m, 4.3m, some heavy minerals
depth
5.85 m
6
2
SAND; medium; subangular; distinct
zones of large shell fragments; 3%
opaques; 2% rock frags
3
MIS 2 reflector
SAND; slightly clayey; medium to fine
sand; subangular; small shell fragments throughout; 3 % opaques
SAND; clayey, very fine; small amount
of shell fragments; clay clast at 4.74.75m
4
EXPLANATION
GRAIN SIZE
LITHOLOGY
gravel
CL clay
ST silt
pea gravel
VF very fine sand
coarse sand
F fine sand
medium sand
M medium sand
fine sand/silt
C coarse sand
clay
VC very coarse sand
clay clast
G gravel
shells/
shell fragments
burrows
charcoal or lignite
roots or twigs
5
Age-depth plot of Holocene-age referenced radiocarbon-dated samples
3 miles
Radiocarbon age in thousands of years BP
0
70o07’30”
1
2
3 kilometers
10
9
8
7
6
5
4
MIS 3
3
2
1
2
74o00’00”
1.20
SAND; very coarse to fine, poorly
sorted, fining upwards; slightly clayey
sand near top; some shell hash
ST F C G
CL VF M VC
CLAY; slightly micaceous; v. small
amount of shell fragments; silt lens/
burrow at 5.20-5.26m, clay below which
contains numerous multidimentional
small sized, silt-filled burrows
5
depth
5.69 m
6
ST F C G
CL VF M VC
Figure 14D. MIS 3 sediments in Core 11a (3.85 - 5.6 meters depth) located shoreward of the barrier
complex, contain interbedded mud, silt, clay and sand, typical of a lagoon/small channel environment.
Barrier complexes on seismic profiles 23b, 25b, 26f, and 75 are documented in Uptegrove (2003) and
are on file at NJGWS. Seismic profile two-way travel time scale is miliseconds (ms).
Figure 14 A. Evidence of MIS 3 barrier/shoreface complex, as found on seismic profiles and in
vibracores. The heavy blue line traces the distribution of the barrier sands, indicating the possible
orientation of the MIS 3 shoreline. Seismic sections blocked in light blue have seaward-dipping
reflectors, suggestive of a barrier/shoreface complex. Two of the barrier sand complexes are
evident on Section AA’ (seismic profiles 76 and 25a).
0
0
MIS 5
and
older
0
5
25
10
4.53
3.1
1
6
7
75
20
4.50 4.18
30
11
4
6.1
3.05
40
9.2
12.2
100
7.69
9
7.13
5
10
G
S
S
150
15.2
S
S
20
S
S
200
GS
60
sand
G
15
S
175
50
G
125
5.63
10
1
50
2.89
8
HOLE 6011
silty clay
0
0.50
3
Wright, J.D., Sheridan, R.E., Miller, K.G., Uptegrove, J., Cramer, B.S., and Browning, J.V., 2009, Late Pleistocene Sea
level on the New Jersey Margin: Implications to eustasy and deep-sea temperature, Global and Planetary Change,
v. 66, p. 93-99.
18.3
225
Legend
7 Sample number keyed to Table 4
4.18 Radiocarbon age in thousands of years before present (BP)
Calibrated age error +/- 2 standard deviations
MIS 2
SAND; medium with coarse in top 20
cm; subangular; coarsening upwards;
distinct zones of shell fragments
1
20
Distribution of barrier
sands and possible
orientation of MIS 3
shoreline
Inferred orientation
of the MIS 3 shoreline
Wellner, R.W., Ashley, G.M., and Sheridan, R.E., 1993, Seismic stratigraphic evidence for a submerged middle Wisconsin
barrier: Implications for sea-level history: Geology, v. 21, p. 109-112.
The views and conclusions contained in this document are those of the authors and should not be interpreted as necessarily
representing the official policies, either expressed or implied, of the U. S. Government.
5
MIS 2 reflector
Figure 14C. Composite core figure for Core 11 linking the lithology of the 20-foot-deep vibracore to a
high-resolution seismic profile to delineate offshore surficial geology and potential beach replenishment
sand resource areas.
8.81
Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping Program, under USGS award
number G09AC00185.
20
3
4
EXPLANATION
GRAIN SIZE
LITHOLOGY
gravel
CL clay
ST silt
pea gravel
VF very fine sand
coarse sand
F fine sand
medium sand
M medium sand
fine sand/silt
C coarse sand
clay
VC very coarse sand
clay clast
G gravel
shells/
shell fragments
burrows
charcoal or lignite
roots or twigs
SF
SAND; medium to very coarse sand
Figure 15. Age-depth plot of Holocene-age referenced radiocarbon-dated samples. Samples 1, 2, 4,5, 6, 7, 8, were collected from the Qmm or MIS
1 be units, i.e., bay or estuarine silts, muds and/or peats. Sample 3 is from a lignite layer in sands, interpreted as a nearshore environment (Miller and
others, 1994). Sample 11 was collected from a peat layer in a vibracore drilled in Barnegat Inlet (Wellner and others, 1993). Samples 9 and 10 were
collected from offshore Core 127, also from the MIS 1 be unit. The samples collected from bay/estuarine silts, muds and/or peats show a trend. The
samples from nearshore sands or from an inlet do not follow the trend, due to the high-energy depositional environment of the inlets and nearshore
sands, which result in highly variable accomondation space and sedimentation rates. Sample numbers are keyed to Table 4.
250
Alternating Sands, Silty Clays and Clays
Edge of MIS 5 bay
SAND; medium; increase in shell hash
with depth
16
Seismic section
20
45
Core 11 location on seismic line 26a:
Lat: 39o 41.2403'
Lon: 74o 02.6232'
SAND; coarse to medium, well sorted;
slightly fining upward; small amount
gravel but none below 5.25; clay clast
at 3.5m; thin lens of organic material
at 4.04m; Some clay with sand at
5.98m
5
MIS 6
Pleistocene
16
25
Figure 14B. MIS 3 sediments in Core 15 (3.0 - 6.0 meters depth) located seaward of the MIS 3 barrier
complex, contain sand, typical of a shoreface setting.
21
Vibracore
18
Channel thalweg
on seismic profile
26c Seismic line
13
23
f
SAND; coarse, well sorted; few gravel; shell fragments; some whole
shells throughout
40
2
Pliocene
21
Vibracore
23
a
22
19
EXPLANATION
18
Lo
Be
Lo
ng
22
13
ic
tlant
ac
ac
23
a
23
f
an
Oce
SAND; very coarse with abundant
gravel and rock fragments; subrounded;some shell fragments
20
SAND; coarse to medium, coarsening
upward; some shell hash and shells
Miocene
18
hI
sla
n
d
hI
sla
n
Atl
39o37’30”
23
b
ean
Oc
antic
3
4
25
a
35
15
CLAY; small amount of quartz sand
MIS 2 reflector
EXPLANATION
GRAIN SIZE
LITHOLOGY
gravel
CL clay
ST silt
pea gravel
VF very fine sand
coarse sand
F fine sand
medium sand
M medium sand
fine sand/silt
C coarse sand
clay
VC very coarse sand
clay clast
G gravel
shells/
shell fragments
burrows
charcoal or lignite
roots or twigs
10
30
Core 11a
SAND; very coarse with pebbles and
granules; Some shell hash throughout
Eocene
39o37’30”
Core 15 Location on seismic line 26c:
Lat: 39o 41.8194'
Lon: 74o 03.9906'
MIS 4
1
meters
Fig. 9
35
17a
27
a
27
a
25
b
26
d
26
d
39o37’30”
MIS 6
2
MIS 2
Depth (meters)
Wellner, R.W., 1990, High-resolution seismic stratigraphy and depositional history of Barnegat Inlet, New Jersey and
vicinity, unpublished Masters of Science Thesis, Rutgers University, New Brunswick, NJ, 109 p.
25
a
13
12
30
SAND; coarse to very coarse with
gravel up to 7cm in diameter; small
clay layer at 2.04-2.05m; moderate
amounts of shell material
5
Depth (feet)
Wehmiller, J.F., and Miller, G.H., 2000, Aminostratigraphic dating methods in Quaternary geology, in J.S. Noller, J.M.
