Evolution of and Factors Controlling Eocene Sedimentation

25 Pages·2005·2.92 MB·English

Turkish Journal of Earth Sciences(Turkish J. Earth Sci.), Vol. 14,2005, pp. 311-335.Copyright 'T(cid:134)B(cid:220)TAK
Evolution of and Factors Controlling Eocene
Sedimentation in the Darende-Balaban Basin, Malatya
(Eastern Turkey)
KEMAL G(cid:134)RB(cid:134)Z1& MURAT G(cid:134)L2
1 (cid:130)ukurova University, Faculty of Architecture and Engineering, Department of Geological Engineering,
Balcal(cid:221), TR—01330 Adana, Turkey (E-mail: [email protected])
2Mersin University, Faculty of Engineering, Department of Geological Engineering, (cid:130)iftlikk(cid:154)y,
TR—33343 Mersin, Turkey
Abstract:Collision of the Arabian and Anatolian plates affected evolution of basins located along the southern flank
of the Anatolian Plate. The Darende-Balaban foreland basin is one such basin — a basin filled with Upper Cretaceous
and Eocene sediments, accumulated unconformably and transgressively above ophiolitic and carbonate basement
rocks. This basin is locally surrounded, to the north and south, by Late Jurassic—Early Cretaceous structural highs
created by tectonic elements during the collision of Arabia and Anatolia. This paper aims to describe the factors
controlling and evolution of the Eocene sedimentation in the Darende-Balaban basin.
The basin fill comprises two distinct sequences separated by an angular unconformity: (1) the Upper
Cretaceous continental to shallow-marine sediments that fall into three formations, namely reefal carbonates of
the Tohma formation, the continental to shallow-marine Ulup(cid:221)nar formation and shallow-marine calcarenites of the
K(cid:221)rankaya formation. In the southern and northern parts of the basin, there are distinct lateral and vertical
lithological variations in each formation; (2) Lutetian shoreline to shallow-marine successions of the Korgantepe
formation, shallow-marine to offshore successions of the Yenice formation, and reefal carbonates of the Asartepe
formation. The basin fill ends with the Priabonian shallow-marine Darende formation. Several sedimentological
sections were measured and rock samples were collected for petrographic and palaeontological studies to examine
facies distribution, lithological and sedimentological changes in the Eocene units, and to obtain precise dates for
the sedimentary succession.
The results suggest that Eocene sedimentation in the Darende-Balaban foreland basin was highly affected
externally by the north—south compressional regime as a consequence of collision between the Anatolian and
Arabian plates which commenced just after the Late Cretaceous and continued until the Eocene. The basin fill was
also affected internally by the sedimentary factors or processes, such as provenance, basin topography,
sedimentary input and climate.
Key Words:Darende-Balaban basin, Malatya, Turkey, Eocene, foreland basin, factors controlling sedimentation
Darende-Balaban Havzas(cid:221)nda Eosen Sedimantasyonunun Evrimi ve
Sedimantasyonu Kontrol Eden Fakt(cid:154)rler, Malatya (Do(cid:219)u T(cid:159)rkiye)
(cid:133)zet:Arap ve Anadolu levhalar(cid:221)n(cid:221)n s(cid:221)k(cid:221)(cid:223)mas(cid:221), Anadolu levhas(cid:221)n(cid:221)n g(cid:159)ney k(cid:221)sm(cid:221)nda yer alan havzalar(cid:221)n olu(cid:223)umunu
etkilemi(cid:223)tir. Bu (cid:141)al(cid:221)(cid:223)ma Darende-Balaban havzas(cid:221)n(cid:221)n olu(cid:223)umunu ve sedimantasyonu etkileyen fakt(cid:154)rleri
a(cid:141)(cid:221)klamaktad(cid:221)r. (cid:133)n(cid:159)lke (foreland) (cid:154)zellikteki Darende-Balaban havzas(cid:221) yersel olarak kuzey ve g(cid:159)neyde Arap ve
Anadolu levhalar(cid:221)n(cid:221)n (cid:141)arp(cid:221)(cid:223)mas(cid:221) ile ilgili tektonik unsurlardan olu(cid:223)an yap(cid:221)sal y(cid:159)kselimlerle s(cid:221)n(cid:221)rlanm(cid:221)(cid:223)t(cid:221)r. Havza
dolgusu genel olarak a(cid:141)(cid:221)sal diskordan ve transgresif olarak ofiyolitik ve karbonat kaya(cid:141)lardan olu(cid:223)an temeli
(cid:159)zerleyen (cid:134)st Kretase ve Eosen sedimanlar(cid:221) ile temsil edilir.
