Benthonic Foraminiferal Biostratigraphy of the UpperCretaceous (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 Mühendisliği Bölümü,Tınaztepe Yerleşkesi, Buca, TR−35160 İzmir, Türkiye

(E-mail: bilal.sari@deu.edu.tr)2 Mersin Üniversitesi, Mühendislik Fakültesi, Jeoloji Mühendisliği Bölümü, Çiftlikköy Kampusü,

TR− 33340 Mersin, Türkiye

Received 20 December 2006; revised typescript received 07 May 2008; accepted 23 July 2008

Abstract: Identification of the benthonic foraminiferal assemblages from ten stratigraphic sections from the innerplatform 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−UpperCenomanian) is represented by relatively rich benthonic foraminiferal assemblages, while the upper part(Turonian−Coniacian) contains poor assemblages. The benthonic foraminiferal assemblages determined in the BDCPare dominated by long-ranging species. The shorter-ranging, stratigraphical index species have been selected to datethe Upper Cretaceous platform limestones of the BDCP based on the distributions of the species in the circum-Mediterranean region. The Pseudolituonella reicheli-Pseudorhapydionina dubia Concurrent Range Zone is defined fromthe Middle−Upper Cenomanian platform limestones. The biozone includes the Cisalveolina lehneri Subzone and theCoxites zubairensis Subzone of Middle Cenomanian and Upper Cenomanian age respectively. The first occurrences ofMoncharmontia apenninica-compressa and Pseudocyclammina sphaeroidea indicate the Late Turonian and theConiacian respectively.The spread of hemipelagic limestones in the BDCP during the Coniacian shows that neritic accumulation on the BDCPpersisted from the Middle Cenomanian to the Coniacian. These data indicate that the global sea level rise at theCenomanian−Turonian boundary, which caused the general demise of many Tethyan carbonate platforms, did notresult in deepening on the BDCP.

Key Words: benthonic foraminifera, biostratigraphy, Upper Cretaceous, Bey Dağları carbonate platform, westernTaurides

Bey Dağları Karbonat Platformu Üst Kretase (Orta Senomaniyen−Koniasiyen)İstiflerinin Bentonik Foraminifer Biyostratigrafisi, Batı Toroslar, Türkiye

Özet: Bey Dağları karbonat platformunun (BDKP) Orta Senomaniyen−Koniasiyen yaşlı platform içi karbonatlarındanölçülen on stratigrafik kesitten saptanan bentonik foraminifer toplulukları bir bentonik foraminifer biyozonu ve iki altzonun tanımlanmasını sağlamıştır. Platform karbonatlarının alt bölümü (Orta−Üst Senomaniyen) bağıl olarak zenginbentonik foraminifer toplulukları ile temsil edilir. Üst bölüm ise (Turoniyen−Koniasiyen) fakir topluluklar ilesimgeseldir. BDKP’de saptanan bentonik foraminifer toplulukları düşey dağılımı geniş türlerce baskındır. BDKP’nin ÜstKretase kireçtaşlarını yaşlandırmak amacıyla, düşey dağılımı dar, stratigrafik açıdan karakteristik türler, Akdenizkuşağındaki stratigrafik dağılımları esas alınarak seçilmiştir. Pseudolituonella reicheli-Pseudorhapydionina dubia AşmalıMenzil Zonu platform kireçtaşlarının Orta−Üst Senomaniyen bölümünde tanımlanmıştır. Biyozon, sırasıya OrtaSenomaniyen ve Üst Senomaniyen’e karşılık gelen Cisalveolina lehneri Alt Zonu ve Coxites zubairensis Alt Zonu’nuiçerir. Moncharmontia apenninica-compressa ve Pseudocyclammina sphaeroidea’nın ilk ortaya çıkışları sırasıyla GeçTuroniyen ve Koniasiyen’i işaret eder.

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Turkish Journal of Earth Sciences (Turkish J. Earth Sci.), Vol. 18, 2009, pp. 393–425. Copyright ©TÜBİTAKdoi:10.3906/yer-0612-5 First published online 10 September 2008

IntroductionLarger benthonic foraminifera are important tools indating the Cretaceous platform carbonates, asimportant pelagic deposit markers such asammonites and/or planktonic foraminifera areusually absent or very rare in neritic environments(Arnaud et al. 1981; Schroeder & Neumann 1985).However, many factors limit the stratigraphic usageof benthonic foraminifera including: (i) benthonicforaminifera are facies dependent and sensitive toenvironmental changes (e.g., Hallock 1982; Murray1991), (ii) many Cretaceous carbonate platforms thathosted larger benthonic foraminifera were sensitiveto sea-level changes caused by eustacy and/ortectonic movements and so faced local and/orwidespread emergence and drowning events(Chiocchini et al. 1984).