Sowers, and W.R. Lettis, eds., Quaternary Geochronology: Methods and Applications, AGU Reference Shelf 4, p.
187-222.
Ship Bottom
25
c
b
24
Wehmiller, J. F., 1997, Data report: aminostratigraphic analysis of mollusk specimens: Cape May Coast Guard station
borehole, in Miller, K. G., and Snyder, S. W., eds., Proceedings of the Ocean Drilling Program: Scientific Results, v.
150x, p. 355-357.
12
f
26
17a
b
24
Waldner, J.S., and Hall, D. W., 1991, A marine seismic survey to delineate Tertiary and Quaternary stratigraphy of Coastal
Plain sediments offshore of Atlantic City, New Jersey: New Jersey Geological Survey, Geological Survey Report
GSR 26, 15 p.
13
26a
26
c
Ship Bottom
25
c
25
20
14
26
c
f
26
Swift, D.J.P., Young, R.A., Clarke, T.L., Vincent, C.E., Niederoda, A., and Lesht, B., 1981, Sediment transport in the middle
bight of North America; synopsis of recent observations: International Association of Sedimentologists Special
Publications, v. 5, p. 361-383.
Uptegrove, J., Waldner, J.S., Hall, D.W., and Monteverde, D. H., 2012, Sand Resources offshore Barnegat Inlet and
northern Long Beach Island, New Jersey: New Jersey Geological and Water Survey, in publication.
26
b
26
b
14
MIS 4
15
11
25
g
26a
5
10
11
Steckler, M.S., Reynolds, D.J., Coakley, B.J., Swift, B.A., and Jarrard, R., 1993, Modeling passive margin sequence
stratigraphy, in Posamentier, H.W., Summerhayes, C.P., Haq, B.U., and Allen, G.P., eds., Sequence stratigraphy
and facies associations: International Association of Sedimentologists Special Publication 18, p. 19-41.
Uptegrove, J., Hall, D.W., Waldner, J.S., Sheridan, R.E., Lubchansky, B.J., and Ashley, G.M., 1999, Geologic framework of
the New Jersey inner shelf: results from resource-based seismic and vibracore studies, in New Jersey Beaches and
Coastal Processes from Geologic and Environmental Perspectives, Puffer, J., ed., Geological Association of New
Jersey, Proceedings, v. 16, p. 45-64.
15
25
g
MIS 2
1
25
SAND; fine to medium sand; subangular to rounded; Fining upwards;
scattered broken shells; 5 % opaques;
3 % rock fragments
15
SAND; medium to very coarse, fining
upward; shell hash throughout; Faint
cross bedding from 0.47-0.6m
15
Snedden, J.W., Tillman, R.W., Kreisa, R.D., Schweller, W.J., Culver, S.J., and Winn, R.D., Jr., 1994, Stratigraphy and
genesis of a modern shoreface-attached sand ridge, Peahala Ridge, New Jersey: Journal of Sedimentary Research,
v. B64, no. 4, p. 560-581.
Uptegrove, J., 2003, Late Pleistocene facies distribution, sea level changes, and paleogeography of the Inner Continental
Shelf off Long Beach Island, New Jersey: unpublished Masters of Science Thesis, Rutgers University, New Brunswick, NJ, 238 p.
11a
11a
Smith, P.C., 1996, Near-shore ridges and underlying upper Pleistocene sediments on the inner continental shelf of New
Jersey: Masters Thesis, Rutgers University, 157 p.
Sugarman, P.J., Miller, K.G., Browning, J.V., Monteverde, D.H., Uptegrove, J., McLaughlin, P.P., Jr., Stanley, A.M., Wehmiller, J., Kulpecz, A., Harris, A., Pusz, A., Kahn, A., Friedman, A., Feigenson, M.D., Barron, J., and McCarthy, F.M.G.,
2007, Cape May Zoo site, in Miller, K.G., Sugarman, P.J., Browning, J.V., et al., Proc. ODP, Init. Repts., 174AX
(Suppl.): College Station, TX (Ocean Drilling Program), 1-66. doi: 10.2973/odp.proc.ir.174AXS.108.2007
Harvey Cedars
20
20
SF
0
SEISMIC PROFILE
SAND; coarse to very coarse, shell
hash up to 3cm in diam.
SF
LITHOLOGY
CL VF M VC
ST F C G
0
Core 11
15
Sheridan, R.E., Ashley, G.M., Miller, K.G., Wright, J.D., Uptegrove, J., Wehmiller, J, and York, L., 2001, Late Pleistocene
sea levels based on sequences from the New Jersey continental shelf, in Abstracts with Programs, Geological
Society of America Annual Meeting, Boston, MA, p. A-99.
CLAY; lenses of coarse sand and
gravel 1-5cm thick; sand and gravel
grains are subrounded; no shell hash
SEISMIC PROFILE
39o45’00”
39o45’00”
Harvey Cedars
15
0
Barnegat
Inlet
Core 15
Sheridan, R.E., Ashley, G.M., Uptegrove, J., Waldner, J.S., and Hall, D.W., 2002, Late Pleistocene sequences on the New
Jersey continental shelf indicate significant Stage 3 ice sheet dynamics: Geological Society of America, Annual
Meeting, Denver, CO, p. 476.
LITHOLOGY
CL VF M VC
ST F C G
SEISMIC PROFILE
39o45’00”
39o45’00”
75
76
75
Barnegat
Bay
Barnegat
Inlet
LITHOLOGY
CL VF M VC
ST F C G
Barnegat
Bay
74o00’00”
Sheridan, R.E., Ashley, G.M., Miller, K.G., Waldner, J.S., Hall, D.W., and Uptegrove, J., 2000, Onshore-offshore correlation
of upper Pleistocene strata, New Jersey coastal plain to continental shelf and slope: Sedimentary Geology, v. 134, p.
197-207.
70o07’30”
Island Beach
State Park
74o00’00”
76
70o07’30”
Island Beach
State Park
Selner, G.I., and Taylor, R.B., 1993, System 9, GSMAP, and other programs for the IBM PC and compatible microcomputers, to assist workers in the earth sciences: U.S.G.S. Open-File Report 93-511, Denver, CO, 363 p.
2.8
Table 4. Radiocarbon age and errors for samples collected within or proximal to the map area. Specifically, the Island Beach samples are from the Island Beach corehole (Miller and
others,1994), the same record from which the gamma log is shown at C11 on CC’. The Great Bay samples were collected approximately 10 miles southwest of the map area, on the
upland side of Barnegat Bay. NJGWS Core 127 was drilled offshore approximately 15 miles south of the map area and the sampled unit is traceable on seismic profiles as the MIS 1
be unit. Samples 12 and 13 are from the onshore core of Newell and others, point C7 on correlation CC’. These dates support the gamma log correlation of the base of the Holoceneage sediments. For a more complete discussion of the age of Barnegat Bay sediments and regional sea level rise rates, see Psuty (1986) and Miller and others (2009). SD - standard
deviation. MSL - mean sea level.
240000
Figure 12A. Depth of the MIS 2 reflector. 12B. Thickness of the overlying MIS 1 sediments. Surfaces are contoured from approximately 2500
data points from the seismic lines shown and labeled on the figure. The contouring is limited to the portion of the map area covered by this
seismic grid. Map scale is in New Jersey state plane coordinates. Vibracore locations are shown as pink triangles and labeled in bold text. MIS
3 sediments are the outcropping unit seaward (to the SE) of the MIS 1 sediments (see Figure 1). Harvey Cedars is located approximately 3
miles south of Barnegat Inlet on Long Beach Island. The location and extent of the contoured area is indicated on Figure 1.