Havza dolgusu Ge(cid:141) Kretase(cid:213)ye ait ve havzan(cid:221)n g(cid:159)ney ve kuzey k(cid:221)sm(cid:221)nda yanal ve d(cid:159)(cid:223)ey litolojik farkl(cid:221)l(cid:221)klar
sunan karasal-s(cid:221)(cid:219) denizel sedimanlar(cid:221)n ardalanmalar(cid:221)ndan olu(cid:223)maktad(cid:221)r. Bunlar: resifal (cid:154)zellikteki Tohma
formasyonu, karasal-s(cid:221)(cid:219) denizel Ulup(cid:221)nar formasyonu ve s(cid:221)(cid:219) denizel kalkarenitli K(cid:221)rankaya formasyonudur. (cid:134)st
Kretase birimleri diskordan olarak k(cid:221)y(cid:221)-s(cid:221)(cid:219) denizel Korgantepe formasyonu (L(cid:159)tesiyen), s(cid:221)(cid:219) deniz-k(cid:221)y(cid:221) ilerisi
(cid:154)zellikteki Yenice formasyonu (L(cid:159)tesiyen), resifal (cid:154)zellikteki Asartepe formasyonu ve son olarak s(cid:221)(cid:219) denizel
Darende formasyonu (Priaboniyen) taraf(cid:221)ndan (cid:159)zerlenmektedir. Eosen birimlerindeki fasiyes de(cid:219)i(cid:223)imleri, litolojik
ve sedimantolojik de(cid:219)i(cid:223)iklikleri incelemek (cid:159)zere sedimantolojik kesitler (cid:154)l(cid:141)(cid:159)lm(cid:159)(cid:223) ve (cid:154)rnekler derlenmi(cid:223)tir.
Sedimanter istifin ya(cid:223)(cid:221)n(cid:221) ve fosil i(cid:141)eri(cid:219)ini saptamak amac(cid:221)yla paleontolojik (cid:154)rneklerde al(cid:221)nm(cid:221)(cid:223)t(cid:221)r.
311
EOCENE SEDIMENTATION IN THE DARENDE-BALABAN BASIN (MALATYA)
Bu (cid:141)al(cid:221)(cid:223)madan elde edilen veriler Eosen sedimantasyonunun Ge(cid:141) Kretase sonras(cid:221)nda olu(cid:223)an ve Eosen(cid:213)de de
olu(cid:223)umuna devam eden Anadolu-Arap levhalar(cid:221)n(cid:221)n kuzey-g(cid:159)ney y(cid:154)ndeki s(cid:221)k(cid:221)(cid:223)ma rejiminden olduk(cid:141)a etkilendi(cid:219)ini
g(cid:154)stermi(cid:223)tir. Bu (cid:154)n(cid:159)lke (foreland) havzas(cid:221)n(cid:221)n dolgusu i(cid:141)sel olarak kaynak havza, havza topografyas(cid:221), sedimanter
girdi ve iklim gibi sedimantolojik etmenlerden de etkilenmi(cid:223)tir.
Anahtar S(cid:154)zc(cid:159)kler: Darende-Balaban Havzas(cid:221), Malatya, T(cid:159)rkiye, Eosen, (cid:154)n(cid:159)lke havzas(cid:221), sedimantasyonu kontrol
eden fakt(cid:154)rler
Introduction shallow-marine, fan and deep-sea environments ((cid:133)nal &
G(cid:154)z(cid:159)bol 1992). The nappes evolved and were emplaced
The Darende-Balaban basin (Malatya, eastern Turkey) is
towards the south during Late Cretaceous, Early—Late
located in the eastern part of the Taurides and evolved
Eocene and Early—Middle Miocene times. Subsequent to
under the effects of the Alpine orogeny (Figure 1). The
complete consumption of the Neotethyan ocean,
Taurus Mountains are divided in three main tectonic
neotectonic deformation in Turkey began.
