Turkish Journal of Earth Sciences
ACCEPTED MANUSCRIPT
Benthonic Foraminiferal Biostratigraphy of the Upper Cretaceous (Middle Cenomanian−
Coniacian) Sequences of the Bey Dağları Carbonate Platform, Western Taurides,
Turkey
BİLAL SARI1, KEMAL SARI2 & SACİT ÖZER1
1 Dokuz Eylül Üniversitesi, Mühendislik Fakültesi, Jeoloji Mühendisliği
Bölümü, Tınaztepe Yerleşkesi, Buca, TR−35160 İzmir, Türkiye [E-mail: [email protected]]
2 Mersin Üniversitesi, Mühendislik Fakültesi, Jeoloji Mühühendisliği Bölümü, Çiftlikköy Kampusü, TR−33340 Mersin, Türkiye
Please cite this article as: SARI, B., TASLI, K. & ÖZER, S. Benthonic Foraminiferal Biostratigraphy of the Upper Cretaceous (Middle Cenomanian−Coniacian) Sequences of the Bey Dağları Carbonate Platform, Western Taurides, Turkey. Turkish Journal of Earth Sciences [Turkish J. Earth Sci.] (2008) [in press]. This PDF file is an early version of a manucript accepted for publication in Turkish Journal of Earth Sciences. It will be copyedited and typeset before proof production, the it will be published in its final form. Please note that there may be some changes to occur if an error is discovered!
Benthonic foraminiferal biostratigraphy of the Upper Cretaceous (Middle Cenomanian-
Coniacian) sequences of the Bey Dağları carbonate platform, western Taurides, Turkey.
BİLAL SARI¹*, KEMAL TASLI² & SACİT ÖZER¹
¹ Dokuz Eylül Üniversitesi, Mühendislik Fakültesi, Jeoloji Müh. Böl., Tınaztepe Yerleşkesi, TR 35160
Buca-İzmir/TÜRKİYE
² Mersin Üniversitesi, Mühendislik Fakültesi, Jeoloji Müh. Böl. Çiftlikköy Kampusü, TR 33340
Mersin/TÜRKİYE
* corresponding authour, e-mail: [email protected]
Abstract
Identifications of the benthonic foraminiferal assemblages from ten stratigraphic sections
measured from the inner platform limestones of the Middle Cenomanian-Coniacian
successions of the Bey Dağları carbonate platform (BDCP) allowed the recognition of one
biozone and two subzones. The lower part of the platform limestones (Middle-Upper
Cenomanian) is represented by relatively rich benthonic foraminiferal assemblages, while the
upper part (Turonian-Coniacian) contains poor assemblages. The benthonic foraminiferal
assemblages determined in the BDCP are dominated by long-ranging species. The shorter-
ranging, stratigraphically index species have been selected to date the Upper Cretaceous
platform limestones of the BDCP based on the distributions of the species in the circum-
Mediterranean region. P. reicheli-P. dubia Concurrent Range Zone is defined from the
Middle-Upper Cenomanian platform limestones. The biozone includes C. lehneri Subzone
and C. zubairensis Subzone, which correspond to the Middle Cenomanian and Upper
Cenomanian respectively. The first occurrences of M. apenninica-compressa and P.
sphaeroidea indicate the Late Turonian and the Coniacian respectively.
The invasion of the BDCP during the Coniacian by the hemipelagic limestones shows that
the neritic accumulation on the BDCP persisted from the Mid Cenomanian to the Coniacian.
These data indicate that the global sea level rise at Cenomanian-Turonian boundary, which
caused the general demise of many Tethyan carbonate platforms did not result in deepening
on the BDCP.
Key Words: benthonic foraminifera, biostratigraphy, Upper Cretaceous, Bey Dağları
carbonate platform, western Taurides.
Bey Dağları karbonat platformu Üst Kretase (Orta Senomaniyen-Koniasiyen)
istiflerinin bentonik foraminifer biyostratigrafisi, batı Toroslar, Türkiye.
Özet
Bey Dağları karbonat platformunun (BDKP) Orta Senomaniyen-Koniasiyen yaşlı platform içi
karbonatlarından ölçülen on stratigrafik kesitten saptanan bentonik foraminifer toplulukları bir
bentonik foraminifer biyozonu ve iki alt zonun tanımlanmasını sağlamıştır. Platform
karbonatlarının alt bölümü (Orta-Üst Senomaniyen) bağıl olarak zengin bentonik foraminifer
toplulukları ile temsil edilir. Üst bölüm ise (Turoniyen-Koniasiyen) fakir topluluklar ile
simgeseldir. BDKP’de saptanan bentonik foraminifer toplulukları düşey dağılımı geniş
türlerce baskındır. BDKP’nin Üst Kretase kireçtaşlarını yaşlandırmak amacıyla, düşey
dağılımı dar, stratigrafik açıdan karakteristik türler, Akdeniz kuşağındaki stratigrafik
dağılımları esas alınarak seçilmiştir. P. reicheli-P. dubia AşmalıMenzil Zonu platform
kireçtaşlarının Orta-Üst Senomaniyen bölümünde tanımlanmıştır. Biyozon, sırasıya Orta
Senomaniyen ve Üst Senomaniyen’e karşılık gelen C. lehneri Alt Zonu ve C. zubairensis Alt
Zonu’nu içerir. M. apenninica-compressa ve P. sphaeroidea’nın ilk ortaya çıkışları sırasıyla
Geç Turoniyen ve Koniasiyen’i işaret eder.
BDKP’nin Koniasiyen’de yarıpelajik kireçtaşları tarafından örtülmesi, BDKP’de neritik
çökelimin Orta Senomaniyen’den Koniasiyen’e kadar sürdüğünü gösterir. Bu veriler, birçok
Tetis karbonat platformunun sona ermesine neden olan Senomaniyen-Turoniyen sınırındaki
küresel deniz seviyesi yükselmesinin BDKP’de derinleşmeye neden olmadığını gösterir.
Anahtar Sözcükler: bentonik foraminifer, biyostratigrafi, Üst Kretase, Bey Dağları karbonat
platformu, batı Toroslar.
Introduction
Larger benthonic foraminifera are important tools to date the Cretaceous platform carbonates
as the valued pelagic deposit markers such as ammonites and/or planktonic foraminifera are
usually absent or very rare in neritic environments (Arnaud et al. 1981; Schroeder &
Neumann 1985). However, the following points have been discussed in the literature, which
limit the usage of benthonic foraminifera:
- benthonic foraminifera are facies dependent and sensible to the environmental changes
(Gusic et al. 1988; Velic & Vlahovic 1994; Caus et al. 2003),
- many Cretaceous carbonate platforms, which hosted larger benthonic foraminifera, were
sensible to the sea-level changes caused by eustacy and/or tectonic movements and so faced
local and/or widespread emersions and drowning events (Chiocchini et al. 1984).
Hence, the apparent ranges of Late Cretaceous benthonic foraminifera may not correspond
to their true evolutionary stratigraphic ranges (appearance-extinction) and they should be used
for biostratigraphic correlations with great care, even in environments such as long-lasting
carbonate platforms (Gusic et al. 1988; Caus et al. 2003). Although several benthonic
foraminiferal stratigraphic distributions and biozonations have been suggested especially for
local areas, a refined, standard biozonation, which can be applied for the Mediterranean
region, has not been able to be created for the Upper Cretaceous up till now due to the
limitations mentioned above.
Many studies have been carried out on the Bey Dağları Autochthon for nearly four
decades. Although neritic limestones have wide geographic distribution throughout the Bey
Dağları Autochthon, benthonic foraminiferal biostratigraphy of the Upper Cretaceous neritic
limestones have been the subject of only a few detailed studies, including Bignot & Poisson
(1974), Poisson (1977), Farinacci & Yeniay (1986), Sarı (1999), (2006b).
The objective of this paper is to establish detailed benthonic foraminiferal zonation of the
Upper Cretaceous (Middle Cenomanian-Coniacian) neritic limestones of the BDCP and
correlate it with the adjacent carbonate platforms. The study is based on twenty-two
stratigraphic sections, which were measured from the northern part of the Bey Dağları
Autochthon. Ten representative sections are illustrated and described herein (Figure 1).
Geological Setting of the Bey Dağları Carbonate Platform
The Bey Dağları Autochthon, which is approximately 150 km long oriented NE-SW from Kaş
to Isparta (Figure 1) represents a segment of a Mesozoic Tethyan platform on which
carbonate accumulation persisted from the Triassic to the Early Miocene. This segment was
overthrusted by the Antalya nappes in the east and by the Lycian nappes in the northwest, and
is partially exposed in the Göcek window (Özgül 1976; Poisson 1977; Farinacci & Köylüoğlu
1982; Naz et al. 1992; Robertson 1993). During the Mesozoic time, the autochthonous unit
was part of a larger crustal fragment of the African palaeomargin which can be traced in the
Taurides and Zagrides to the east, and the Hellenides, Dinarides and Apennines to the west
(Şengör & Yılmaz 1981; Farinacci & Köylüoğlu 1982; Poisson et al. 1984; Özgül 1984;
Robertson & Dixon 1984; Robertson & Woodcock 1984; Waldron 1984; Farinacci & Yeniay
1986; Robertson et al. 1991; Robertson 1993; Robertson et al. 2003; Poisson et al. 2003).