Figure 11A. Depth of the MIS 4 reflector. 11B. Thickness of the overlying MIS 3 sediments. Surfaces are contoured from approximately 2500
data points from the seismic lines shown and labeled on the figure. The contouring is limited to the portion of the map area covered by this
seismic grid. Note trace of MIS 3 barrier/shoreface (heavy violet line) and interpreted MIS 3 inlet offshore present-day Harvey Cedars (dashed
yellow line). Harvey Cedars is located approximately 3 miles south of Barnegat Inlet on Long Beach Island. Map scale is in New Jersey state
plane coordinates. Vibracore locations are shown as pink triangles and labeled in bold text. The location and extent of the contoured area is
indicated on Figure 1.
9.19
(Wellner and others, 1993)
260000
3
-71
3041
organic sediments,
Sample
depth (m)
primarily peats
lignite
280000
9
270000
30
74o 19' 11.35" W
Sample
depth (ft)
C11 - Island Beach
11
-62
2890
30o 30' 36.51" N
Calibrated
age error
+/- 2 SD
Great Bay #2
290000
13
-59
15
Calibrated
age
Material
2
300000
-53
18
14C
age error
+/-1 SD
Longitude
Great Bay #1
310000
19
-50
290000
Surface elevation
of boring site (ft)
relative to MSL
age
14C
Latitude
1
21
-47
Site
23
-44
300000
Number
320000
Harvey
Cedars
depth thickness
in feet in feet
?
21
Barnegat Inlet
ebb-tidal delta
sand
nearshore
shoal
Lithology. The section consists of 260 meters
of alternating shelly sands, silty clays, clays
and some gravel of Eocene and Miocene
through Pleistocene age. Glauconite is
common in the lower part of the section.
Palentology. Planktic foraminifers and calcareous nannofossils are very sparse in the upper
part of this core, although they occur in greater
numbers in the Miocene and Eocene
sediments found lower in the section. Zones
rich in diatoms are found in the Miocene and
younger strata. A shallow shelf environment of
deposition is inferred.
Interstitial water. This drill site penetrated
approximately 125 meters of relatively fresh
water, the greatest thickness encountered in
this drilling program. Salinity decreased from
29 0/00 in the firest core collected to 1.5 0/00
at 71 meters.
Drilling date: August 17-18, 1976
Latitude :
39o 43.5’ N
Longitude: 73o 58.6’ W
GS
25
GS
GS
GS
28
GS
G
S
Numbered core interval,
recovery arbitrarily shown
at upper end of interval
Glauconite
Shells
Figure 16. Interpretation of top intervals of the AMCOR 6011 borehole,
correlated to NJGWS seismic line 517 and known MIS 3 and MIS 5 lithologies, on stratigraphic section of AMCOR 6011, from Hathaway and others,
1976, p. 104. Location of AMCOR 6011 is shown in Figure 1.
Penetration
String depth in feet
Number of
Core relative to Kelly Bushing
Interval
Cumulative
sections
interval
feet
top
bottom
feet
meters
Recovery
Lithology - Age
(core catcher sample)
feet
meters
%
Salinity
parts per mil
1
105
135
30
30
9.1
1
4.5
1.4
15
Olive gray silty clay
28.9
2
135
165
30
60
18.3
1
1.5
0.5
5
Medium to coarse sand, fair
amount heavy minerals
NA
Table 5. Excerpt from Core Table for AMCOR 6011, in Hathaway and others, 1976, p. 107. Water depth is 73 ft (22.3 m). String depth
is water depth plus the height of the Kelly Bushing (on the drilling vessel) above the sea surface. Correlated with NJGWS seismic line
517, we interpret the sediment in Core Interval #1 as MIS 3 and the sediment in Core Interval #2 as MIS 5 and older. Location of AMCOR
6011 is shown in figure 1.
VICINITY OF BARNEGAT INLET AND LONG BEACH ISLAND
by
Jane Uptegrove1, Jeffrey S. Waldner1, Scott D. Stanford1,
Donald H. Monteverde1, Robert E. Sheridan2, and David W. Hall1
1
Rutgers University, Department of Earth and Planetary Sciences
2
Booklet accompanies the map,
Geology of the New Jersey offshore
in the vicinity of Barnegat Inlet and Long Beach Island
1:80,000
(2 Plates, part of GMS 12-3)
Prepared with support from the
U.S. Geological Survey
National Cooperative Geologic Mapping Program,
Award # G09AC00185
STATE OF NEW JERSEY
Chris Christie, Governor
Kim Guadagno, Lt. Governor
Department of Environmental Protection
Bob Martin, Commissioner
Water Resources Management
Michele Siekerka, Assistant Commissioner
Geological and Water Survey
Karl Muessig, State Geologist
NEW JERSEY DEPARTMENT OF ENVIRONMENTAL PROTECTION
The mission of the New Jersey Department of Environmental Protection is to assist the residents of New Jersey in preserving,
sustaining, protecting and enhancing the environment to ensure the integration of high environmental quality, public health and
economic vitality.
The mission of the New Jersey Geological and Water Survey is to map, research, interpret and provide scientific information
regarding the state’s geology and ground-water resources. This information supports the regulatory and planning functions of DEP
and other governmental agencies and provides the business community and public with information necessary to address
environmental concerns and make economic decisions.
For more information, contact:
New Jersey Department of Environmental Protection
P.O. Box 420, Mail Code 29-01
Trenton, NJ 08625-0420
(609) 292-1185
http://www.njgeology.org/
Cover photo: Heading out of Barnegat Inlet to collect seismic profile data in the Atlantic Ocean. The marine seismic Geopulse TM
boomer with flotation pontoons is stowed on the work deck of the vessel en route to the survey area (foreground); Barnegat
Lighthouse is visible in the background. Photograph by Jane Uptegrove, 2000.
Regional Geologic Setting
Modern depositional setting
INTRODUCTION
The New Jersey Geological and Water Survey
(NJGWS) started mapping the State’s offshore geology
in the late 1990s by acquiring, analyzing, and
interpreting marine geologic and geophysical data.
Original
exploration
efforts
identified
and
characterized near-shore sand resources in both State
and Federal waters (within and beyond the 3-mile
State/Federal jurisdictional boundary). Exploration in
the map area (fig. 1) was part of this original effort.
NJGWS compiled the sand resource information in a
Sand Resources Map of the area (Uptegrove and
others, 2012). Uptegrove (2003) interpreted the seismic
and vibracore data, identifying and dating several
sequences and unconformities (in ascending
stratigraphic order) from Marine Isotope Stage (MIS) 6
through MIS 1 (recent). That interpretation is the basis
of this map. In addition, the map includes correlation
of offshore data with onshore borings and mapping,
and with several previous near-shore studies. It is the
aim of the authors that the map will serve as a broadly
available compilation and synthesis.
The modern depositional setting of this
offshore area, located in the mid-Atlantic bight (fig. 2),
is a storm-dominated continental shelf about 100-150
km wide having an average seaward deepening
bathymetric gradient of 0.001 (Swift and others, 1981;
Ashley and others, 1991). Inner shelf topography is
characterized by low relief (~ 3 to 12-m) northeastsouthwest-trending sand ridges formed during the
Pleistocene/Holocene transgression (Duane and others,
1972; Ashley and others, 1991). Shore-perpendicular
shelf valleys extend across the entire shelf. However,
there is no large inland drainage within the map area.
The New Jersey coastline is a mixed-energy
micro-tidal coastline with a tidal range of ~1 m, a mean
wave height of 0.82 m, and average wave period of 8
seconds (Ashley and others, 1991). Net longshore drift
is to the south of Barnegat Inlet, and residual current
flow on the shelf is to the south and southeast (Butman
and others, 1979).
Regional tectonic and glacial controls on sedimentation
ACKNOWLEDGEMENTS
This area is close to the Baltimore Canyon
Trough tectonic hinge line (Grow and others, 1988;
Owens and others, 1998), that is, the linear expression
of the inflection point between the upland arch and the
offshore basin of the Baltimore Canyon Trough (fig.