elements: namely, western, central and eastern (Ketin
1960, 1966; Alt(cid:221)nl(cid:221) 1966; Arpat & (cid:222)aro(cid:219)lu 1972; (cid:133)zg(cid:159)l The neotectonic architecture of Turkey is controlled
1976; Robertson 2000). (cid:133)zg(cid:159)l (1976) emphasized that by three major structural elements: (1) the Aegean-
the Ecemi(cid:223) fault forms the western boundary of the Cyprean Arc; (2) the North Anatolian Fault System; and
eastern Taurides, while Robertson (2000) implied that (3) the East Anatolian Fault System (EAFS) (e.g., Bozkurt
the junction of the East Anatolian Fault Zone and Dead 2001 and references therein). The EAFS is the major
Sea Fault Zone near Kahraman Mara(cid:223) is the western limit. structural element closest to the Darende-Balaban basin.
On the other hand, Akay (1989) claimed that the eastern The age and evolution of this structure is under debate
Taurides is the region located to the east of the East and proposals range between Late Miocene and 3 Ma
Anatolian Fault System and lies to the north of the (e.g., Bozkurt 2001 and references therein). Conversely,
Southeast Anatolian thrust belt. Neotethys opened after others claim that sinistral motion along the EAFS
the Late Triassic, following closure of Palaeotethys commenced sometime between 5—3 Ma following
((cid:222)eng(cid:154)r & Y(cid:221)lmaz 1981). The northern branch of cessation of motion along the Malatya-Ovac(cid:221)k fault zone
Neotethys was situated between the Anatolide-Tauride (Westaway & Arger 1996, 2001; Westaway 2003).
platform to the south and the Pontides to the north,
Several researchers have indicated that a
while the southern branch was situated between the
compressional regime prevailed in the area between
Anatolide-Tauride platform to the north and the African-
Malatya and Elaz(cid:221)(cid:219) causing foreland-basin(s) development
Arabian plate to the south ((cid:222)eng(cid:154)r & Y(cid:221)lmaz 1981;
during the Late Cretaceous—Early Palaeocene (Yazgan
Yazgan 1984; Kozlu 1997; G(cid:159)l 2000). North-dipping
1984; Cronin et al. 2000; Aksoy et al. 2005). A
subduction zone(s) developed as a consequence of
continuum of Anatolia-Arabia collision during the Eocene
collision between the Eurasian and Arabian-African plates
resulted in formation of rather narrow, elongate
during the late Early Cretaceous (Yazgan 1984) or Late
sedimentary basins at the margins of these plates,
Cretaceous ((cid:222)eng(cid:154)r & Y(cid:221)lmaz 1981; Kozlu 1997; G(cid:159)l
particularly in the foreland and on the southern flank of
2000). Volcanic arcs, and several back-arc and foreland
the Anatolian plate. Some of these are described as
basins developed in connection with subduction during
elongate strike-slip/thrust-bounded basins (e.g., Van and
Late Cretaceous—Palaeocene time (e.g., (cid:222)eng(cid:154)r & Y(cid:221)lmaz
Mu(cid:223) basins; Dewey et al.1986). During this time, arcs
1981; Yazgan 1984; Akta(cid:223) & Robertson 1984, 1990;
and back-arc basins developed in the Elaz(cid:221)(cid:219) and Hazar
Robertson 2000; Aksoy et al.2005). Yazgan & Chessex
areas (Aksoy et al.2005), while initially foreland basins
(1991) implied that the collision between the arc and
also developed over the Arabian plate and consuming
continent began in Late Campanian—Early Maastrichtian
oceanic plate situated between the Arabian plate and the
time and continued until the Early Eocene. The geologic
Maden Complex (Yazgan 1984). The continuum of this
units that belong to this time interval occur as para-
compression resulted in closure of Neotethys and caused
allochthonous and/or autochthonous units that overlie
large tectonic- slab emplacements and development of
either the allochthonous Malatya metamorphics or
several intramontane basins with irregular basin surfaces
sedimentary successions deposited in continental,
upon these slabs (Yazgan 1984).
