Benthonic foraminiferal biostratigraphy of the Upper Cretaceous

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 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 11. Stratigraphic distribution of microfossils within the Kargalıköy section. (See


Figure 12. Stratigraphic distribution of microfossils within the Boztaş Tepe section. (See


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 15. Stratigraphic distribution of microfossils within the Çamkuyusu section. (See


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.



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.



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.



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.



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

TAVŞANLI ZONE

SULTA

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BEY

DA

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AN

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BOZKIR UNITALA

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INTRA-PONTIDE SUTURE

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RA

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MENDERES-TAURUSPLATFORM

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9

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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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PelagonianPanormidesPindos-OlonosSevan-Akera BasinSanandadjSouth ArmeniaSeydişehirTranscaucasusWestern Pontides

Sar ı

et al.- Fig. 2

FO

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AG

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SU

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TH

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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


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


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03-406

03-405

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03-396

03-395

03-394

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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


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


?

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


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


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


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

.


?Tur

onia

nM

idd l

e-U

pper

Cen

o man

ian

Upp

erT

uro n

ian


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.


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


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

?


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

Documents

Benthonic foraminiferal biostratigraphy of the Upper Cretaceous