The BDCP was one of the many Mesozoic Tethyan carbonate platforms initiated as a
result of flooding of blocks, which had rifted from the northern margin of Gondwana during
mid-Late Triassic (following Late Permian-Early Triassic rifting) throughout the southern part
of the Eastern Mediterranean region (Robertson 2002). The BDCP underwent the entire
predictible geodynamic spectrum of the Wilson cycle: rifting, drifting, transtension,
transpression, and collision (Bosellini 1989). The BDCP is reconstructed as an isolated
carbonate platform (Figure 2), which was the southernmost representative of the girdle of
intraoceanic platforms extending from the western Mediterranean to the eastern
Mediterranean Neotethys during the Late Cenomanian (Dercourt et al. 2000).
The Bey Dağları Autochthon was under the effect of different tectonic regimes during the
Late Cretaceous, a time of intense tectonic movements in the eastern Mediterranean region.
Late Cretaceous tectonic activities are thought to be responsible for the drowning of carbonate
platforms, opening of small oceanic basins and collision of different tectonic units. Many
studies have shown that the Upper Cretaceous sequences are characterized by breaks in
deposition and important facies variations in both neritic and pelagic carbonates (Poisson
1977; Gutnic et al. 1979; Farinacci & Köylüoğlu 1982; Farinacci & Yeniay 1986; Özkan &
Köylüoğlu 1988; Naz et al. 1992; Sarı 1999; Sarı & Özer 2001, 2002; Sarı et al. 2004; Sarı
2006a, 2006b).
Materials and Methods
Eight hundred and sixty-one thin sections of the limestone samples were collected from the
twenty-two measured stratigraphic sections and examined in order to establish the
biostratigraphic framework, and to date and detect depositional environments of the neritic
limestones of the BDCP. Ten representative stratigraphic sections were selected to construct
the biostratigraphical framework; other sections are characterized by either relatively poor
benthonic foraminiferal assemblages, or generally similar distributions (Figure 1).
Benthonic foraminiferal biozonation is established based on the first and last occurrence
datums of the taxa in accordance with the rules recommended by the North American
Stratigraphic Code (NASC 1983) and International Stratigraphic Guide (ISG) (Salvador,
1994).
Previous Studies
Upper Cretaceous neritic limestones of the Bey Dağları Autochthon have been subject to a
few studies dealing with the benthonic foraminiferal biostratigraphy. Altınlı (1944) was the
first to mention the presence of Cenomanian benthonic foraminifera in the area between
Burdur and Isparta. Later on Blumenthal (1960-1963) found Actaeonella and Orbitolina in
Pınarbaşı and attributed these levels to Aptian and Cenomanian-Turonian. Colin (1962),
Tolun (1965) and Lefevre (1966) are researchers, who mentioned the Cenomanian limestones
with few benthonic foraminifera.
Poisson (1967) gave first detailed benthonic foraminifera assemblage from the Korkuteli
area. He noted that the assemblage comprising C. gradata, D. schlumbergeri, P. cf. reicheli,
O. cf. ovum and Cuneolina sp., which indicated Late Cenomanian age.
Bignot & Poisson (1974) described a rich benthonic foraminifera assemblage in the
Katran Dağ area. They determined two different horizons, one with P. laurinensis, and the
other one with S. viallii. They noted that the two species were not found together and they
were content to accept that the level with S. viallii laid beneath the level with P. laurinensis
on the basis of the following previous data from the Mediterranean region; P. laurinensis,
associated with C. gradata and C. fraasi, is accepted as an indicator of the Late Cenomanian
in Italy (de Castro 1965, 1966), Croatia (Husinec, 2002), Portugal (Berthou & Philip 1972),
Greece (Guernet 1971; Bignot et al. 1971; Fleury 1972), Lebanon (Saint-Marc 1969, 1970)
and probably in Iran (Sampo 1969). S. viallii was found in the level beneath P. laurinensis
and C. fraasi in Italy (Sartoni & Crescenti 1962; Colalongo 1963; Devoto 1964; Farinacci &
Radoicic 1965; de Castro 1966; Angelucci & Devoto 1966), former Yugoslavia (Radoicic
1960), Greece (Fleury 1972), Lebanon (Saint-Marc 1969, 1970) and Tunisia (Bismuth et al.
1967).
Poisson (1977) noted the presence of the Cenomanian assemblages through the
stratigraphic sections in his detailed thesis.
Farinacci & Yeniay (1986) also found rich benthonic foraminiferal assemblages through
the eight stratigraphic sections scattered throughout the autochthon. They noted that the
assemblages indicated Cenomanian age and were overlain by the Lower Turonian with
abundant rudist fragments, calcisphaerulids and planktonic foraminifera to firstly appear on
the platform.
Recently Sarı (2006b) established the Upper Cretaceous biostratigraphy of the BDCP
based on benthonic foraminifera, planktonic foraminifera and rudists.
Upper Cretaceous Litho-biostratigraphy and Depositional Environment of the BDCP.
The Upper Cretaceous sequence of the northern area of the autochthon is represented by two
formations (Figure 3). The Bey Dağları Formation comprises thick neritic limestones at the
base and thin hemipelagic limestones at the top. Approximately 700-m-thick, Middle
Cenomanian-Coniacian neritic part consists of shallow water platform limestones, that were
deposited in peritidal environments. The neritic limestones are capped by a 26-m-thick
package of Coniacian-Santonian hemipelagic limestones. Thin-to medium-bedded cherty
pelagic limestones of the Late Campanian-Late Maastrichtian Akdağ Formation reach a total
thickness of 100 m and disconformably overlie various stratigraphic levels of the underlying
Bey Dağları Formation. The pelagic marls of the Palaeogene, which locally begin with a
pelagic conglomerates, disconformably overlie the different stratigraphic levels of the Upper
Cretaceous sequence (Figure 3).
Neritic limestones of the Katran Dağ area are represented by the rudist-rich (mainly
caprinids) Mid-Late Cenomanian Yağca Köy Formation, which is disconformably overlain by
pelagic deposits of the Karakirse Formation. The lowermost part of the Karakirse Formation
comprises large pebbles and blocks derived from the underlying rudist-rich limestones of the
Yağca Köy Formation.
Benthonic foraminifera and rudists are the ony fossil components used to date the neritic
limestones of the BDCP. The lower part of the neritic limestones corresponding to Middle-
Upper Cenomanian is relatively rich in benthonic foraminifera. They are rich in number of
individuals but poor in diversity probably due to restricted environment. The upper part,
which corresponds to the Turonian-Coniacian interval, has a poor assemblage.
Two rudist formations have been observed in the neritic limestones. The lower level,
which is observed in the Middle-Upper Cenomanian of the Sarp Dere Section is represented
by scarce and unidentifiable caprinids associated with radiolitids (caprinid lithosome). The
upper level is dominated by hippuritids and found near the top of the platform limestones
(hippuritid lithosome). The fauna is represented by the dominance of V. praegiganteus, which
is accompanied by rare V. inferus, H socialis, H. resecta and radiolitids in the Korkuteli area.
The 87Sr/86Sr values of well preserved low-Mg calcite of the shells of V. praegiganteus show
that the age of this level is Late Turonian (Sarı et al. 2004). The upper rudist level, which
prominently occurs in the Korkuteli area, is observed patchyly throughout the northermost
part of the platform. The occurrence of M. heraki, D. bassani, B. angulosus in the Koparan
Tepe section also supports the Late Turonian age obtained by Sr-isotope analysis.
The faunal change after the Late Turonian (probably in the Coniacian) from
predominantly rudists and benthonic foraminifera to planktonic foraminifera, indicates a
incipient drowning of the platform and subsequent establishment of hemipelagic conditions
on the platform that lasted until the end of the Santonian. The limestones deposited in
hemipelagic conditions are massive, cream-coloured, fractured and contain rare planktonic
foraminifera and abundant calcispheres. The neritic and hemipelagic limestones are both
massive and cream-coloured and similar in appearance (i.e. textures on broken, fresh surface
are the same), hence they are indistinguishable in the field. A special microfacies, containing
abundant crinoids enclosed by syntaxial cement, has been determined between the neritic and
hemipelagic facies in some stratigraphic sections. The crinoid grains enclosed by syntaxial
cement are characteristic features of the drowning phase (Flügel 2004). Besides, there is no
evidence to support an intense karstification before drowning. The maximum thickness of the
hemipelagic levels was measured in the Kocaboğaz Dere section and is 26 m (Sarı 2006b).