312
K.G(cid:134)RB(cid:134)Z & M. G(cid:134)L
a
27 33 39 45
BlackSea GreaterCaucasus
LesserCaucasus
PONNTAIDFEZS PONTIDES N E A F Z
b
wTeasAutreiNrdneAsTOLceIAntNralTPaLuAridTeEs KM E A F Z BMitlis-ZagrosSuEtuarseteZrnonTeaurides
AegeanSea N
Cyprean ARABIAN
Arc FZ PLATE
S
D
MediterraneanSea
0 km 200
AFRICANPLATE
b
YFZ
ERZİNCAN
SİVAS
Akdağmadeni YGFZ
F
K Divriği Ovacık
Kangal O F
M
Y G F Z
KAYSERİ Yuzyurdu OF
M Hazar
Darende
G(cid:246)l(cid:252)
Erciyes K.MARAŞ
Dağı
E
N
O
MALATYA Z
FZ S(cid:252)F A U L T
G F
Y G(cid:246)lbaşı N
A
LI N
O
A T
N
A
E A S T
0 50
Ceyhan
ADANA
km
Figure 1. Simplified tectonic map of Turkey showing major neotectonic structures and plates (a) and
location map (b)of the study area (simplified and modified from Bozkurt 2001). M — Malatya,
KF — Kangal Fault, KM— Kahramanmara(cid:223), MOF — Malatya-Ovac(cid:221)k Fault, S(cid:159)F — S(cid:159)rg(cid:159) Fault, YFZ
— Y(cid:221)ld(cid:221)zeli Fault Zone, DSFZ — Dead-Sea Fault Zone, EAFZ— East Anatolian Fault Zone, NAFZ—
North Anatolian Fault Zone, YGFZ — Yakap(cid:221)nar-G(cid:154)ksun Fault Zone, and NEAFZ — Northeast
Anatolian Fault Zone.
313
EOCENE SEDIMENTATION IN THE DARENDE-BALABAN BASIN (MALATYA)
The Darende—Balaban basin is one of these foreland ophiolites consist of serpentinite, gabbro, spilite and
basins, and is connected with a back-arc basin (Yazgan Jurassic limestone olistoliths (Akku(cid:223) 1970, 1971;
1984; Akta(cid:223) & Robertson 1984, 1990; (cid:133)zkul 1988; Robertson 2000).
Cronin et al. 2000) located to the ESE, namely the
The sedimentary fill of the Darende-Balaban basin
K(cid:221)rkge(cid:141)it (Turan 1993; Aksoy 1988) or Elaz(cid:221)(cid:219) basin
(Figures 2 & 3) is composed mainly of shallow-marine to
(Cronin et al. 2000; Aksoy et al. 2005).
offshore sediments and can be divided — based on age and
Jurassic—Cretaceous limestones and Upper Cretaceous
contact relationhips — into three parts: pre-Eocene,
ophiolites comprise basement to this basin. Upper
Eocene and post-Eocene units.
Cretaceous and Tertiary sediments successively and
unconformably overlie the basement rocks (Akku(cid:223) 1970,
1971). Pre-Eocene Basin Fill
Many general geological and petroleum exploration- As a result of the collision between the Taurides and the
related studies have been done in and around the Arabian Plate during the Late Cretaceous, the (cid:220)spendere
Darende-Balaban basin since 1938 (Blumenthal 1938; ophiolite was thrust over Jurassic—Cretaceous platform
Baykal 1944; Demirta(cid:223)l(cid:221) & Ayan 1963; (cid:134)rg(cid:159)n 1963; carbonates (Akku(cid:223) 1970, 1971; Yazgan 1984). Thus,
Ayan & Bulut 1964; Wirtz 1965; Akku(cid:223) 1970, 1971; several narrow and elongate basins, such as the Darende-
Kurtman & Akku(cid:223) 1974; Kurtman 1978; (cid:133)r(cid:141)en 1985- Balaban basin, formed and evolved in and around this
1986; Metin et al. 1987; Tarhan 1987; Yazgan & thrust zone (Yazgan 1984; Dewey et al.1986). The basal
Chessex 1991; Dilek et al.1996; Dumanl(cid:221)lar et al.1999). part of the basin fill is represented by Upper Cretaceous
Despite this enormous amount of work, studies of the siliciclastics (Ulup(cid:221)nar formation), reefal limestones
sedimentological aspects and evolution of the basin are (Tohma reefs) and limestones (K(cid:221)rankaya formation);
scarce. Studying the evolution of this basin is therefore these rocks unconformably and transgressively overlie the
important and would contribute to a better basement limestones (Jurassic) and ophiolites
understanding of the regional processes related to (Cretaceous). Reddish conglomerates and sandstones of
collision of the Anatolian and Arabian plates and the Ulup(cid:221)nar formation (Figure 4) are composed of
consequent closure of Neotethys. The depositional pebbles derived and transported from the nearby
characteristics of the basin have been examined in order basement highs. As the transgression continued, reddish