2). It is oriented sub-parallel to shore along the
southern New Jersey coast, curves in a northeasterly
direction north of Barnegat Inlet, and is oriented in an
easterly direction south of Long Island, N.Y. As such,
subsidence related to the collapse of the outer limit of
crustal forebulge since the Last Glacial Maximum
(LGM), approximately 25 thousand calendar years ago,
runs sub-parallel to the basin/arch depositional control
of the Baltimore Canyon Trough hinge line (Dillon and
Oldale, 1978) northeast of the map area, and is almost
perpendicular to it southwest of the map area. Along
the coast, this tectonic and glacio-isostatic control on
sedimentation is reflected in the contrasting
depositional settings of eroding headlands of the
northern New Jersey coast and the barrier-islands of
the central and southern New Jersey coast (fig. 2).
Laurie Whitesell, Benjamin Lubchansky
(Rider University), Kimberly Bishop (Rider
University) and Stephanie Gaswirth (Rutgers
University) participated in vibracore analyses.
Kimberly Bishop prepared digitized lithologic logs and
performed grain-size calculations on most of these
cores as part of an independent study, December, 2000.
Zehdreh Allen-Lafayette, NJGWS cartographer,
prepared the GIS base maps and data coverages, and
performed the map cartography and final layout of the
map sheets. John F. Wehmiller performed amino-acid
racemization analyses on NJGWS core samples,
extending our ability to date map units beyond the
limits of radiocarbon dating.
The New Jersey Department of Environmental
Protection Coastal Engineering Program and the
Bureau of Ocean Energy Management (formerly the
Minerals Management Service) of the U.S. Department
of Interior, Agreement No. 14-35-0001-30751 funded
acquisition of the data. Analysis and production was
supported by the U. S. Geological Survey, National
Cooperative Geologic Mapping Program, under USGS
award number G09AC00185.
Marine seismic data show the offshore
expression of this contrast in depositional settings.
Subbottom profiles collected offshore northern New
Jersey reveal Tertiary sediments either at the sediment
1
surface or covered by a thin veneer (up to 3 m) of late
Pleistocene or Holocene sediments. Coast-parallel
seismic profiles extending from Manasquan south to
Barnegat Inlet, a distance of about 40 kilometers (25
miles),
reveal a transition from little or no
Pleistocene/Holocene cover in the north through a
gradually thickening sediment wedge to the south
(Uptegrove and others, 1999). In the map area
(Barnegat Inlet and south), Pleistocene or Pleistoceneplus-Holocene sediments are ubiquitous in outcrop at
the sediment surface, overlying the Tertiary sediments
with a total thickness of ~8 to 20 m. Pleistocene units
thicken slightly towards the southeast (seaward).
Holocene sediments are not preserved in the study area
at water depths exceeding about 20 m (66 ft.) below
mean sea level (fig. 1). However, Holocene-age
sediments are preserved at locations on the mid-shelf
(Duncan and others, 2000).
during sea-level rise and sea-level highstands (Carey
and others, 1998). As a result, only submarine sand
shoal features and estuarine interbedded sand and mud,
deposited after the LGM (MIS 2) are intact in the nearshore. Likewise, it is probable that even some of the
post-LGM shoals have not persisted, eroded during
sea-level rise or scoured by present-day submarine
currents.
Stratigraphy
The offshore area of the map is located on a
passive margin, where high-magnitude sea level
change is a much more significant control on sediment
deposition/erosion than tectonic subsidence or
sediment influx. Erosion surfaces created during sealevel lowstands are evident on the seismic profiles as
prominent, laterally continuous reflectors. The most
recent of these in the map area is the MIS 2 lowstand
reflector, which separates Pleistocene and Holocene
sediments, and which formed when Pleistocene
sediments were exposed on the shelf during the LGM.
Holocene transgressive systems tracts are preserved in
the near-shore, either as estuarine interbedded sand and
mud (the MIS 1 be unit), or shoreface deposits and/or
submarine ridges (the MIS 1 brs unit) (table 1).
The sediments in the map area are grouped
into depositional packages according to
marine
(
oxygen isotope stage (MIS)
ages. MIS is defined by
O from deep-sea cores that
measurements of
provide a proxy record of global ice volume and
corresponding sea level during the Pleistocene and
O
Holocene (Imbrie and others, 1984) (fig. 3).
values with higher positive values (e.g. 1-2 o/oo)
correspond to periods of increased global ice volume
and lowered sea level and are designated by an even
Marine Isotope Stage (MIS) number. For instance,
the sea-level lowstand associated with MIS 2, aka the
Last Glacial Maximum, occurred approximately 22-18
thousand years ago; the sea-level lowstand associated
with MIS 4 occurred approximately 70 thousand years
ago; and the sea-level lowstand associated with MIS 6
occurred approximately 130 thousand years ago (fig.
3). In the map area, sediments are grouped into four
different Marine Isotope Stage (MIS) periods that
correspond to higher sea level events, based on
radiocarbon and amino-acid racemization dating of the
sediments and seismic stratigraphic relationships.
These are MIS 1, MIS 3, MIS 5, and >MIS 6. (The
earliest period groups sediments older than the MIS 6
sea-level lowstand, i.e., sediments from multiple
Marine Isotope Stages, beyond the sampling and dating
capabilities of this study.)
Similarly, the sediments preserved above the
MIS 6 and MIS 4 lowstand erosion surfaces were
deposited during periods of sea-level rise after the MIS
6 and MIS 4 lowstands. The MIS 5 sediments (MIS 5
cbms) in the map area, identified at depth on the
seismic profiles, are characterized by migrating
channel features with sediment deposited as the
shoreline advanced landward and/or bayward. This
pattern extends for several km on many of the seismic
dip lines (lines running perpendicular to the shoreline)
in the study area. The MIS 3 deposits (MIS 3 ecbr) are
a mix of dissected channel fill and extensive horizontal
units of varied lithologies, as seen in the series of
prominent alternating flat-lying reflectors that
comprise the Pleistocene erosional remnants. In
addition, there is evidence of preserved MIS 3
barrier/shoreface deposits in the near-shore. These
may have been preserved as a result of their location in
an interfluve between the channel at Barnegat Inlet and
a former channel to the southwest, possibly in the
vicinity of Harvey Cedars.
The low subsidence rate and high-frequency
(~20 thousand years) glacially controlled sea-level
oscillations on the New Jersey shelf result in extensive
erosion and reworking of sediments by fluvial incision
during sea level lowstands and by marine erosion
Shore-attached, shore-detached ridges
The sand resource shoal identified previously
by NJGWS is a shore-detached ridge, formed through a
2
combination of eustatic and hydrodynamic factors.
The evolution of these continental shelf sand bodies is
characteristic of transgressive episodes in sea-level
cycles (Snedden and others, 1994, McBride and
Moslow, 1991, Figueiredo, 1984). Short-term alongshore inlet shifting due to longshore currents and other
factors, combined with longer term landward inlet
migration due to sea level rise, result in ebb-tidal delta
sediments being cut off from inlet sediment sources. In
the New Jersey offshore, they are subsequently
reshaped by longshore currents into ridges typically
oriented 10o to 30o oblique to the shoreline (fig. 1).
Currents and waves reshape the sand body, carving
swales that may cut below the base of the former delta,
adding relief to the shoal feature and transforming a
shore-attached ridge into a shore-detached ridge
(Snedden and others, 1994). The sand resource shoal
offshore Harvey Cedars may have developed from ebbtidal delta sands of an earlier, more southerly inlet,
perhaps located approximately 2.4 kilometers (1.5
miles) offshore of Loveladies, Long Beach Island,
interpreted from plots of the MIS 4 surface and MIS 3
thickness (Uptegrove, 2003).
3)radiocarbon dating of peat and wood fragments
found in the cores, and 4)amino-acid racemization of
shells from the cores.
Twenty-foot vibracores provide groundtruth
for seismic data, with core locations chosen to verify
lithologies, sedimentation patterns, and sediment age
(figs 4 – 7).
Sample Dating
Fragments of wood, charcoal, and peat were
collected for radiocarbon dating at a commercial lab
(Cores 12, 15, and 18) and shell material was collected
for amino acid racemization analysis (Cores 12, 13,
17a, and 18) (Wehmiller and Miller, 2000) (fig. 8).