Neritic limestones of the Bey Dağları Formation mainly accumulated in a platform
interior environment that existed from Mid Cenomanian to Coniacian. Microfacies analyses
of neritic limestones have indicated peritidal (tidal flat, ponds and channels), subtidal, shelf
(restricted circulation), shelf lagoon (open circulation), winnowed edge, organic build up and
foreslope environments (Sarı & Özer 2001; Sarı 2006b). The planktonic foraminifera-bearing
Coniacian-Santonian massive limestones were deposited in hemipelagic environment (Sarı
2006a; 2006b). The following microfacies have been distinguished belonging to the
mentioned environments. These are the main microfacies and they are transitional and
intercalated: a) Laminated peloidal packstone and fenestral mudstone microfacies, b)
Alternating cryptalgal and laminated peloidal packstone microfacies, c) Sparse benthonic
foraminifera-bearing non-laminated peloidal packstone/grainstone microfacies, b) Rich
benthonic foraminifera-bearing wackestone/packstone microfacies, d) Rudist fragments-
bearing packstone microfacies (Sarı & Özer 2001; Sarı 2006b).
The neritic limestones of the Katran Dağ area (Karain and Yağca sections) are represented
by the Yağca Köy Formation and have different facies characteristics from the other
stratigraphic sections probably as a result of a different palaeogeographic evolution. The
sequence in the Katran Dağ area comprises the Middle Cenomanian caprinid-rich neritic
limestones and is dominated by the winnowed bioclastic rudstone/grainstone microfacies with
rich rudist fragments and rare corals and gastropods. Coarse bioclastic grains are well-
rounded, coated with micrite envelopes and replaced by sparry calcite. The microfacies
indicate the dominance of winnowed platform edge environment, where lime mud is removed
because of constant wave action, at or above wave base (Wilson 1975; Flügel 2004). The
rudstone/grainstone microfacies rarely alternate with the ‘coral framestone’, ‘floatstone with
rudist fragments and intraclasts’ and ‘packstone with benthonic foraminifera and rare
intraclasts’ microfacies (Sarı 2006b).
Measured Stratigraphic Sections
As almost each stratigraphic section represents different biostratigraphic data, biostratigraphic
characteristics of each section will be presented separately from north to south of the area
investigated (See Figure 1 for location of the sections).
1. Koparan Tepe section
The occurrence of C. lehneri in the 36-m-thick lower part of the 230-m-thick succession
suggests the Mid Cenomanian age (Figures 5 & 6). The middle part of the section is mostly
represented by the scarce occurrences of the Cenomanian taxa like P. reicheli, V. radoicicae,
P. dubia, B. peneropliformis, M. cretacea, P. parvus, T. avnimelechi and B. bentori (Figure
5). The occurrence of C. fraasi in sample 03-381 suggests a Late Cenomanian age (Figure 5).
The last occurrence of the Cenomanian assemblage is seen in sample 03-322. The occurrence
of C. zubairensis in sample 03-324 indicate that the age of this level is also Late Cenomanian.
The uppermost part of the section is characterized by the Upper Turonian rudist level
(hippuritid lithosome), which is dominated by V. praegiganteus. The 62-m-thick level
between the last occurrences of the Cenomanian assemblage and the first occurrence of the
rudists may correspond to the Turonian. The benthonic foraminifera in this interval are very
rare and include B. capitata, which is restricted to this interval. N. regularis is found in the
middle part of this interval (sample 03-313). Association of P. reicheli, V. radoicicae and B.
peneropliformis with C. lehneri in the lower part of the section support the data, which
suggest the occurrence of these species in the Mid Cenomanian (Figure 5). P. laurinensis
appears seven metres above the level, where C. fraasi disappears. C. gradata, T. avnimelechi,
N. regularis and B. bentori appear at the uppermost part of the Upper Cenomanian in this
section (samples 03-324-03-322). The absence of bauxitic and lateritic levels, which indicate
subaerial exposure and pelagic interlayers clues of drowning, suggest that the platform
conditions persisted from the Mid Cenomanian to the Late Turonian at least in this part of the
platform.
2. Demirci Dere section
The 7-m-thick neritic limestones beneath the pelagic limestones include C. zubairensis, which
suggest a Late Cenomanian age (Figures 5 & 7). C. gradata in sample 03-475 accompanies C.
zubairensis. The 5.5-m-thick lower part of the neritic limestones, are brecciated and include
rudist shell fragments at the lowermost part of the section. The 1.5-m-thick uppermost part is
made up of thick-bedded limestones. Thin-bedded (10-15 cm) pelagic limestones, including
sand to fine pebble-size intraclasts derived from various stratigraphic levels of neritic,
hemipelagic and pelagic limestones, disconformably rest over the neritic limestones along a
prominent erosional surface. The planktonic foraminifera associations indicate that the age of
the lower part of the pelagic limestones is Late Campanian (Sarı 2006b).
3. Karain section
The section is represented by a rich caprinid, ichthyosarcolitid and radiolitid fauna (caprinid
lithosome), which suggest a Mid-Late Cenomanian age and are associated with corals and
gastropods. However, benthonic foraminifera are rather scarce (Figure 8). The uppermost part
of the 120-m-thick sequence is characterized by the occurrence of Orbitolina sp. in three
samples. The presence of M. cretacea and P. laurinensis within the assemblage determined in
sample 03-634 close to the middle part of the succession indicates that the level where the
sample 03-634 was taken should not be older than the Mid Cenomanian as these species are
not older than the Mid Cenomanian (Figure 5).
The rudist fauna comprising I. bicarinatus, I. triangularis, C. Schiosensis, N. gigantea, S.
cf. Schiosensis, S. woodwardi, Durania sp., Radiolites sp. and Sauvagesia sp. and
unidentifiable radiolitids, was previously studied by Özer (1988) and has also been reported
from Serinhisar (Denizli) by Özer (1998). The fauna has been reported from many Middle-
Upper Cenomanian outcrops in the circum-Mediterranean region as well (Plenicar 1963;
Sliskovic 1968; Polsak & Mamuzic 1969; Bilotte 1985; Accordi et al. 1989; Lupu 1992;
Cherchi et al. 1993).
4. Yağca section
The neritic limestones at the lowermost part of the section are the lateral equivalent of
limestones observed in the Karain section. The limestones have rather scarce foraminifera and
rich rudist assemblage as in the Karain section. A different Cenomanian assemblage is
observed in the pebbles of the Karakirse Formation (Figure 9). The pebbles and blocks of the
neritic limestones are embedded in pelagic matrix with planktonic foraminifera, which
indicate a latest Campanian-Early Maastrichtian age (Sarı 2006b).
5. Canavar Boğazı section
The neritic part of the section is mainly represented by scarce benthonic foraminifera. P.
laurinensis is present in samples 07-627 and 97-630 and is known as a Mid-Late Cenomanian
species (Figure 5 & 10). Occurrence of P. reicheli, P. dubia, B. peneropliformis, N. regularis
and C. gradata in the uppermost part of the neritic limestones indicate that the neritic part of
this section should not be younger than the Late Cenomanian. The uppermost part of the
neritic succession is represented by the occurrence of unidentifiable radiolitid fragments. The
neritic succession is disconformably overlain by pelagic limestones. Planktonic foraminifera
assemblage observed in the pelagic limestones suggest a Late Campanian age (Sarı 2006b).
6. Kargalıköy section
The section is represented by cream-coloured, well-bedded (30-60 cm), indurated neritic
limestones of the Bey Dağları Formation and one of the most important sections as it contains
the remarkable road-cut outcrop of the Upper Turonian rudist level (hippuritid lithosome)
(Figure 11). The lower part of the 20-m-thick lithosome is dominated by V. praegiganteus,
which is associated with rare V. inferus, small-sized hippuritids and radiolitids. Analysis of
geochemically well-preserved low-Mg calcite of shells of V. praegiganteus for 87Sr/86Sr
values yielded a Late Turonian age (Sarı et al., 2004). The abundance of V. praegiganteus as
well as the other rudists decrease towards the upper part of the lithosome, in which small-
sized hippuritids and radiolitids are common. The lower part of the section has a Mid-Late
Cenomanian foraminiferal assemblage. There is no paleontologic data for the level between
the last occurrence of the Cenomanian assemblage and the first occurrence of rudists. The
uppermost part of the neritic succession between the last occurrence of the rudists and the first
occurrence of the ?Coniacian-Santonian planktonic foraminifera is also barren and may
questionably correspond to the latest Turonian or Coniacian. The rare planktonic foraminifera
content of the 10-m-thick hemipelagic level at the uppermost part of the section suggest a ?
Coniacian-Santonian age (Sarı 2006b). The boundary relationship between the neritic and the
hemipelagic limestones in this section is not clear.
7. Boztaş Tepe section
The section includes an assemblage containing P. dubia, P. laurinensis and C. gradata at the
base of the section (Figure 12). This association indicates a Mid-Late Cenomanian age. The
rest of the succession has long-ranging taxa. The first occurrence of M. apenninica-compressa
in sample 97-193 indicates the Coniacian (Figure 5). The uppermost part of the section is
made up of massive neritic limestones, which are cut by an erosional surface and overlain by
pelagic conglomerates. The planktonic foraminifera observed in the matrix of the pelagic
conglomerates and the overlying pelagic limestones indicates Mid Eocene (Sarı 2006b). The
absence of any pelagic interlayer or any sedimentary structures showing subaerial exposure
throughout the 625-m-thick sequence indicates that the platform environment were not
interrupted in this part of the platform.