to assess the external and internal factors that controlled to beige, medium- to fine-grained sandstones together
basin evolution. with beige siltstone and marl alternations developed in
the upper parts of the Ulup(cid:221)nar formation. The overlying
reefal limestones (Tohma reef) were deposited on
Stratigraphy and Sedimentology of the Basin
palaeotopographic highs as patch reefs where the water
The basement to the Darende-Balaban basin is was clean, warm and nutrient-rich (Akku(cid:223) 1970). These
represented by Upper Jurassic—Lower Cretaceous carbonate build-ups contain abundant microfossils and
carbonate and ophiolitic rocks that are exposed on have transitional contacts with underlying fine-grained
tectonically uplifted structural highs north and south of clastics of the Ulup(cid:221)nar formation. Reactivation of the
the basin (Figure 2). The oldest basement unit is the basin-bounding extensional faults restricted the basin and
Geniz limestone, comprising limestone, chert, chalk and caused deposition of first coarse-grained then fine-
some dolomite horizons of Jurassic—Early Cretaceous age grained sediments in a shallow-marine environment.
(Figures 2 & 3). The limestones are interpreted as having These are conformably overlain first by clayey limestones
formed on a shallow-marine carbonate platform during and later by limestones of the K(cid:221)rankaya formation,
the opening of the southern branch of Neotethys (Akku(cid:223) forming the uppermost levels of the Cretaceous
1970, 1971). These shallow-marine carbonates are sedimentation in the basin (Figure 4). This was followed
tectonically overlain by tectonically transported ophiolitic by regression and uplift and consequent erosion in the
rocks of the (cid:220)spendere ophiolites — remnants of Neotethys Late Cretaceous (Akku(cid:223) 1970).
(Metin et al. 1987; Dumanl(cid:221)lar et al. 1999). These
314
K.G(cid:134)RB(cid:134)Z & M. G(cid:134)L
G(cid:252)r(cid:252)n
Geniztepel
+ -
+-
Darende
+ Balaban
-
+-+- studyarea
+- Akçadağ Malatya
+- +- EBlbeisythaainzllseki 0 40km
3
Alidedetepe N
DARENDE
22kkmm
alluvium
Etretepe
Karadeğin Suçatı
Akçatoprak ÇaybaşıFm.
G(cid:252)d(cid:252)l
Pliocenevolcanics
DarendeFm.
AsartepeFm.
YeniceFm.
KorgantepeFm.
pre-Eoceneunits
BALABAN
+-
Yenice
+ - ophiolites
river
2
Yeniceşuğul
+ - fault
Aşağıulupınar
+- Thrust
Oturaktepe +- + - 1 3 Alidedesection
-
Kepez
İmamelitepel + Dağı 2
Yenicesection
Kahramanlar
-+ 1
AsarTepesection
Yukarıulupınar
Figure 2. Simplified geological map of the Darende-Balaban basin and locations of measured sections (modified after Akku(cid:223)
1971).
315
EOCENE SEDIMENTATION IN THE DARENDE-BALABAN BASIN (MALATYA)
TECTONICANDOTHEREVENTS thrusting-anduplift-related(neotectonic)erosion compression&upliftatthebasinmargins;localsea-levelfluctiations compression&upliftatthebasinmargins;localsea-levelfluctiations compression&upliftatthebasinmargins;localsea-levelfluctiations thrusting localsea-levelfluctiations thrusting Noscale
e
s
RELATIVESEA-LEVELCHANGESri Notstudied otstudied
all n
f
F
OT-
EUEN
ELATIVERATCLASTICINPCARBONATDEPOSITIO
R
EXPLANATION ,uncementedgravel,sandandsiltdeposits angulargravellyconglomerateandlocalsandstoneandmarlbeds greenish-lightgreyconglomerateinterbeddedwiththinsandstone,Usiltstoneandmarlalternations;evaporiticlenses(u)areabundant U UU carbonateswithcoral,algeaandnummulitefossils;carbonatesareinterbeddedwithsandylimestonesandthinmarls siltstoneinterbeddedwithmarlsinlowerandupperparts,calcarenitesinthemiddlepart(south);siltstoneinterbeddedwithmarls(north). darkgreenconglomerates,looselycementedfine-medium-grainedsandstoneandsandymarls lightyellowandwhitecoloredcalcarenite. redshale,sandymarl,sandstoneandconglomeratealternations;coarse-grainedconglomerateisdominantinlowerparts;grainsizedecreasesupward biohermallenseswithincalcarenites lightgreyorwhiterecrystallizedlimestones ophiolitesthrustedontolimestones modified and redrawn after Akku(cid:223) 1971).