Sampled core halves are stored with archived halves at
the NJGWS core storage facility. A complete account
of vibracore acquisition and analysis is in Uptegrove
(2003).
Seismic Stratigraphic Age Correlation
Three major reflectors were identified on the
seismic profiles (fig. 9).
These reflectors were
matched (“looped”) at line intersections on the seismic
profiles and correlated with the lithologies in
vibracores. The seismic data were digitized with USMAP software (Selner and Taylor, 1993) and
SonarWiz5TM, and contoured in SurferTM, Version 7.0,
creating topographic maps of four reflection surfaces
and thickness plots of three sequences (figs. 10 - 12).
The reflectors and the lithologic units they bracket are
referred to by Marine Isotope Stage (MIS) age, based
on analysis in Uptegrove (2003). A brief summary of
the age/sequence anaylsis follows.
The sand ridges typically have a convex upper
surface and a flat lower surface (Snedden and others,
1994). The flat lower surface is typically floored by a
gravel layer that was formed during the LGM, when
sea level was approximately 125 m (~400 ft.) lower
than it is today. Leading up to and during the LGM, the
surface was subaerial, as indicated by extensive
oxidation of the sand and gravel (in the vibracore
samples). The convex upper surface has a smooth
shape, due in part to the unconsolidated and texturally
more homogeneous sands which typically comprise the
upper sections of these ridges. In addition to the
Pleistocene gravel at the base of the shoal features,
some may contain an interbedded sand/clay unit of
variable thickness overlying the gravel (Smith, 1996).
The interbedded section is interpreted to be estuarine
sediments of the Holocene transgression (MIS1 be),
buried by advancing barrier sands and related shore
ridges (MIS1 brs) as Holocene sea-level continued to
rise (Smith, 1996; Uptegrove, 2003).
Analysis of dated samples from cores
A combination of amino-acid racemization
(AAR) (Wehmiller and Miller, 2000) (fig. 8) and
radiocarbon dates for samples from Cores 12, 15, 17a,
and 18 support a stratigraphic interpretation of three
sequences as: MIS 5, 3, and 1, corresponding to
approximately 125-80 thousand years ago, 55-35
thousand years ago, and 13 thousand years ago to the
present, respectively. The three major unconformities
that bound these sequences are, from oldest to
youngest, the MIS 6 sequence boundary (approx. 130
ka), the MIS 4 sequence boundary (approx. 70 ka), and
the MIS 2, Pleistocene/Holocene sequence boundary
(approx.18 – 13 ka) (Uptegrove, 2003).
Seismic, lithologic, and age correlation
The age and correlation of offshore units
identified on the map and in the seismic profiles was
determined based on 1) stratigraphic relationships seen
on the seismic profiles and 2)ground-truthed with
lithologic analysis of shallow core samples,
3
Table 2. Five dated samples which provide the ages of two of the laterally continuous units traced on the seismic data
throughout the map area. Table 2 also can be found on Sheet 1 of the map.
Core
15
12
12
17a
18
18
Depth in
Material
Lab #
Method
Age
core (m)__________________________________________________________________
4
charcoal GX-27722
conventional
31,600 +9760/-4280
radiocarbon
4.18
charcoal GX27719-AMS
AMS
>49,870
4.95
Spisula
JW2000-057
AAR
MIS 3
3.85
Spisula
JW2000-040
AAR
MIS 3
6.00
peat
GX027721-AMS
AMS
48,890 +/-3360 BP
5.85
Spisula
JW2000-043
AAR
MIS 5
Section AA’, CC’ table 3). This date indicates an MIS 1
age for the upper unit. Furthermore, a correlation is
made between the inshore Wellner and others (1993)
seismic data as shown in BB’. Correlation with the
Snedden and others (1994) seismic and vibracore data
further constrains the age, depth, character, and extent
of these 3 major depositional units.
Correlation of units
Of a larger group of both radiocarbon and
amino acid racemization dates derived from samples in
the study area, a subset of samples helped pinpoint the
ages of the two deeper extensive and seismically
continuous units as MIS 5 and MIS 3 (table 2). The
conventional radiocarbon date for the Core 15 sample
(4-m depth) of 31,600 +9760/-4280 indicates an MIS 3
age for this material. The radiocarbon date from Core
12 is inconclusive, but older than 49,870. The AAR
relative age date from a Spisula shell collected 0.8 m
deeper in the same unit (fig. 4) brackets the unit as
MIS 3 in age.
INTERPRETATION / DISCUSSION
OF MAP UNITS
Following is a discussion of the three
sequences in ascending order, from oldest to youngest.
MIS 5 Sequence
This sequence is continuous but subcropping
in the map area. The numerous channels oriented
NNE-SSW toward the seaward side of the seismic grid
contain sediments from ~5 to 12 m thick. (figs. 9, 10,
and 13).
Dip-line seismic profiles reveal extensive
cut-and-fill structures in the channels, distinctive for
their well-developed oblique progradational clinoforms
(fig. 9, Sections AA’ and BB’).
The Spisula sample from Core 17a (fig. 6)
produced an AAR relative age date that clusters with
the Core 12 Spisula relative age date, i.e. MIS 3.
Correlation of the unit on the grid of seismic profiles
confirms that these samples came from one continuous
depositional unit.
The peat sample from 6 m depth in Core 18
gave a radiocarbon age of 48,890 +/-3360. This date is
considered unreliable because it is older than 40,000
years BP. A Spisula shell from the same unit, 5.85 m
depth in Core 18 produced an AAR relative age date of
MIS 5, clustering with the known age date of the
reference Spisula sample from Parramore Island (J.F.
Wehmiller, oral commun., 2002).
The width of the channels, the multiple
incisions, and the direction of the prograding
clinoforms (shoreward) indicate that the channels
migrated shoreward over time (figs. 9, 13; Sections
AA’ and BB’). The multiple channels may have
functioned as separate flood- and ebb-tidal channels in
the bay. The steep clinoforms on the seaward side
would mark the location of the flood-tidal channel. It
is difficult to identify an ebb-tidal channel on these
seismic lines. However, two smaller channels are
visible inshore of the larger channel on line 25a (fig.
13, Section AA’). The MIS 6 surface gradient is
generally less steep on the landward side of the channel
(fig. 10A), and the thickest and deepest sections of the
The age of the uppermost laterally extensive
unit imaged on the seismic profiles in the map area is
correlated by a seismic tie (NJGWS line 76) to the data
of Ashley and others (1991) and Wellner and others
(1993), who report a Holocene radiocarbon date of
8810 +/- 170 years BP from a core in the uppermost
depositional unit drilled in Barnegat Inlet along a
seismic profile that ties to NJGWS’ seismic grid (see
4
sculpted either by MIS 2 fluvial systems or MIS 1
waves and submarine currents. These remnants resist
erosion because they contain distinct layers of
Pleistocene gravel, clay and sand. The sub-horizontal
seismic reflectors recorded in these features indicate
interbedded flat-lying sediments, probably deposited in
a bay, with occasional tidal-barrier-washover sand.
Core 17a, collected from one of the remnants, contains
sand with interbedded clay and pea gravel (figs. 6, 9).
MIS 5 channel are on the on the seaward side
(fig.10B).
A larger baymouth structure may have been
eroded by the numerous crossing channels seen in the
seismic profiles. Also, erosion surfaces seen on the
seismic profiles within the MIS 5 sediments (fig. 9;
Sections AA’ and BB’) indicate that the channel
features were eroded down by wave action as sea level
rose during the MIS 5 transgression. Similarly, erosion
surfaces seen on the seismic profiles indicate that the
MIS 3 transgression also eroded the original full
thickness of some of the MIS 5 channels.
MIS 3 thickness variations are caused by the
uneven underlying MIS 4 surface below and the varied
depth of the water bottom and the MIS 2 unconformity
above. In the near-shore (< 8 km from shore and < 62
ft. depth) zone, where MIS 1 sediments overlie MIS 3
sediments, the MIS 2 reflector forms the bounding
surface for the MIS 3 sediments (Sections AA’ and
BB’). The MIS 2 surface is of varied depth due to nonuniform erosion of MIS 3 sediments during the LGM.