8. Sarp Dere section
The Sarp Dere section is the only section where the caprinids (rudists) were determined in the
whole Bey Dağları Autochthon outside the Katran Dağ area. The caprinids are observed in the
middle part of the section as few unidentifiable individuals associated with rare radiolitids
(Figure 13). The occurrence of the caprinids indicates Cenomanian. The poor benthonic
foraminifeal assemblage determined in the lowermost part of the section is typical Mid-Late
Cenomanian Bey Dağları assemblage observed in the other stratigraphic sections. The
appearance of P. sphaeroidea in sample 97-9 at the uppermost part of the succession indicates
the Coniacian. The neritic limestones are cut by an erosional surface and overlain by the thin-
bedded pelagic limestones of the Akdağ Formation. Rich planktonic foraminiferal assemblage
suggests a Late Campanian-Early Maastrichtian age (Sarı, 2006a).
9. Küçük Tepe section
The samples at the lower part of the section include Mid-Late Cenomanian assemblages
(Figure 14). The occurrence of P. sphaeroidea in sample 97-68 allows to draw the Turonian-
Coniacian boundary. The uppermost part of the neritic limestones is represented by a rudist
level with abundant radiolitids. The neritic limestones are disconformably overlain by the
pelagic limestones of the Akdağ Formation. The rich planktonic foraminifera assemblages
suggest a Late Campanian-Early Maastrichtian age (Sarı 2006a).
10. Çamkuyusu section
The approximately 400-m-thick lower part of the sequence is almost barren and only sample
04-41 includes a poor assemblage, which is made up of a few species such as C. gradata, N.
picardi and P. reicheli. The lower part of the second half includes a relatively rich
assemblage. The last occurrences of C. gradata and P. reicheli in sample 04-65 draw the
Cenomanian-Turonian boundary. The first occurrence of P. sphaeroidea in sample 04-69
suggests the Coniacian. The approximately 200-m-thick upper part of the section is
represented only by long-ranging taxa. The sequence includes rare non-diagnostic rudists and
non-rudist bivalves throughout.
Benthonic Foraminiferal Biostratigraphy
Detailed investigations of ten measured stratigraphic sections from the BDCP (Figures 6
through 15) show that the lower part of the platform limestones (Middle-Upper Cenomanian)
is represented by relatively rich benthonic foraminiferal assemblages, while the upper part
(Turonian-Coniacian) contains poor assemblages. These data consistent with the other
Mediterranean successions (Figure 5). Numerous studies of the Upper Cretaceous benthonic
foraminiferal biostratigraphy have been carried out in the Mediterranean region since the
beginning of the second half of the last century. The data were compiled by Arnaud et al.
(1981) and Schroeder & Neumann (1985). Bilotte (1998) presented the distributions of
important Tethyan and Adriatic benthonic foraminiferal species. Correlation of the
stratigraphic distribution of the important benthonic foraminiferal species, derived from the
22 published papers, is summarized in Figure 5. The species in this chart are only those that
were also observed in the BDCP. Correlation of the biozonations offered for the Upper
Cretaceous neritic successions is given in Figure 16. The benthonic foraminiferal
biozonations proposed for each area are different due to the limitations mentioned in the
introduction part.
The benthonic foraminiferal assemblages determined in the BDCP successions are
dominated by long-ranging species. The presence of shorter-ranging, stratigraphically index
species, the first (FO) and/or the last occurrence (LO) of the taxa and the co-occurrence of
two or more taxa are all important for finer biostratigraphic subdivision. The benthonic
foraminiferal biozones have been established based on the recommendations of the NASC
(1983) and the ISG (Salvador, 1994).
P. reicheli-P. dubia Concurrent Range Zone has been defined from the Middle-Upper
Cenomanian platform limestones. The biozone includes C. lehneri Subzone and C.
zubairensis Subzone, which correspond to the Middle Cenomanian and Upper Cenomanian
respectively (Figure 17). The biozones identified in this study are briefly described below
from oldest to youngest (See Plates 1 to 4 for the images):
P. reicheli-P. dubia Concurrent Range Zone
This biozone is determined from the FO of P. reicheli and the LO of P. dubia (Figure 17).
P. reicheli and P. dubia are selected as biozone markers, because they are the most common
species observed in the BDCP. The species are also widely recorded from the Cenomanian
shallow-water limestones of the circum-Mediterranean region. The biozone is defined from
the Koparan Tepe section (Figure 7). P. reicheli firstly occurs in sample 03-424. The species
is rare throughout the section and has its last occurrence in sample 03-324. The FO and the
LO of P. dubia are observed in samples 03-417 and 03-322 respectively. The total thickness
of the biozone is 176.5 metres in this section. P. reicheli-P. dubia Concurrent Range Zone
includes many Cenomanian (i.e., P. parvus, T. avnimelechi, V. radoicicae, B. bentori, B.
peneropliformis, N. regularis, P. reicheli and C. gradata) and Mid-Late Cenomanian (i.e., M.
cretacea, P. laurinensis, C. lehneri, C. fraasi and C. zubairensis) species. Long-ranging
species such as D. schlumbergeri, C. pavonia, N. simplex, P. heimi and N. picardi also occur
within this biozone (Figures 6 & 17). The lower and the upper boundaries of the biozone can
not be recognized properly in the other stratigraphic sections due to the rareness of the species
and/or reduced thickness of neritic limestones in some stratigraphic sections. P. reicheli-P.
dubia Concurrent Range Zone includes two subzones:
C. lehneri Subzone: This biozone is defined by the total range of the nominate taxon in the
Koparan Tepe section (Figures 6 & 17). The species has its FO and LO in samples 03-417 and
03-398 respectively and total thickness of the biozone is 35.5 metres in this section (Figure 6).
The biozone includes D. schlumbergeri, P. reicheli, C. pavonia, V. radoicicae, N. conica, N.
simplex, P. dubia, P. heimi and B. peneropliformis (Figures 6 & 17). C. lehneri is recorded
from the Middle Cenomanian successions in the circum-Mediterranean region (Chiocchini et
al. 1984; 1994; Schroeder & Neumann 1985). Hence, the age of the interval corresponding to
this biozone should be Mid Cenomanian in the Koparan Tepe section (Figure 6).
C. zubairensis Subzone: This biozone is defined from the FO to the LO of the nominate taxon
in the Demirci Dere section (Figures 7 & 17). Total thickness of the biozone is 4.5 metres in
this section. The biozone comprises C. pavonia, N. simplex, P. reicheli, C. gradata, M.
cretacea, N. picardi, N. conica and B. peneropliformis in the Demirci Dere section (Figure 7).
C. zubairensis is also observed in sample 03-324 in the Koparan Tepe section. The species is
associated with D. schlumbergeri, P. reicheli, N. conica, N. simplex, P. dubia, B.
peneropliformis, M. cretacea, C. gradata and T. avnimelechi (Figure 6). C. zubairensis is
recorded from the Upper Cenomanian successions of the circum-Mediterranean region (Saint-
Marc 1977; 1981; Chiocchini et al. 1984; 1994). Therefore, the age of this biozone should be
Late Cenomanian in the Demirci Dere section (Figure 7).
The other stratigraphically importat taxa: The FO of the two important species such as M.
apenninica-compressa and P. sphaeroidea is also used to date the post Cenomanian
limestones of the BDCP (Figure 17). The FO of M. apenninica-compressa is accepted within
the Late Turonian (de Castro 1966; Gusic & Jelaska 1990; Chiocchini & Mancinelli 1977;
Chiocchini et al. 1994; Korbar & Husinec 2003). M. apenninica-compressa is determined in
two stratigraphic sections in this study. The FO of the species in sample 97-200 in the Boztaş
Tepe section indicates the Late Turonian (Figure 12). The species is associated with P.
sphaeroidea in sample 97-68 in the Küçük Tepe section (Figure 14).
The FO of P. sphaeroidea is used to draw the Turonian-Coniacian boundary (Bilotte
1984; 1998; Fucek et al. 1990) or the FO of the species is accepted within the Coniacian
(Chiocchini & Mancinelli 1977; Bilotte 1985; Grosheny & Tronchetti 1993; Chiocchini et al.
1994). P. sphaeroidea is observed in four stratigraphic sections and its FO allows to draw the
Turonian-Coniacian boundary (Figures 12-15 & 17)
In addition to the biozones and the ‘index’ species, the LO of some taxa are also useful to
draw the Cenomanian-Turonian boundary in the absence of zone marker species. Many taxa
are accepted as Cenomanian species in the peri Mediterranean region (Figure 5). Some of
these taxa such as B. peneropliformis, C. gradata, P. laurinesis, B. bentori, M. cretacea, N.
regularis and T. avnimelechi have been observed in the Bey Dağları successions and are used
to draw the Cenomanian-Turonian boundary. M. cretacea and P. laurinensis are known as
Mid-Late Cenomanan species (Figure 17).