UTH UU UU asin (
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OLOGY U U ende-Bala
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FORMATION alluvium Çaybaşı Darende Asartepe Yenice Korgantepe Kırankaya ranıapmulUhoT GenizLimestone neralized str
EGATS NAINOBAIRP NAITETUL NAITHCIRTSAAM-NAINAPMAC Ge
SEIRES ENECOILP E N E C O E SUOECATERCREPPU SUOECATERC.U-CISSARUJ 3.
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316
K.G(cid:134)RB(cid:134)Z & M. G(cid:134)L
S N
Asartepeformation
KırankayafoKrmoarngtiaonntepeformation Ye nic e f o rAmsstaar artitoiTgenrpaep hic s e c tio n
o
ati
20m m
r
o
f
r
a
n
pı
u
Ul
Figure 4. General view of the geologic units in the Darende-Balaban basin. The Lutetian includes conglomerates of the Korgantepe
formation, calcarenites of the Yenice formation and reefal limestones of the Asar Tepe formation, and unconformably overlies
pre-Lutetian clastics of the Ulup(cid:221)nar formation and limestones of the K(cid:221)rankaya formation. White dashed line represents the Asar
Tepe stratigraphic section.
Eocene Basin Fill The Korgantepe Formation.The Korgantepe formation
overlies carbonates of the K(cid:221)rankaya formation and
Eocene basin fill unconformably overlies the pre-Eocene
siliciclastics of the Ulup(cid:221)nar formation along an angular
rocks and is represented by very shallow- to deep
unconformity and is overlain gradationally by the Yenice
(offshore)-marine sedimentary successions with some
formation (Figures 3 & 5). The maximum measured
biohermal build-ups and evaporitic occurrences. The
thickness is about 100 m in the northeastern part of the
succession comprises the Lutetian Korgantepe, Yenice and
Darende-Balaban basin (Akku(cid:223) 1971) and only 4—25 m in
Asartepe formations, and the Priabonian Darende
the south. These rocks have also been named the
formation. The lower parts of the succession (Lutetian)
Korgantepe conglomerates because of their coarse-
are aligned parallel to the Upper Cretaceous basement
grained character (Akku(cid:223) 1971).
rocks and display thickness- and facies-change variations
over short distances in both N—S and E—W directions. The Two sections were measured to identify and analyze
Priabonian rocks are relatively widespread and exhibit the lithological character of the Korgantepe formation at
low-angle dips (10—20¡) compared to the Lutetian Asar Tepe and Yenice. This formation commences with
sediments (15—45¡) in the marginal parts of the basin. conglomerates unconformably overlying fine-grained
Three sections (two from the southern part and one from sediments of the Ulup(cid:221)nar formation; the contact is sharp
the northern part of the study area) were measured to and erosional in the two measured sections. The
examine possible lateral and vertical differences in the conglomerates display thinning- and fining-upward
sedimentary succession, particularly between the character, and typically pinch-out over short distances
northern and southern parts of the basin (Figure 2). and grade into pebbly sandstones and sandstones.