The “low” in the MIS 4 surface forms the base of a
channel system running NNE-SSW, sub-parallel to and
~5 km west of the MIS 5 channels (fig. 11A). MIS 3
in the eastern section of the map area is characterized
by a relatively shallow section of the MIS 4 surface
and a marked thinning of MIS 3 sediments over it,
suggesting that this zone was an interfluve during MIS
4, and was only shallowly flooded during MIS 3 owing
to scant accommodation space.
Correlation of the Cape May Formation, Unit 2 and
MIS 5 units
The onshore Cape May Formation, Unit 2, or
Cape May 2 correlates to the offshore MIS 5 unit. We
are able to identify the MIS 5 in the offshore based on
the AAR date from Core 18 and by correlating the
seismic profiles. We can trace MIS 5 at depth beneath
Barnegat Inlet from seismic data (Wellner and others,
1993) and beneath Long Beach Island and Island
Beach from well logs (Section CC’).
The Cape May Formation, Unit 2 and MIS 5
are the oldest onshore-offshore correlated units in the
map area. We are not able to identify interglacial
deposits older than MIS 5 in the offshore owing to our
lack of age control for these relatively deep sediments.
Where preserved, they are evident on seismic profiles
as sub-horizontal reflectors between the MIS 6
reflector and the southeast-dipping Miocene-age
coastal plain units (fig. 9), with a total thickness of
only several meters, or up to 6 m if filling an incised
channel.
MIS 3 Sequence
The underlying MIS 4 sequence boundary
extends in the subsurface throughout the entire map
area. During MIS 4, the lowstand shoreline was located
approximately 70 km offshore (Carey and others,
1998). MIS 5 highstand deposits were subaerially
exposed on the shelf as far seaward as the MIS 4
lowstand shoreline (70 km offshore). In the map area,
the MIS 4 surface was flooded during the MIS 3
transgression (approximately 55 ka).
Thickness variations
Newly found MIS 3c shoreline
The MIS 3 depositional unit is underlain by the
MIS 4 surface, which is uneven, being deeper in the
central-western and southern sections of the study area
(fig. 11A). The MIS 3 sequence varies in thickness
from 3 to 30 ft. (fig. 11B). The top of the MIS 3
sequence is either the water bottom (seaward of ~ 8 km
from the shoreline, and deeper than ~62 ft.) or the MIS
2 reflector (inshore of 8 km and shallower than 62
ft.)(fig. 1). Where the top of the MIS 3 depositional
unit is the water-bottom surface, it is uneven, like the
MIS 4 surface, its bathymetric highs formed by
erosional remnants of MIS 3 deposits that have been
There is a newly found shoreline in the MIS 3
sequence. Seaward-sloping reflectors identified on six
seismic profiles extending from 1.5 to 6 km offshore
Long Beach Island show an orientation of N55oE,
about 30o oblique to the present barrier island
(Uptegrove, 2003), (fig.14; lines 25a and 76 on
Sections AA’ and BB’). They are interpreted as a
barrier island shoreface system associated with the 55ka highstand (fig. 14; Sections AA’ and BB’). Depth of
the top of the barrier island feature is ~19-20 m (62 -65
ft.) below sea level. This feature is truncated by the
MIS 2 lowstand unconformity or by small channel
5
features in the MIS 3 barrier island sands that also have
been truncated by the MIS 2 lowstand unconformity.
The barrier shoreface system is oriented in a more E-W
direction than the present shoreline by approximately
30o. (fig. 14; Section AA’). It is possible that this paleo
shoreline orientation results from a more northerly
position of the glacial forebulge during MIS 3
compared to during the LGM, owing to reduced
Laurentide ice volume during MIS 3. In that case, the
Baltimore Canyon Trough Hinge Line (fig. 2) may
have been the dominant regional boundary depositional
control at that time, with a tectonic high located
shoreward and to the north of the hinge line and the
basin located seaward and to the south.
Depth of MIS 3 in the near-shore
In previous studies of the Barnegat Inlet
subsurface (Wellner, 1990; Ashley and others, 1991;
Wellner and others, 1993), it was reported that the MIS
3 sediments in the near-shore extended to a depth of 28
m (92 ft.). This finding was based on interpretation of
seismic data from the Barnegat Inlet area, including the
near-shore off Long Beach Island. However, the
present study indicates that the MIS 3 sediments in the
near-shore extend to a depth of only 17 to 22 m (56 to
72 ft.). The 28-m/92-ft. surface interpreted as MIS 4
by Wellner (1990) and Ashley and others (1991)
correlates with the MIS 6 surface identified in this
study. The accumulation of MIS 3 sediments in the
near-shore is about half the thickness of that reported
in the earlier studies. Also, MIS 5 sediments in the
near-shore are at shallower depths than previously
thought.. The buried shoreline features identified by
Wellner and others (1993) and Ashley and others
(1991) are here identified as being in the MIS 5
sequence (Sections AA’ and BB’).
Former inlet offshore Harvey Cedars
The small, shore-normal MIS 3 channel
located approximately 1.5 km offshore of Harvey
Cedars, Long Beach Island on the MIS 3 contour plot
is interpreted as a former inlet which bisected the MIS
3 barrier island system (figs. 11A and B). The linear
thickening of sediments directly seaward of the small
inlet feature indicates an earlier trellis-style drainage
system or a combination of deep-thalweg inlet throat
and outboard shallowing ebb-tidal delta. Sequence
analysis of these MIS 3 features indicates that the
broad channel to the south predates the MIS 3
highstand barrier system (fig. 14). Perhaps MIS 4
subaerial erosion carved the NNE-SSW channel. This
intermediate-sized channel may have emptied into an
MIS 3 estuary in the southern section of the study area
and beyond. The thickness data in the southern section
of the seismic grid is inconclusive on this point.
Subsequent flooding during MIS 3 infilled the incised
channels with fine mud and sand. The lower third of
Core 12 consists of such channel-fill sediments, i.e.,
interbedded medium to fine sand and clay (fig. 4).
Near-shore depths of the MIS 4 surface of 56
to 72 ft. below sea level, and new seismic evidence
that Wellner and others’s (1993) shoreface deposits are
stratigraphically below the MIS 4 unconformity
(Uptegrove, 2003) suggest that the buried shoreface
deposits seen on Wellner and others’ (1993) near-shore
seismic lines are MIS 5 in age, possibly a remnant
from MIS 5b, the last lowering in MIS 5 (Section AA’).
MIS 5 and/or MIS 3 in upland deposits near Barnegat
Bay
In the map area, the Cape May Formation
forms a set of marine terraces along the west edge of
Barnegat Bay, where it overlies the Miocene Cohansey
or Kirkwood Formations (Owens and others, 1998)
(fig. 1). Newell and others (2000) mapped three Cape
May terraces (Cape May 1, 2, and 3, from youngest to
oldest), which they propose range in age from early to
late Sangamon, possibly to early Wisconsinan. For
consistency with earlier mapping and with numbering
conventions in pre-Quaternary formations, the New
Jersey Geological and Water Survey (2007) numbers
the Cape May 1 (Qcm1) as the oldest and 3 the
youngest, as originally defined in Newell and others
(1995). This convention is used here. Amino-acid
racemization dates on shells from the Cape May
peninsula and along Delaware Bay indicate that the
oldest Cape May deposit (Cape May 1) is older than
200 ka (Lacovara, 1997; O’Neal and others, 2000;
The prominent, elongate ridge of MIS 3
sediments seen on line 25b (fig. 9) indicates that the
basin in the map area was deep enough to hold
sediment accumulations at least 30 ft. thick during MIS
3. Given the very low slope of the seafloor, there may
have been a very broad bay in this area (landward of
the “mid-shelf high” of Carey and others, 1998) that
caused a gradual accumulation of sediment up until the
55-ka highstand. Note that the MIS 3 sedimentation
patterns are more planar and horizontal than the
underlying MIS 5 sediments (typified by relatively
steeper clinoforms and/or incised valley structures)
(fig. 9).