Conclusions
Detailed investigations of the ten measured stratigraphic sections logged from the inner
platform limestones have yielded new data to construct the Upper Cretaceous (Middle
Cenomanian-Coniacian) benthonic foraminiferal biostratigraphy of the BDCP. These data
have been integrated with the data obtained from rudists and planktonic foraminifera
biostratigraphy and Sr-isotope stratigraphy. The lower part of the platform limestones
(Middle-Upper Cenomanian) is represented by relatively rich benthonic foraminiferal
assemblages, while the upper part (Turonian-Coniacian) contains poor assemblages. These
data consistent with the other Mediterranean successions. The benthonic foraminiferal
assemblages determined in the BDCP are dominated by long-ranging species. The shorter-
ranging, stratigraphically index species have been selected to establish biostratigraphic
framework and to date the Upper Cretaceous platform limestones of the BDCP based on the
distributions of the species in the circum-Mediterranean region.
The benthonic foraminiferal assemblages identified from the neritic limestones have
allowed recognition of one biozone and two subzones. P. reicheli-P. dubia Concurrent Range
Zone is defined from the Middle-Upper Cenomanian part of the succession and includes two
subzones. C. lehneri Subzone and C. zubairensis Subzone are characterized by the range of
the nominate taxa and corresponds to the Middle Cenomanian and Upper Cenomanian
respectively. M. apenninica-compressa and P. sphaeroidea are the stratigraphically important
taxa for the post Cenomanian part of the Bey Dağları successions and they indicate the
beginning of the Upper Turonian and the Coniacian respectively.
All the data mentioned above show that the neritic accummulation on the BDCP persisted
from the Mid Cenomanian to the Coniacian and the subsidence event did not affect the DDCP
before the Coniacian.
Acknowledgements
We thank to Antun Husinec for his invaluable review that improved the manuscript
considerably. İsmail İşintek is thanked for his advice and discussions on benthonic
foraminiferal biozonations. The helps of Akif Sarı, Ümit Kasım, Evren Yücel and Görkem
Oskay are also appreciated who took part in the field works. This work was financially
supported by a TUBITAK project, no. 102Y062, which is also gratefully acknowledged.
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Appendix: List of species mentioned in the text and the figures with author attributions and date
Benthonic Foraminifera Antalyna sp. Belorussiella sp. Biconcava bentori Hamaoui & Saint-Marc, 1970 Biplanata peneropliformis Hamaoui & Saint-Marc, 1970 Bolivinopsis capitata Yakovlev, 1891 Charentia sp. Chrysalidina gradata D’ Orbigny, 1839 Cisalveolina fraasi (Gümbel, 1872) Cisalveolina lehneri Reichel, 1941 Coxites zubairensis Smout, 1956 Cuneolina pavonia D’ Orbigny, 1846 Cuneolina sp. Dicyclina schlumbergeri Munier-Chalmas, 1887 Merlingina cretacea Hamaoui & Saint-Marc, 1970 Moncharmontia apenninica-compressa Nezzazata conica (Smout, 1956) Nezzazata simplex Omara, 1956 Nezzazata sp. Nezzazatinella picardi (Henson, 1948) Nezzazatinella sp. Nummoloculina regularis Philipson, 1887 Orbitolina sp. Peneroplis parvus De Castro, 1965 Peneroplis sp. Pseudocyclammina sphaeroidea Gendrot, 1968 Pseudocyclammina sp. Pseudodomia drorimensis Reiss, Hamaoui & Ecker, 1964 Pseudolituonella reicheli Marie, 1952 Pseudonummoloculina heimi (Bonet, 1956) Pseudonummoloculina sp. Pseudorhapydionina dubia (De Castro, 1965) Pseudorhapydionina laurinensis (De Castro, 1965), Pseudorhapydionina sp. Spiroloculina sp. Textularia sp. Trochospira avnimelechi Hamaoui & Saint-Marc, 1970 Vidalina radoicicae Cherchi & Schroeder, 1985
Rudists Biradiolites angulosus D’Orbigny, 1850 Caprina schiosensis Boehm, 1892 Distefanella bassani Parona, 1901 Durania sp. Hippurites socialis Douvillé, 1890 Hippuritella resecta (Defrance, 1821) Ichthyosarcolites bicarinatus Gemmellaro, 1865 Ichthyosarcolites triangularis Desmarest, 1817 Milovanovicia heraki Polsak, 1967 Neocaprina gigantea Plenicar, 1961 Radiolites sp. Sauvagesia sp. Schiosia cf. schiosensis Boehm, 1892 Sphaerucaprina woodwardi Gemmellaro, 1865 Vaccinites inferus (Douvillé, 1891), Vaccinites praegiganteus (Toucas, 1904)
Figure Captions
Figure 1. I) Main tectonic units of Turkey (after Görür & Tüysüz, 2001), II) Main tectonic
belts of the western Taurides (simplified from Poisson et al., 1984) and the location of
the measured stratigraphic sections a) Upper Miocene-Quaternary post-compressional
tectonic formations, b) Neogene formations preceding the Aksu compressional event, c)
Lower and Middle Miocene of the Bey Dağları Autochthon, d) Bey Dağları Autochthon
(Upper Triassic to Oligocene), e) Antalya nappes, f) Lycian nappes.
Figure 2. Late Cenomanian palaeogeography of the Mediterranean Tethys (Simplified and
modified from Dercourt et al., 2000). The Bey Dağları is restored as an isolated
carbonate platform surrounded by pelagic basins.
Figure 3. Generalized stratigraphic columnar section of the northern part of the Bey Dağları
Autochthon. (See Figure 4 for explanations).
Figure 4. Lithology, fossil and sedimentary structure explanation for all measured
stratigraphic sections.
Figure 5. Correlation of the stratigraphic distributions of the benthonic foraminifera, which
have also been recorded in the Bey Dağları carbonate platform. Data were derived from
the following sources; 1. Fleury (1971) Greece, 2. Berthou (1973) Portugal, 3. Saint-
Marc (1977) Mesogea, 4. Chiocchini & Mancinelli (1977) Italy, 5. Saint-Marc (1981)
Lebanon, 6. Gargouri-Razgallah (1983) Tunisia, 7. Berthou (1984) Portugal, 8. Bilotte
(1984) France & Spain, 9. Chiocchini et al. (1984) Italy, 10. Tronchetti (1984) France,
11. Bilotte (1985) France & Spain, 12. Moullade et al. (1985) Mesogea, 13. Schroeder
& Neumann (1985) Mediterranean region, 14. Cherchi & Schroeder (1985) Italy, 15.
Gusic et al. (1988) Croatia, 16. Fucek et al. (1990) Croatia, 17. Grosheny & Tronchetti,
(1993) France, 18. Velic & Vlahovic (1994) Croatia, 19. Chiocchini et al. (1994) Italy,
20. Bilotte (1998) Tethyan & Adriatic, 21. Chiocchini & Mancinelli (2001) Italy, 22.
Taslı et al. (2006) Turkey (Time scale is adapted from Gradstein et al. 1994).
Figure 6. Stratigraphic distribution of microfossils within the Koparan Tepe section. (See
Figure 4 for explanations and Figure 1 for location of the section).
Figure 7. Stratigraphic distribution of microfossils within the Demirci Dere section. (See
Figure 4 for explanations and Figure 1 for location of the section).
Figure 8. Stratigraphic distribution of microfossils within the Karain section. (See Figure 4 for
explanations and Figure 1 for location of the section).
Figure 9. Stratigraphic distribution of microfossils within the Yağca section. (See Figure 4 for
explanations and Figure 1 for location of the section).
Figure 10. Stratigraphic distribution of microfossils within the Canavar Boğazı section. (See
Figure 4 for explanations and Figure 1 for location of the section).
Figure 11. Stratigraphic distribution of microfossils within the Kargalıköy section. (See
Figure 4 for explanations and Figure 1 for location of the section).
Figure 12. Stratigraphic distribution of microfossils within the Boztaş Tepe section. (See
Figure 4 for explanations and Figure 1 for location of the section).
Figure 13. Stratigraphic distribution of microfossils within the Sarp Dere section. (See Figure
4 for explanations and Figure 1 for location of the section).
Figure 14. Stratigraphic distribution of microfossils within the Küçük Tepe section. (See
Figure 4 for explanations and Figure 1 for location of the section).
Figure 15. Stratigraphic distribution of microfossils within the Çamkuyusu section. (See
Figure 4 for explanations and Figure 1 for location of the section).
Figure 16. Local ranges of the benthonic foraminifera observed in the Upper Cretaceous
carbonate successions of the BDCP.
Figure 17. Chart showing the benthonic foraminiferal biozonations offered for the peri-
Mediterranean Upper Cretaceous platform limestones and correlation of these
biozonations with the Upper Cretaceous benthonic foraminiferal biozonation of the
northern part of the Bey Dağları carbonate platform. (Time scale is adapted from
Gradstein et al. 1994).
Plate Captions
The bar below each photomicrographs is 500 µm.
Plate-1
1- Cisalveolina lehneri; sample 03-416.
2- Cisalveolina lehneri; sample 03-413.