Those differences will be discussed in the following
Five conglomeratic packages with various thicknesses
sections.
are observed in the Asar Tepe section (Figures 4 & 6). On
317
EOCENE SEDIMENTATION IN THE DARENDE-BALABAN BASIN (MALATYA)
Yeniceformation
K
or
g
a
nt
e
p
Ulupınarformation ef
or
m
ati
o
n
5m
Figure 5. Field view showing conglomerates of the Korgantepe formation that overlie the fine-grained clastics of the Ulup(cid:221)nar
formation with an angular unconformity. Marl and siltstone alternations of the Yenice formation concordantly overlie
sandy conglomerates of the Korgantepe formation.
the other hand, there is only one conglomeratic package Similar coarse-grained sediments deposited in
at the base of the Yenice section in the SW part of the terrestrial (alluvial fan) or shallow-marine environments,
basin (Figure 7). The thickness of individual conglomerate with asymmetric distributions along basin margins, have
beds ranges from 2 m to 4 m. Conglomerates are been reported from different localities (in the vicinity of
polygenic, grain-supported and well-imbricated. They Karaman: (cid:222)afak 1999; in the Sivas basin: Ocako(cid:219)lu 1999;
first grade upward into pebbly sandstones (1—1.2 m in the (cid:130)ank(cid:221)r(cid:221) basin: Akg(cid:159)n et al.2002; and in Igualada,
thick), then into 20—30-cm-thick medium-grained NE Spain: Taberner et al.2002). Levin (2003) indicated
sandstones, and finally thin-bedded, fine-grained that compression and uplift along basin margins cause
sandstones intercalated with marls. release of coarse-grained particles and formation of
clastic wedges. Leeder (1982) emphasized that shoreline
The conglomerates and sandstones are composed
changes with subsidence at basin margins cause lateral
dominantly of subrounded-rounded grains of crystallized
and vertical facies changes in shallow-marine
limestone, ophiolitic material and Cretaceous siliciclastic
environment.
material that crop out at the southern margin of the
basin. The Korgantepe formation is characteristically The erosional base of the conglomeratic beds, the
fossiliferous and contains large benthic foraminifers of lenticular geometry of whole strata, sequence
Lutetian age, such as Assilina exponens (Sowerby), characteristics and palaeontological evidence from the
Nummulites beaumontid(cid:213)Archiac & Haime, Nummulites Korgantepe formation are consistent with deposition in a
millecaput Boubee, Nummulites praeaturicus Schaub shoreline- to shallow-marine (shoreline-shore face)
(Nummulites, Assilina) that are abundant (up to 80 %) in environment (Nazik 1993; Erdo(cid:219)an 2003). A sharp
some levels (Figure 8a). There is also a sandstone horizon erosional base and imbricated conglomerates in the first
in the upper part of the conglomerate which is classified part of the section, along with abundant large benthic
as lithic arenite (Pettijohn et al.1987; Figure 8b). foraminifers, may reflect the initial flooding of the
318
K.G(cid:134)RB(cid:134)Z & M. G(cid:134)L
m)
(
seriesstage formation thickness lithology sedismaemgnrptaalienrylsosicztareut,icotnures, EXPLANATIONFOR
MEASUREDSECTIONS
m.100
f
e loadcast
p
e parallellamination
art normalgrading
As flutemark
groovemark
90 imbrication
benthicforaminifera
pelecypod
gastropoda
echinoid
ostracod
80 limestone
calcarenite
marl
gypsum
70 Clastics
cl s f m c p b
sand
cl:clay
n s:silt
o f:finesand
ti 60 m:mediumsand
N a
E m c:coarsesand
NA r p:pebble
I o b:boulder
ET f
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OT c 50
i
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Y
40
30
20
n
o
ati
m
or 10
f
e
p
e
nt
a
g
or
K 0
pre-Lutetian cl s f m c p b
sand
Figure 6. Asartepe measured stratigraphic section of the Asar Tepe formation.
319
EOCENE SEDIMENTATION IN THE DARENDE-BALABAN BASIN (MALATYA)
m)
(
seriesstage formation thickness lithology sedismaemgnrptaalienrylsosicztareut,icotnures, seriesstage formation thickness(m) lithology sedismaemgnrptaalienrylsosicztareut,icotnures,
250
n
o
I
t
a
m
r
o
f
100
e
p
e
t
r Figure11
n a
o As
I
t
a
m
r
N o
E
A f
N
I
ET N 200
CE e E
A
OT Ic N I
EU n E T
L e C En
Y O To
Figure10b E UI
Lt
50 a
m
r
o
f
e
c
Figure10a I Figure10d
n
e
Y
150
m. Figure8b
f
e
p
e
nt
ga Figure8a
or Figure10c
K 0
pre-Lutetian cl s f m c p b cl s f m c p b
sand sand
Figure 7. Yenice measured stratigraphic section of the Yenice formation.
320