6
Wehmiller, 1997; Sugarman and others, 2007). The
Cape May 1 occurs in the subsurface beneath the Cape
May peninsula, and as erosional remnants of a marine
terrace as much as 20 m above sea level along the
Delaware Bay and Atlantic coasts. This elevation
indicates that it may have been deposited during MIS
11 (~400 ka) or 9 (~300 ka), when global sea level was
significantly higher than at present, or during earlier
highstands of similar elevation in the middle or early
Pleistocene. The Cape May 2 (Qcm2) forms a
prominent, continuous terrace approximately 6 to 10 m
above mean sea level along the Delaware Bay and
Atlantic coasts, and forms the spine of the Cape May
peninsula, where it overlies the Cape May 1. Aminoacid racemization dates on shells from shallow depth
on the Cape May peninsula indicate that the Cape May
2 was deposited during MIS 5 (Lacavora, 1997). The
amino-acid ages and elevation of the Qcm2 terrace
indicate that it probably was deposited during the
Sangamonian highstand (MIS 5e). As discussed
above, the Qcm2 and MIS 5 cbms are the oldest
onshore-offshore correlated units in the map area.
Recent optical luminescence studies have
found MIS 3 sediments at elevations as high as 11 m
above sea level in the Virginia coastal plain (Scott and
others, 2010) No data in the present study
unequivocally rules out or confirms MIS 5 or MIS 3 as
the age of the youngest Cape May terrace in New
Jersey.
There is evidence in the marine sediments that
both MIS 3 and MIS 5 sequences are truncated by the
MIS 1 erosion surface at a depth of about 18 m (59 ft.)
in the vicinity of Barnegat Inlet (Sections AA’ and
CC’). Additionally, Miller and others (2009) report a
radiocarbon age of 40,100 +/- 810 years from organic
matter associated with an Elphidium biofacies found
in the Great Bay no. 2 core hole at a depth of 14.2 m
(47 ft.) (table 4). This depth is in good agreement with
this study’s MIS 3 highstand depth of 15 to 18 m (49 to
59 ft.) below sea level. The shallow marine/brackish
Elphidium biofacies (Miller and others, 1997)
corroborates the existence of the extensive MIS 3
estuarine system seen in the seismic grid (fig. 11A and
B). The 40.1 ka date suggests that it was deposited at
the end of the MIS 3c highstand, or possibly reworked
during MIS 3b and 3a, when the area would have been
sub-aerial.
No onshore correlation to the MIS 3 sequence
Newell and others (1995) report a radiocarbon
date of 34,890 +/-960 BP from organic material
recovered from
a depth of 28 ft. (8.5 m)
(approximately 2.4 m below present-day sea level) in
the Ship Bottom (SB) no.1 auger hole (C7, Section
CC’ table 3). Pollen located directly above the dated
material, at a depth of 24 ft. (7.3 m), showed a mix of
temperate and colder region flora (Newell and others,
1995). Newell and others (1995) interpret the sediment
containing the dated material and pollen as Cape May
3 (Qcm3) marginal-marine and estuarine sediments of
middle Wisconsinan age (MIS 3), marking a marine
highstand overlain in turn by debris flow/alluvial fan
deposits of late Wisconsinan age (Qs1d). We reinterpret all the deposits above the dated material as
alluvial-fan sediments (included with the Lower
Terrace Deposits, unit Qtl, of NJGWS, 2007). The fan
was probably laid down during the LGM (MIS 2),
when permafrost led to slope erosion in the upland
west of the fan and deposition by local small streams
atop the Qcm2 terrace fronting the bay.
We reinterpret the dated organic material as deposited in a
freshwater wetland before the glacial maximum, as the
climate was slowly getting colder, as evidenced by the
mix of temperate and cold taxa in the pollen sample.
And, as stated above, Core 15 has a
radiocarbon date from a cedar fragment of 31 ka at 65
feet (19.8m) depth, just below the MIS 2 sequence
boundary. This cedar fragment found in sand in the
core could be part of the preserved MIS 3 barrier
feature, registering a relatively younger age (younger
than 40.1 ka) from a greater depth farther offshore as
the MIS 3b or 3a ocean retreated seaward.
MIS 1 Sequence
Two units are mapped in the MIS 1 sequence,
the lower bay/estuarine deposits (MIS 1 be) and
overlying barrier/shoal deposits (MIS 1 brs). The MIS
1 be unit is the leading edge of the Holocene
transgression, deposited in the quiet water of a bay or
estuary during sea-level rise. The sediments are
interbedded sand, silt and clay. This unit correlates
with the Qmm onshore unit, as the Qmm is the leading
edge of the Holocene transgression to date. In the
offshore, the MIS 1 be may crop out, or may be
overlain by shoals. During transgression, some of the
bay/estuarine sediments also may be eroded by the
high energy of the shoreface setting, as shoals and
barrier islands migrate shoreward with sea-level rise.
In some areas of the Atlantic coast, the underlying
7
bay/estuarine unit may be exposed in the surf zone,
beneath the barrier sands, as the barrier migrates over it
shoreward.
1 sand shoals, perhaps formed during the early stages
of the migration of the ridges. In contrast, the MIS 3
erosional remnants have sub-horizontal bedding and
steeper flanks and/or have a dissected profile, owing to
erosion of a mixed section of interbedded sands, clays,
and gravels (fig. 9).
The overlying barrier/shoal deposits (MIS 1
brs) form three areas of greater thickness in the MIS 1
sediments. They are 1) a Holocene sand ridge; 2) a
near-shore modern shoreface sand deposit; and 3)
Barnegat Inlet ebb-tidal delta sands (fig. 12B). As
described by Smith (1996), sand ridges typically are 1
km (0.63 mile) wide and 3-8 km (2-5 miles) long.
Shore-attached/shore-detached ridges develop initially
from ebb-tidal-delta deposits associated with barriersystem inlets (Snedden and others, 1994). A
combination of short-term lateral inlet shifting due to
longshore currents and other factors, combined with
longer term landward inlet migration due to sea level
rise results in the cutting off of ebb-tidal delta
sediments from inlet sediment sources. They are
subsequently reshaped by longshore currents into
ridges oriented 10o to 30o oblique to the shoreline.
Snedden and others (1994) found that the 5-fathom
(30-ft.) isobath outlines the location and extent of
several of these ridges offshore Long Beach Island (fig.
1).
Shore-detached ridge
The large shoal located approximately 4 miles
offshore Harvey Cedars (figs. 1, 12B) is very similar in
seismic profile and general morphology to the Peahala
Ridge of Snedden and others (1994), located about 11
km (7 mi) to the southwest. The main difference is
that this shoal is no longer attached to the shoreface.
Given the proximity of the Harvey Cedars shoal to
Barnegat Inlet, it most likely developed from ebb-tidal
delta sands of an earlier inlet, either those of Barnegat
Inlet which had migrated south of its present location,
or those of a separate inlet that has since closed.
Modern Shoreface
The near-shore bathymetric high running along
the NW edge of the study area 1 to 3 km (0.6 to 1.9
miles) offshore is part of the modern shoreface
deposits. Water depth in this area is 30-40 ft. (fig. 1)
and the sediment is 11 to 23 ft. thick (fig. 12B).
Similar thicknesses occur in the shore-detached ridge
discussed above.
The MIS 1 sequence as a whole (fig. 12B)
contains thicker, more complete sediment packages
than the MIS 3 and MIS 5 sequences because it is less
eroded. The MIS 5 and MIS3 deposits are typically
fragments of paleo-channel systems or estuaries, with
overlying
sediments
eroded
by
subsequent
transgressions (Ashley and Sheridan, 1994). As noted
by Smith (1996), recent (MIS 1) features also are
eroded. This is evident on line 25a, (sections AA’,
BB’) where currents have eroded the flanks of shoals
and left local areas of nondeposition and/or swales
parallel to the shoals. Swales between Holocene shoreattached and shore-detached ridges southeast of
Barnegat Inlet cut down into sands, interbedded
sand/mud, and gravels (lines 25a, 24b, cross-sections
AA’, BB’), forming the fensters seen in figure 1. In
some places, ridges of Holocene sand are forming in
swales (line 25b, seaward of Core 14, in Uptegrove,
2003). In addition, the MIS 2 surface under these
ridges can shift in depth, depending on whether the
area was downcut during the MIS 2 lowstand (Line
25a, section AA’, BB’), or remains as an erosion
remnant (Line 25b, fig. 9).