3- Cisalveolina lehneri; sample 03-413.
4- Cisalveolina fraasi; sample 03-381.
5- Cisalveolina fraasi; sample 03-381.
6- Orbitolina sp.; sample 03-660.
7- Vidalina radoicicae; sample 03-418.
8- Vidalina radoicicae; sample 03-416.
9- Bolivinopsis capitata; sample 03-296.
Plate-2
1- Biplanata peneropliformis; sample 03-349.
2- Biplanata peneropliformis; sample 97-633.
3- Merlingina cretacea; sample 03-324.
4- Merlingina cretacea; sample 03-324.
5- Biconcava bentori; sample 97-631.
6- Biconcava bentori; sample 03-322.
7- Nezzazata simplex; sample 03-416.
8- Nezzazata simplex; sample 03-416.
9- Nezzazata simplex; sample 03-478.
10- Nezzazata conica; sample 03-671.
11- Trochospira avnimelechi; sample 03-324.
12- Nezzazatinella picardi; sample 03-310.
13- Nezzazatinella picardi; sample 97-185.
Plate-3
1- Chrysalidina gradata; sample 97-634.
2- Chrysalidina gradata; sample 97-38.
3- Pseudorhapydionina laurinensis; sample 03-378.
4- Pseudorhapydionina laurinensis; sample 97-627.
5- Pseudorhapydionina laurinensis; sample 97-627.
6- Pseudorhapydionina dubia; sample 03-416.
7- Cuneolina pavonia; sample 03-419.
8- Dicyclina schlumbergeri; sample 03-671.
9- Dicyclina schlumbergeri; sample 03-671.
10- Pseudolituonella reicheli; sample 03-478.
Plate-4
1- Coxites zubairensis; sample 03-324.
2- Coxites zubairensis; sample 03-474.
3- Coxites zubairensis; sample 03-479.
4- Moncharmontia apenninica-compressa; sample 97-191.
5- Moncharmontia apenninica-compressa; sample 97-200.
6- Pseudonummoluculina heimi; sample 97-627.
7- Pseudonummoluculina heimi; sample 03-368.
8- Nummoloculina regularis; sample 03-416.
9- Pseudocyclammina sphaeroidea; sample 97-193.
Sarı et al.- Fig. 1
Black Sea
Mediterranean Sea
Aeg
ean
Sea
Sea ofMarmara
100 km
MENDERESMASSIF
BORNOVAFLYSCH
ZONE AFYON ZONE
LYCIAN
NAPPES
İZMİ AR- NKARA SUTU
RE
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MENDERES-TAURUSPLATFORM
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AN
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Stratigraphic Sections
1. Koparan Tepe2. Demirci Dere3. Karain4. Yağca5. Canavar Boğazı6. Kargalıköy7. Boztaş Tepe8. Sarp Dere9. Küçük Tepe10. Çamkuyusu
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Shallow marinecarbonate deposits(platforms)
Deep(er) carbonates,hemipelagic oozes
Deep oceanic basins
Deep marine
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ApuliaAppennine Carbonate Platform
Black SeaCalabriaConstantine PlatformDalmatia
Bey Dağları
Eastern Mediterranean BasinEastern Pontides
Eastern TaurusFriuliGavrovoGolija MassifKarstHezanKırşehirMenderesMunzur
PelagonianPanormidesPindos-OlonosSevan-Akera BasinSanandadjSouth ArmeniaSeydişehirTranscaucasusWestern Pontides
Sar ı
et al.- Fig. 2
FO
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ST
AG
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SU
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SE
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DISCONFORMITY
DISCONFORMITY
Planktonic foraminifera-bearing pelagic marls,locally thin pelagic conglomerates at the base
Thinly to medium bedded, planktonicforaminifera-bearing pelagiclimestones with chert nodules.
Planktonic foraminifera and calcisphere-bearing massive hemipelagic limestones
Massively or thickly-bedded limestones,hippuritid lithosome dominatedby (Toucas, 1904).Vaccinites praegiganteus
Benthonic foraminifera-bearing mediumto thick, locally massive-bedded neriticlimestones and dolomitic limestoneswith stromatolitic lamination.Radiolitids are common.
Scattered caprinid-bearing massiveneritic limestones,caprinid lithosome.
Coniacian
Rich benthonic foraminifera-bearingmedium to thick-bedded neritic limestones
Sarı et al.- Fig. 3
Vaccinites praegiganteus
Small-sized hippuritids
Radiolitids
Distefanella sp.
Benthonic foraminifera
Late CretaceousPlanktonic foraminifera
Stromatolitic lamination
Disconformity surface
Thin-beddedpelagic limestones
Massive hemipelagiclimestones
Medium-to thick-beddedneritic limestones, locallymassive
Caprinid fragments
Intraformational breccia
Stylolite
Pelagic marls
Pelagic mudstones
Pelagic sandstones
Lithified pelagic marls
Pelagic conglomerates
Pelagic limestones with
chert nodules
Pelagic limestones with pebbles
Dolomitized limestones
Brecciated limestones
Non-rudist bivalves
Gastropods
Rudist fragments (general)
Caprinids
Corals
Ichthyosarcolitids
EXPLANATIONS
LITHOLOGYFOSSIL CONTENT AND
SEDIMENTARY STRUCTURES
Hardground
occurrence of the species
probable identificationcf.=
PalaeogenePlanktonic foraminifera
Sarı et al.- Fig. 4
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03-407
03-406
03-405
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03-397
03-396
03-395
03-394
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nen
sis
sp.
sp.
Mil
ioli
dae
sp.
gr.
Upp
er C
enom
ania
nT
uron
ian
BE
YD
AĞ
LA
RI
Lit
holo
gy
Thi
ckne
ss (
m)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
S-1: KOPARAN TEPE continued
Dic
ycli
na s
chlu
mber
ger
iP
seudoli
tuonel
la r
eich
eli
Coxi
tes
zubair
ensi
sC
uneo
lina p
avo
nia
Nez
zaza
ta c
onic
aN
ezza
zata
sim
ple
xP
seudor h
apyd
ionin
a d
ubia
Bip
lanata
pen
eropli
form
isN
ezza
zata
Nez
zaza
tinel
la p
icar d
iP
seudor h
apyd
ionin
a l
auri
nen
sis
Mer
lingin
a c
r eta
cea
Pen
eropli
s parv
us
Pse
udonum
molo
culi
na
Pse
udor h
apyd
ionin
aC
hry
sali
din
a g
radata
Tr o
chosp
ira a
vnim
elec
hi
Num
molo
culi
na r
egula
ris
Bic
onca
va b
ento
riB
oli
vinopsi
s ca
pit
ata
Mil
ioli
dae
sp.
sp.
sp.
Nez
zaza
tida
e
UpperTuronian
116118
120
122
124
126
128
130
132
134
136
138
140
142
144
146
148
150
152
154
156
158160
162164
168
166
170
172
174176
178
180
182184
186
188
190
192
194
196
198
200
202
204
206
208
210
212
214
216
218
220
222
224
226
228
03-366
03-36503-364
03-363
03-36203-36103-36003-35903-35803-35703-35603-35503-35403-35303-35203-35103-35003-34903-34803-34703-34603-34503-34403-34303-34203-341
03-340
03-33903-338
03-33703-33603-33503-33403-33303-332
03-325
03-329
03-318
03-31703-316
03-315
03-314
03-31303-31203-31103-310
03-309
03-308
03-30703-306
03-30503-304
03-32203-32103-32003-319
03-33103-330
03-32803-32703-326
03-32403-323
03-30303-302
03-301Occurrence of the rudist bivalve
(hippuritid lithosome)Vaccinites praegiganteus
Pse
ud
or h
ap
ydio
nin
a d
ub
iaC
un
eoli
na
pa
von
iaN
ezza
zata
sim
ple
xP
seu
do
litu
on
ella
rei
chel
iC
oxi
tes
zub
air
ensi
sC
hry
sali
din
a g
rad
ata
Mer
lin
gin
a c
r eta
cea
Nez
zaza
taN
ezza
zati
nel
la p
ica
r di
Sp
iro
locu
lin
aN
ezza
zata
co
nic
aB
ipla
na
ta p
ener
op
lifo
rmis
sp. sp
.
0
1
2
3
0
1
2
3
4
5
6
7
8
9
10
03-489
03-490
03-49103-49203-493
03-494
03-495
03-472
03-473
03-474
03-475
03-476
03-477
03-478
03-479
03-480
03-48103-482
03-484
03-486
03-483
03-485
03-487
03-488
Lit
holo
gy
Thi
ckne
ss (
m)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
Benthonic foraminiferaS-2: DEMİRCİ DERE
Upp
er C
enom
ania
n
BE
YD
AĞ
LA
RI
AK
DA
Ğ
rew
orke
d
Sarı et al.- Fig. 7
Upp
er C
ampa
nian
03-60403-605
03-609
03-60603-607
03-608
03-61003-61103-61303-61403-61503-61603-61703-618
03-61903-62003-62103-62203-623
03-624
03-626
03-627
03-62803-62903-63003-63103-63203-63303-634
03-63503-636
03-637
03-63803-639
03-640
03-64103-642
03-643
03-64403-645
03-64703-646
03-64803-649
03-650
03-65103-652
03-65303-654
03-65503-65603-657
03-658
03-65903-660
03-661
03-662
03-663
03-664
03-665
03-666
03-667
0
5
10
15
20
25
30
35
40
45
50
55
60
65
70
75
80
85
90
95
100
105
110
115
120
Bic
onca
va b
ento
riC
uneo
lina p
avo
nia
Mer
lingin
a c
r eta
cea
Nez
zaza
ta s
imple
xP
seudor h
apyd
ionin
a d
ubia
Pse
udor h
apyd
ionin
a l
auri
nen
sis
Spir
olo
culi
na
Orb
itoli
na
sp.
sp.