Hence, the apparent ranges of Late Cretaceousbenthonic foraminifera may not correspond to theirtrue evolutionary stratigraphic ranges (firstappearance-last appearance) and they should beused for biostratigraphic correlations with great care,even in environments such as long-lasting carbonateplatforms (Gusic et al. 1988; Caus et al. 2003).Although several local Late Cretaceous benthonicforaminiferal biozonations have been proposed, arefined, standard biozonation applicable across theentire Mediterranean region is still lacking.

Over nearly four decades many studies have beencarried out on the Bey Dağları Autochthon.Although neritic limestones are widely distributedthroughout the Bey Dağları Autochthon, benthonicforaminiferal biostratigraphy of the UpperCretaceous neritic limestones has been the subject ofonly a few detailed studies, including Bignot &Poisson (1974), Poisson (1977), Farinacci & Yeniay(1986), Sarı (1999, 2006b).

The objective of this paper is to establish adetailed benthonic foraminiferal zonation of the

Upper Cretaceous (Middle Cenomanian−Coniacian) neritic limestones of the BDCP and tocorrelate it with adjacent carbonate platforms. Thestudy is based on twenty-two stratigraphic sectionsmeasured from the northern part of the Bey DağlarıAutochthon. Ten representative sections areillustrated and described herein (Figure 1).

Geological Setting of the Bey Dağları CarbonatePlatform (BDCP)The Bey Dağları autochthon extends NE−SW forapproximately 150 km from Kaş to Isparta (Figure1), and represents a segment of the Mesozoic Tethyanplatform on which carbonate accumulation persistedfrom the Triassic to the Early Miocene. This segmentwas overthrust by the Antalya nappes in the east andby the Lycian nappes in the northwest, and ispartially exposed in the Göcek window (Özgül 1976;Poisson 1977; Farinacci & Köylüoğlu 1982; Naz et al.1992; Robertson 1993). Numerous authors (e.g.,Şengör & Yılmaz 1981; Farinacci & Köylüoğlu 1982;Poisson et al. 1984; Robertson & Dixon 1984;Robertson & Woodcock 1984; Waldron 1984;Farinacci & Yeniay 1986; Robertson et al. 1991, 2003;Robertson 1993; Poisson et al. 2003) have shown thatduring the Mesozoic, the autochthonous unit waspart of a larger crustal fragment of the Africanpalaeomargin which can be traced from the Tauridesand Zagrides in the east, to the Hellenides, Dinaridesand Apennines in the west (e.g., Dercourt et al. 1993;Stampfli & Mosar 1999; Robertson 2002).

The BDCP was one of many Mesozoic Tethyancarbonate platforms initiated when blocks that hadrifted from the northern margin of Gondwanaduring the mid-Late Triassic (following LatePermian−Early Triassic rifting) and now distributedthroughout the southern part of the EasternMediterranean region, were immersed (Robertson2002). The BDCP underwent the entire predictable

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BDKP’nin Koniasiyen’de yarıpelajik kireçtaşları tarafından örtülmesi, BDKP’de neritik çökelimin OrtaSenomaniyen’den Koniasiyen’e kadar sürdüğünü gösterir. Bu veriler, birçok Tetis karbonat platformunun sona ermesineneden olan Senomaniyen-Turoniyen sınırındaki küresel deniz seviyesi yükselmesinin BDKP’de derinleşmeye nedenolmadığını gösterir.

Anahtar Sözcükler: bentonik foraminifer, biyostratigrafi, Üst Kretase, Bey Dağları karbonat platformu, batı Toroslar

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Figure 1. (A) Main tectonic units of Turkey (after Görür & Tüysüz 2001), (B) main tectonic beltsof the western Taurides (simplified from Poisson et al. 1984) and locations of measuredstratigraphic sections. Key to symbols: a− Upper Miocene−Quaternary post-compressional tectonic formations, b− Neogene formations preceding the Aksucompressional event, c− Lower and Middle Miocene of the Bey Dağları Autochthon, d−Bey Dağları Autochthon (Upper Triassic to Oligocene), e− Antalya nappes, f− Lyciannappes.

geodynamic spectrum of the Wilson cycle: rifting,drifting, transtension, transpression, and collision(Bosellini 1989), and is reconstructed here as anisolated carbonate platform (Figure 2) that was thesouthernmost representative of the girdle ofintraoceanic platforms extending from the westernMediterranean to the eastern MediterraneanNeotethys during the Late Cenomanian (Dercourt etal. 2000).

