Page 1 TECTONOSTRATIGRAPHY AND NEOTECT ONIC

Formation.However, some other Liassic sequences are also
recognized in
the study area where their lithologic aspects
are different
(e.g. Kirklar Mountain, N of Moramil, W and S
of Dereagil localities,Plate 1). Thickness of the Vermis
formation
was measured
to be 30 m in the Pasaoglaninçal
hill
section.
Lithology and
Type Section:
The type section of the
Vermis formation was measured from the southwestern slope of
Pasaoglaninçal hill (1 km N of Vermis village) (Plate 1). In
this measured section, the sequence starts with greengrayish green,
massive conglomerates, bioclastic calcareous
and
conglomerates
(arenaceous,
bioclastic
echinoidal-crinoidal
biocalcirudite) (Figure
debris with
less amount
detrital
packstone
9). The
of rock
and
or
crinoidal
fragments are cemented by
The rock
fragments are
rocks. Quartz
fragments are
calcite (Figure 10).
mainly quartz
and metamorphic
is made
to grainstone
echinoidal
drussy sparry
mainly of
limestones
metamorphic in origin (Folk, 1974). The biodebris
up of echinoids, crinoids, echinoid spines, bryozoa
and lamellibranchiata fragments all of which are rounded and
well sorted. Above this level, green, massive to
bedded arenaceous
green calcareous
sandstone beds
bioclastic
carbonates
conglomerate lenses
are present
alternating
and green
thickwith
calcareous
(Figure 9). Crinoids, echinoids
and lamellibranchiata are the abundant fossil fragments with
minor metamorphic rock and quartz fragments,all of which are
cemented by
drussy sparry calcite. The sequence grades
28
Figure 15.
Major microfossil
biozonation of the Amasya Group.
groups
used
in the
1-3.
Globuligerina gr. oxfordiana (Grigelis) (Sample
No:882k, X 200)
4.
Globuligerina sp. (Sample No:882b, X 200)
5.
Clypeina jurassica (Favre) (Sample No:868w,
X 90)
6-7.
Mesoendothyra izjumiana Dain (Sample No:868c,d,
X 110)
8-1C. Alveosepta gr.
jaccardi (Schrodt)
(Sample
No:882b, 868b, X 60)
11-13.ProtopeMeroplis
trochoangulata
S~ptfontaine
(Sample No:5450,b, XL00)
14-15. Haplophramoides
joukowskyi
Charollais,
Brönnimann
and
Zaninetti)
(Sample
No:5450,a, X 110)
16-18. Montsalevia salevensis (Charollais, Brönnimann
and Zaninetti) (Sample No:5450,a, X 110)
19-22. Hedbergella
delrioensis
(Carsey)
(Sample
No:545b,e,X 110)
23.
25-26
.
Hedbergella sp.(Sample No:545b, X 200)
Hedbergella
planispira
(Tappan)
(Sample
No:545b,c, X 200)
27.
Hedbergella
gorbachikae
Longoria
(Sample
No:545b, X 200)
28-29. Globigerinelloides
ferreolensis
(Moullade)
(Sample No:545b, X 200)
30.
Globigerinelloides algerianus Cushman and Ten
Dam (Sample No:545b, X 200)
to the east between Saribugdayand BOgazköy villages is 25
km
(p ia te
3).
Terrace conglomerates:
These are
dominantly located
at the center of the Merzifon-Suluova basin between çayirözü
and Kapanci settlements and at the western slopes of eastern
margin (Plate 3). Conglomerates are strongly cemented or
grain supported and exposed at 30-40 m above the today's
valley bottom. The thickness of the conglomerates varies
from 0.5 to 2 m.
Swamps: A widespread swamp development is observed at
the southeastern
margin of
the Merzifon-Suluova basin. The
N-S flowing Tersakan river is shifted in E-W direction
between Kapanci and BOgazköy settlementsand results in a
swamp occurence
(Plate 3). It covers totally an area of 15-
20 square km. At
some other localities,swamps also occur
which are closely associated with faults.
Travertines: At few localities,namely the Alican hill
(NE
of
Harap settlement), Dereagil settlement and the
Sigirevlegi ridge,
some travertine occurences which are not
active today, are observed (Plate 3). In general,travertines
are grayish white, porous to compact, massive calcareous
tufa with a maximum thickness of 7 m.
128
Figure 83. Retreat of fault scarps and related physiographic
landforms developing along faults during the period of time.
Letters A to C indicate younger to older morphologies,
respectively. F.fault, dotted line is the continuation of
fault beneath sediments.
There are
several streams flowing from mountains and
entering the basin. Most of these subsequent streams die out
and leave
their load
lines. As
they
controlled by
in alluvial
enter
the
faults. The
dominantly consequent
basin,
fans or
they
along the fault
are
drainage system
structurally
in the basin is
which follows the fault valleys up to
recent depocenter (Figure 82, Plate 2). The main drainage
systems within the basin are Köseler stream, Keçiköyand
Gümüssuyu
streams,
Bulanik stream and Tersakan stream
whereby each stream flows through fault valleys (Figure 82).
The main
drainage system, Tersakan stream, flows across the
basin by
entering from
leaving the
Çeltek area (N of Suluova town) and
basin after Bogazköy village. Within the basin,
166
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i_i
i-i.
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il C_.........._-....
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1.-10
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or IIn'd'-s.>I_
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Flgure 87.
of northern
Tentative isket.ch cross sections
depicting
br_nch of t.he Neo-Tethye
1"Amasya
region.
posi.-T'I'iassic
evolutlon
PLATE 1 Giological Map
Soulhirn' Mar, .
af Ihi
r!P
-
!..f;;:
-I~-\
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o
i
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IIIOCIoI
PlATE 2
Cross Sections of the Southern
Geolagical
Merzifon-Suluova
Margin of
Besin. Amasya.
Asarcal.
hia
SW
1100
JKa
NEIS
500
o
200
G
1000
(meteis)
500
Tersakan
riVQr
500
1000
>.
a
?
F
o
900SW
YasSlçal
o
hill
Tc
500~ JKa
.0.'
c
D
KTk
~
JKa
500 i
i
100
A
,
Paleozoic
~
~
Jurassic -~r
SchistsSlates
~
E_
0-
U
~
Cretaceous
Amasya
Group
pre -Companian
~
~
Campanian-Maastrichtian
North Anatoiian
Ophioliiic Melange
Maaslrichtion-Paleocene(?)
Geyikozu
Formation
~
cr,
~
Tepetarla.
~
~
formaliQn
~
~
Findikti
.
Fo
rmation
-eo
~~
Tuzlugersin
.
f
~
N
c:io:i
ö '::
~
Marble
blocks} ~....
~
CretaceOU5 petagic
carbonates
~:X
~ ~
} '"
Luteiian
a.
5
C,
ormation
i=r.T'5'I
Kutunun
~
formation
}
-" ~
Ü
0-~
öA.
;;::
~
~
Cindere
group
Plio- Ouaternary
Quaternary
1':.: TQs
=1
o
F"TL Moramil
dacite
~
Suluova
group
Fluvial
sediments
j