Lit
holo
gy
Thi
ckne
ss (
m)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
S-3: KARAİN
YA
ĞC
AK
ÖY
Mid
d le
- U
pper
Cen
o man
ian
Sarı et al.- Fig. 8
?
Reworkedassociation
Caprinid lithosome
03-668
03-669
03-670
03-67303-671
03-67403-675
03-677
03-676
0
1
2
3
4
5
6
Lit
holo
gy
Thi
ckne
ss (
m)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
Orb
ito
lin
aC
un
eoli
na
pa
von
iaC
hry
sali
din
a g
rad
ata
Dic
ycli
na
sch
lum
ber
ger
iN
ezza
zata
co
nic
aN
ezza
zata
sim
ple
xP
seu
do
do
mia
dr o
rim
ensi
sP
seo
do
litu
on
ella
rei
chel
iP
seu
do
r ha
pyd
ion
ina
du
bia
Sp
iro
locu
lin
asp. sp
.M
ilio
lida
eT
extu
lari
dae
Benthonic foraminiferaS-4: YAĞCA
Mid
dle-
Upp
erC
enom
ania
n
KA
RA
Kİ R
SE
YA
ĞC
AK
ÖY
Upp
er C
ampa
nian
-L
ower
Maa
stri
chti
an
Sarı et al.- Fig. 9
97-625
97-626
97-627
97-628
97-629
97-630
97-631
97-632
97-633
97-634
97-635
97-636
97-637
97-639
97-638
0
2
4
6
8
10
12
14
16
18
20
22
24
26
28
Lit
holo
gy
Thi
ckne
ss(m
)
Sta
ge/S
u bst
age
For
mat
ion
Sam
ple
Num
b er
S-5: CANAVAR BOĞAZI
Cu
neo
lina
pa
von
iaC
ha
r en
tia
Dic
ycli
na
sch
lum
ber
ger
iP
seu
do
nu
mm
olo
culi
na
hei
mi
Pse
ud
or h
ap
ydio
nin
ala
uri
nen
sis
Bic
onca
vab
ento
riN
ezza
zati
nel
lap
icar d
iS
pir
olo
culi
na
Vid
ali
na
rad
oic
icae
Nez
zaza
taco
nic
aN
ezza
zata
sim
ple
xP
seu
do
litu
on
ella
r eic
hel
iP
seu
do
r ha
pyd
ion
ina
du
bia
Bip
lan
ata
pen
ero
pli
form
isN
um
mo
locu
lin
ar e
gu
lari
sC
hry
sali
din
ag
rad
ata
Pen
ero
pli
ssp. sp
.
Mil
ioli
d ae
sp.
Benthonic foraminifera
Mid
dle
- U
pper
Cen
oman
ian
AK
DA
ĞB
EY
DA
ĞL
AR
I
Sarı et al.- Fig. 10
Upp
er C
ampa
nian
Lit
holo
gy
Thi
ckne
ss (
m)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
S-6: KARGALIKÖY
0
5
10
15
20
25
30
35
40
45
50
55
60
65
70
75
80
85
90
95
97-405
97-406
97-407
97-408
97-409
97-410
97-411
97-412
97-413
97-414
97-415
97-416
97-417
97-418
97-419
97-420
97-421
97-423
97-424
97-428
97-429
97-430
97-431
97-432
97-433
97-434
97-435M
iddl
e -
Upp
er C
enom
ania
nU
pper
Tur
onia
n?
Con
iaci
an-
L. S
anto
nian
BE
YD
AĞ
LA
RI
Cuneo
lina p
avo
nia
Dic
ycli
na s
chlu
mber
ger
iM
erli
ngin
a c
r eta
cea
Nez
zaza
tinel
la p
icar d
iP
seudoli
tuonel
la r
eich
eli
Boli
vinopsi
s ca
pit
ata
Pse
udocy
clam
min
aN
ezza
zata
Pen
eropli
sP
seudor h
apyd
ionin
a d
ubia
Pse
udor h
apyd
ionin
a l
auri
nen
sis
sp.
sp.
sp.
Mil
ioli
dae
Sarı et al.- Fig. 11
Abundant occurrence of
Hippuritid lithosome)Vaccinites praegiganteus(
0
25
50
75
100
125
150
175
200
225
250
275
300
325
350
375
400
425
450
475
500
525
550
575
600
625
650
675
Lit
holo
gy
Thi
ckne
ss (
m)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
S-7: BOZTAŞ TEPE
97-263
97-264
97-265
97-266
97-267
97-268
97-21297-21197-210
97-20997-208
97-20797-206
97-205
97-20497-20397-20297-201
97-200
97-199
97-198
97-197
97-196
97-19597-194
97-19397-192
97-19197-190
97-189
97-188
97-187
97-186
97-185
97-184
97-183
97-182
97-181
97-180
97-179
97-178
97-177
97-175
97-17497-17397-17297-16897-16697-16597-164
97-16197-16297-163
Con
iaci
anB
EY
DA
ĞL
AR
I
MiddleEocene
Pse
udor h
apyd
ionin
a d
ubia
Pse
udor h
apyd
ionin
a l
auri
nen
sis
Chry
sali
din
a g
radata
Cuneo
lina p
avo
nia
Nez
zaza
tinel
la p
icar d
iP
seudoli
tuonel
la r
eich
eli
Boli
vinopsi
s ca
pit
ata
Dic
ycli
na s
chlu
mber
ger
iM
onch
arm
onti
a a
pen
nin
ica-c
om
pr e
ssa
Pse
udocy
clam
min
a s
phaer
oid
eaN
ezza
zata
sim
ple
xP
seudonum
molo
culi
na h
eim
i
Cuneo
lina
pavo
nia
Nez
zaza
tinel
la
Pse
udocy
clam
min
a
Mil
ioli
dae
Rot
alid
ae/D
isco
rbid
aesp
. (no
n)
sp.
Ata
xoph
ragm
iida
esp
.
Sarı et al.- Fig. 12
?Tur
onia
nM
idd l
e-U
pper
Cen
o man
ian
Upp
erT
uro n
ian
Sarı et al.- Fig. 13
0
20
40
60
80
100
120
140
160
180
200
220
240
260
280
300
320
340
360
380
400
Lit
holo
gy
Thi
ckne
ss (
m)
Sta
ge/S
ubst
age
For
mat
ion
S-8: SARP DERE
Sam
ple
Num
ber
97-45
97-44
97-43
97-42
97-41
97-40
97-39
97-38
97-37
97-36
97-35
97-34
97-9b
97-9
97-8
97-3397-32
97-3197-2997-2897-26
97-25
97-24
97-23
97-22
97-20
97-19
97-18
97-17
97-16
97-1597-14
97-13
97-1297-11
97-10
97-21
Tur
onia
n -
? C
onia
cian
BE
YD
AĞ
LA
RI
AK
DA
Ğ
Pse
ud
on
um
mo
locu
lin
a h
eim
iB
ico
nca
va b
ento
riP
seu
do
cycl
am
min
aP
seu
do
r ha
pyd
ion
ina
du
bia
Ch
rysa
lid
ina
gra
da
taN
ezza
zati
nel
la p
ica
r di
Pse
ud
oli
tuo
nel
la r
eich
eli
Sp
iro
locu
lin
a
Nez
zaza
taP
seu
do
r ha
pyd
ion
ina
la
uri
nen
sis
Tex
tula
ria
Cu
neo
lin
a p
avo
nia
Bo
livi
no
psi
s ca
pit
ata
Pse
ud
ocy
cla
mm
ina
sp
ha
ero
idea
Bel
oru
ssie
lla
sp.
sp.
Mil
ioli
dae
sp.
sp.
Dis
corb
idae
sp.
Nez
zaza
tida
e
U.C
amp.
-L
.Maa
st.
Mid
dle
- U
pper
Cen
oman
ian
Coniac.