Ebb-tidal delta sands
MIS 1 sediments in the northern part of the
map area form a broad deposit of intermediate
thickness (2.5 to 4.5 m, 8 – 15 ft.). Here, the
uppermost MIS 1 brs unit is a sheet-like sand deposit
associated with the outer edge of the present-day
Barnegat Inlet ebb-tidal delta (figs.1, 12B). This broad
sheet-like feature is similar to sand deposits directly
seaward of Beach Haven and Little Egg Inlets
(Uptegrove and others, 1999). The MIS 1 brs unit is
more extensive south and east of Barnegat Inlet than to
the northeast (fig. 1), in part due to the net longshore
drift and residual current flow to the south and
southeast (Butman and others, 1979).
Depth-limited MIS 1 preservation in map area
As noted above, the MIS 1 sediments cover
only the near-shore section of the map area, to water
depths of approximately 19 meters (62 ft.) below sea
level (fig. 1). In deeper water (in the map area),
Holocene deposits are not preserved. What remain are
MIS 3 erosional remnants and the relatively planar and
In seismic profile, southeast-dipping crossbedding is locally evident on the seaward flank of MIS
8
gently sloping (~0.001) MIS 2 unconformity, formed
during the sea-level lowstand of the LGM. Based on
the lithology of cores 16 and 18, the NE-SW-oriented
bathymetric high in the area of those cores consists of
mixed Pleistocene sediments, without overlying MIS 1
interbeds or sand.
was eroded by wave action as sea level rose, and some
was preserved when barrier shoals formed on top of the
bay muds as the sea advanced shoreward.
Duncan and others (2000) note that the MIS 1
transgression took place on the mid-shelf ~16 to 10 ka,
that sea level advanced to the Franklin Shores at ~ 15.7
ka, and to the mid-shelf scarp by ~10.5 ka.
MIS 1 age/depth correlation
A radiocarbon age of 5,625 +/- 200 yr from
lignite at 46 feet (14 meters) below sea level in the
Island Beach Core (Miller and others, 1994) indicates
Holocene sediments to a depth of 58 ft. below sea level
(17.7 m) (table 4, Fig. 15, and C11, Section CC’).
Ashley and others (1991) report peat in bay muds dated
to 8,800 +/- 170 yrs BP from Core 3 (table 4, Fig. 15,
and C10 in CC’) from Barnegat Inlet at a depth of ~17
m (56 ft.). Seismic interpretations in Ashley and others
(1991) and Wellner and others (1993) show the base of
the Holocene in Barnegat Inlet at 18 m (59 ft.) below
sea level (Sections AA’ and CC’).
A basal peat from a depth of 16.07 m (52.7 ft.)
in NJGWS offshore Core 127 records a calibrated
radiocarbon age of 7960 +/- 921 (Miller and others,
2009) (table 4, Fig. 15).
In general, recorded
radiocarbon dates from the salt-marsh and estuarine
deposits (Qmm) in Great Bay are shallower (10 m
depth or less) and younger (6000 yr BP or younger)
than those from offshore samples (fig. 15). Thus, the
offshore MIS 1 bay/estuarine deposits (MIS 1be) track
the earlier/deeper phase of the Holocene transgression,
whereas the salt-marsh and estuarine deposits in Great
Bay (Qmm) comprise the leading edge of the
transgression. Though the Holocene sediments in
general are backstepping in this region, the Qmm and
the preserved MIS1be units are one in the same unit,
the onshore and offshore equivalents, respectively.
Likewise, the onshore beach and near-shore marine
sand (Qbs) and the offshore barrier/shoal deposits
(MIS1 brs) are onshore and offshore equivalents of the
same unit.
Radiocarbon dates from Great Bay (southern
section of Barnegat Bay) show sediment ages in the
back-barrier lagoon and marsh ranging from 4495 +/125 yrs BP at a depth of 27.1 ft. (8.3 m) to 500 +/- 70
yrs BP at a depth of 9.2 ft. (2.8 m) (Table 4, fig. 15)
(Psuty, 1986; Miller and others, 2009). Thus, backbarrier lagoon sediments were accumulating in the
vicinity of Great Bay at least as early as ~4500 yrs BP.
Correlation of onshore well log records and
offshore units
These ages and depths correlate generally with
depth of the MIS 2 unconformity in Area C. However,
the Island Beach core hole radiocarbon age of 5,625
+/-200 yrs. is slightly younger for its depth than the
age-depth relationship seen in the Barnegat Bay muds
and offshore Core 127 peat (Psuty, 1986; Miller and
others, 2009) (fig. 15). Perhaps the Island Beach
corehole sample (a clast within sand rather than an
organic deposit) was associated with downcutting at a
previous inlet located north of the present-day
Barnegat Inlet, such that younger sediments filled the
deeper channel before it closed up entirely
Gamma log records from barrier island well
sites show a low response from the upper barrier sands
and a change to a stronger gamma signal from the
underlying Holocene inter-bedded sand/mud unit
(Section CC’, table 3). Below an elevation of -15m (50 ft.), the lowermost part of this interbedded unit may
be MIS 3 bay deposits, based on the maximum
elevation of the MIS 3 highstand. Beneath the
interbedded sand/mud unit, the gamma signal is again
low. This gamma signal agrees with our findings on
the MIS 5 sequence, i.e., typical of bay-mouth or
barrier sand and gravel sediments.
The Holocene depositional environment in the
map area progresses from shallow marine to barrier
island to fluvial/estuarine. MIS 1 deposits do not exist
seaward of the ~20-m isobath in the map area. It is
possible that during Holocene sea-level rise, basal
Holocene interbedded layers formed in back-barrier
lagoons in a backstepping pattern. Some of the
material was preserved in the next pulse of sea-level
rise, some in ebb-tidal deltas (Wellner, 1990), some
Significantly, gamma log records from C2
(well no. 31) and C6 (well no. 129), on the western
margin of Barnegat Bay indicate marsh deposits to a
depth of 65 ft. and 58 ft., respectively. These gamma
records lack the uppermost weak signal attributed to
barrier sands that are found on the well logs from
barrier island sites (Section CC’). Likewise the C7
9
well record (SB no.1, which lacks a gamma record but
has a lithologic log), is here interpreted as late
Pleistocene fresh-water wetland overlain by late
Pleistocene lower stream- terrace deposits, with no
evidence of the Holocene marine-marsh and/or barriersand deposits.
similar to that of the MIS 1 sand ridges. However, the
depth of these sands and the thickness of overburden
render them unfeasible for dredging.
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Ashley, G.M., and Sheridan, R.E., 1994, Depositional
model for valley fills on a passive continental
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Zaitlin, eds., Incised-valley systems: origin and
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As noted above, the MIS 5 correlates with the
Qcm2. The weak gamma signal of the MIS 5
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MIS 6 reflector. The underlying Coastal Plain unit at
the Island Beach Borehole (C11, well no. 534, Section
CC’) is the Wildwood Member of the Kirkwood
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No large inland drainage in the map area
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perimeter, sand volume in the shoal offshore Harvey
Cedars is calculated as 49.1 million cubic meters, or
64.2 million cubic yards (Uptegrove and others, 2011)
(fig. 12B). The U.S. Army Corps of Engineers
dredged a section of this shoal for beach replenishment
on Long Beach Island in the mid-2000s. Ebb-tidal
deltaic sands located in the northern section of the map
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13

NJDEP - NJGWS - Geologic Map Series GMS 12

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