Sarı et al.- Fig. 14
0
20
40
60
80
100
120
140
160
180
200
220
240
260
280
300
320
340
360
Lit
holo
gy
Thi
ckne
ss (
m)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
97-46
97-47
97-48
97-49
97-50
97-51
97-52
97-53
97-54
97-55
97-56
97-57
97-58
97-59
97-60
97-61
97-62
97-63
97-64
97-65
97-66
97-67
97-68
97-69
97-70
97-71
97-72
97-73
97-74
S-9: KÜÇÜK TEPE
97-75
BE
YD
AĞ
LA
RI
Mid
dle
- U
pper
Cen
oman
ian
Chry
sali
din
a g
radata
Nez
zaza
ta c
onic
aN
ezza
zata
sim
ple
xN
ezza
zati
nel
la p
icar d
iP
seudoli
tuonel
la r
eich
eli
Pse
udor h
apyd
ionin
a d
ubia
Spir
olo
culi
na
Tex
tula
ria
Vid
ali
na r
adoic
icae
Cuneo
lina p
avo
nia
Pse
udor h
apyd
ionin
a l
auri
nen
sis
Pse
udonum
molo
culi
na
Pse
udonum
molo
culi
na h
eim
iM
onch
arm
onti
a a
pen
nin
ica-c
om
pr e
ssa
Pse
udocy
clam
min
a s
phaer
oid
ea
sp.
sp.
sp.
Con
iaci
anL.Maast.-U.Camp.
?T
uron
ian
AK
DA
Ğ
0
20
40
60
80
100
120
140
160
180
200
220
240
260
280
300
320
340
360
380
Lit
holo
gy
Thi
ckne
ss (
m)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
S-10: ÇAMKUYUSU
04-3304-35
04-36
04-37
04-38
04-39
04-40
04-41
04-4204-43
04-44
04-45
04-46
04-47
04-48
04-49
04-50
04-51
380
400
420
440
460
480
500
520
540
560
580
600
620
640
660
680
700
720
740
Lit
holo
gy
Thi
ckne
ss (
m)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
S-10: ÇAMKUYUSU continued
04-52
04-53
04-54
04-55
04-56
04-57
04-58
04-60
04-61
04-6204-63
04-64
04-65
04-67
04-68
04-69
04-70
04-71
04-72
04-73
04-74
04-75
04-76
04-77
04-78
04-79
04-80
04-81
04-82
04-84
04-85
04-86
04-83
BE
YD
AĞ
LA
RI
Con
iaci
an
BE
YD
AĞ
LA
RI
Chry
sali
din
a g
radata
Nez
zaza
tinel
la p
icar d
iP
seudoli
tuonel
la r
eich
eli
Mil
ioli
dae
Ch
rysa
lid
ina
gra
da
taN
ezza
zati
nel
la p
ica
r di
Pse
ud
oli
tuo
nel
la r
eich
eli
Pse
ud
or h
ap
ydio
nin
aC
un
eoli
na
pa
von
iaP
seu
do
r ha
pyd
ion
ina
du
bia
Sp
iro
locu
lin
aN
ezza
zati
nel
laP
seu
do
r ha
pyd
ion
ina
la
uri
nen
sis
Tr o
cho
spir
a a
vnim
elec
hi
Tex
tula
ria
Pse
ud
ocy
cla
mm
ina
sp
ha
ero
idea
Pse
ud
on
um
mo
locu
lin
a h
eim
iD
icyc
lin
a s
chlu
mb
erg
eri
Nez
zaza
ta s
imp
lex
Mil
ioli
dae
sp.
sp. sp.
sp.
? M
iddl
e -
Upp
er C
enom
ania
n
?
? M
iddl
e -
Upp
er C
enom
ania
n?T
uron
ian
Sarı et al.- Fig. 15
Cen
oman
ian
Tur
onia
nC
onia
cian
San
toni
an
Camp.
ST
AG
ES
INF
OR
MA
LS
UB
ST
AG
ES
Alb.
Low.
Mid.
Up.
Mid.
Mid.
Mid.
Up.
Up.
Up.
Low.
Low.
Low.
Low.
Up.
Fleury (1980)Greece
Altıner &Decrouez
(1982)SouthernTurkey
Gargouri-Razgallah (1983)Central Tunisia
Bilotte (1985)Spain-France
Chiocchini &Mancinelli (1977),Chiocchini et al.
(1984)(Italy)
Moullade et al.(1985)
Mesogea
Velic & Vlahovic(1994)
Croatia
Taslı et al. (2006)Southern Turkey
This StudySouthwestern Turkey
(Bey Dağları Carbonate Platform)Northern Part
Saint-Marc(1981)
Lebanon
CsB
1C
sB2
CsB
3C
sB4
Sel
lialv
eoli
na
viall
iigr
.bi
ozon
eB
r oec
kin
a b
alc
an
ica
bioz
one
Pse
ud
ocy
cla
mm
ina
sp
ha
ero
idea
bioz
one
Murgellalata
biozone
?
C4-
1C
4-2
C4-3a
C4-3b
C5-
1C
5-2
Pse
ud
od
om
ia v
iall
ii
P.laurinensis
Cisalveolinafallax
Hippurites
Nu
mm
olo
culi
na
reg
ula
ris
Mer
lin
gin
aP
seu
do
r ha
pyd
ion
ina
Pseudodomiaviallii
Undifferentiated
Nummofallotia apulaPseudorhapydioninaNummoloculine
Ostracodaand
Miliolidae
P. dubiaP. laurinensis
and
C. gradata
P. reicheliand
Simplalveolinasimplex
P. cretaceaO. (C.) conica
Praealveolinacretacea
Orb
ito
lin
a (
Co
nic
orb
ito
lin
a)
con
ica
CE
N-1
CE
N-2
C3a
C-4
CE
N-5
O. maccagnoaeS. viallii
O. maccagnoaeC. gradata
C. gradata + Orb.C. gradata - Orb.
C. gradataB. P. balcanica( )
C. gradataB. P. balcanicaV. radoicicae
( )
C3b
Pse
ud
or h
ap
ydio
nin
ad
ub
iaB
ico
nca
va b
ento
rice
nozo
ne
Ost
raco
da a
nd M
ilio
lida
e
Inte
rval
Zon
e
Mo
nch
arm
on
tia
co
mp
r ess
a
Dic
ycli
na
sch
lum
ber
ger
i
ceno
zone
Calcispherulidae &Globotruncanidae
Foraminiferalbiozones
Stratigraphiccolumn
Med
ium
to
thic
k-be
dded
sha
llow
wat
er(i
nner
pla
tfor
m)
lim
esto
nes
Pla
nkto
nic
fora
min
ifer
a-be
arin
gm
assi
ve h
emip
elag
ic l
imes
tone
s
Disconformity
NOT TO SCALE
Dicarinellaconcavata
interval zone(part)
Dicarinellaasymetricarange zone
Abundant occurrence of the rudistbivalve(Toucas).
Vaccinites praegiganteus
Analysis of geochemically well-preservedlow-Mg calcite of shells of the species
Pelagiclimestones
Radotruncanacalcaratarange zone
Valvulamminapicardi
Nummoloculinaheimi
and
Accordiellaconica
Rotorbinellascarsellai
and
Chiocchini et al.(1994),
Chiocchini &Mancinelli (2001),
(Italy)
Accordiellaconica
Rotorbinellascarsellai
and
Nezzazatinellaaegyptiaca
Nummoloculinairregularis
cf.and
cf.
C. gradata
P. reicheliand
P. dubiaP. laurinensis
and
Ostracodaand
Miliolidae
Caprinid lithosome (Mid-Late Cenomanian)
Sar ı
et al.- Fig. 16
P.r
eich
eli-
P.d
ubia
Con
curr
ent
Ran
geZ
one
C. zubairensisSubzone
C. lehneriSubzone
M. apen
nin
ica-
com
pr e
ssa
P. sp
haer
oid
ea
?
Sarı et al.- Fig. 17
D. sc
hlu
mber
ger
iC
. pavo
nia
N. si
mple
xP. hei
mi
P. dubia
P. r e
ichel
iN
. co
nic
aV. ra
doic
icae
C. le
hner
iB
. pen
eropli
form
isN
. pic
ar d
iC
. gra
data
C. fr
aasi
P. la
uri
nen
sis
B. ben
tori
M. cr
etace
aP. parv
us
N. r e
gula
ris
B. ca
pit
ata
C. zu
bair
ensi
sT. avn
imel
echi
M. apen
nin
ica-c
om
pr e
ssa
ST
AG
E
SU
BS
TA
GE
SU
BZ
ON
ES
Cen
oman
ian
Tur
onia
n Upp
erT
uron
ian
C.
zub
air
ensi
sS
ubzo
neC
. le
hn
eri
Sub
zone
BIOZONES
P.
r eic
hel
iP.
du
bia
-C
oncu
rren
t R
ange
Zon
e
Mid
dle
Cen
oman
ian
?
Mid
dle
to U
pper
Cen
oman
ian
Upp
erC
enom
ania
n
Con
iaci
an
PLATE-1
1
5
3
4
2
6
7 8 9
Sarı et al.- Pl. 1
PLATE-2
1 23 4
5 6 7
8
9
10
11
12 13
Sarı et al.- Pl. 2
PLATE-3
1 2 3
4 5
6
7 8 9 10
Sarı et al.- Pl. 3
PLATE-4
1
2
34
5
6
7
8
9
Sarı et al.- Pl. 4