The Bey Dağları autochthon was subjected todifferent tectonic regimes during the LateCretaceous, a time of intense tectonic movements inthe eastern Mediterranean region. The LateCretaceous tectonic activities were probablyresponsible for submerging the carbonate platforms,opening small oceanic basins and the collision ofdifferent tectonic units. Many studies have shownthat the Upper Cretaceous sequences arecharacterized by breaks in deposition and importantfacies variations in both neritic and pelagiccarbonates (Poisson 1977; Gutnic et al. 1979;Farinacci & Köylüoğlu 1982; Farinacci & Yeniay1986; Özkan & Köylüoğlu 1988; Naz et al. 1992; Sarı1999, 2006a,b; Sarı & Özer 2001, 2002; Sarı et al.2004).

Materials and MethodsEight hundred and sixty-one thin sections of thelimestone samples were collected from the twenty-two measured stratigraphic sections and examinedin order to establish the biostratigraphic framework,and to date and detect the depositional environmentsof the BDCP neritic limestones. Ten representativestratigraphic sections were selected to construct thebiostratigraphical framework; other sections werecharacterized by either relatively poor benthonicforaminiferal assemblages, or generally similardistributions (Figure 1).

Benthonic foraminiferal biozonation isestablished based on the first and last occurrencedatums of the taxa in accordance with the rulesrecommended by the North American StratigraphicCode (North American Commission onStratigraphic Nomenclature) (NASC 1983) and theInternational Stratigraphic Guide (ISG) (Salvador1994).

Previous Studies Several studies have dealt with the benthonicforaminiferal biostratigraphy of the UpperCretaceous neritic limestones of the Bey Dağlarıautochthon. Altınlı (1944) was the first to record thepresence of Cenomanian benthonic foraminifera inthe area between Burdur and Isparta. Subsequently,Blumenthal (1960-1963) found Actaeonella andOrbitolina in Pınarbaşı and assigned these levels tothe Aptian and Cenomanian−Turonian. Colin(1962), Tolun (1965) and Lefevre (1966) describedthe Cenomanian limestones with few benthonicforaminifera.

Poisson (1967) was the first author to describe adetailed benthonic foraminifera assemblage from theKorkuteli area, noting that the assemblagecomprising C. gradata, D. schlumbergeri, P. cf.reicheli, O. cf. ovum and Cuneolina sp. indicated aLate Cenomanian age.

Bignot & Poisson (1974) described a richbenthonic foraminifera assemblage in the KatranDağ area. They identified two different horizons, onewith P. laurinensis, and the other one with S. viallii.They noted that the two species were not foundtogether and they were content to accept that thelevel with S. viallii underlay the level with P.laurinensis on the basis of previous data from theMediterranean region, namely that P. laurinensis,associated with C. gradata and C. fraasi, is acceptedas an indicator of the Late Cenomanian in Italy (DeCastro 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 (Sampo1969). Sellialveolina viallii was found to appearbefore the first occurrences of P. laurinensis and C.fraasi in Italy (Sartoni & Crescenti 1962; Colalongo1963; Devoto 1964; Farinacci & Radoicic 1965; deCastro 1966; Angelucci & Devoto 1966), Croatia(Radoicic 1960), Greece (Fleury 1972), Lebanon(Saint-Marc 1969, 1970) and Tunisia (Bismuth et al.1967).

Poisson (1977) noted the presence of theCenomanian assemblages through the stratigraphicsections in his detailed thesis.

Farinacci & Yeniay (1986) also found richbenthonic foraminiferal assemblages through the

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eight stratigraphic sections scattered throughout theautochthon. They noted that the assemblagesindicated Cenomanian age and were overlain by theLower Turonian with abundant rudist fragments,calcisphaerulids and planktonic foraminifera.

Recently Sarı (2006b) established the UpperCretaceous biostratigraphy of the BDCP based onbenthonic foraminifera, planktonic foraminifera andrudists.

Upper Cretaceous Litho-biostratigraphy andDepositional Environment of the BDCP The Upper Cretaceous sequence of the northern areaof the autochthon is represented by two formations(Figure 3). The Bey Dağları Formation comprisesthick neritic limestones at the base and thinhemipelagic limestones at the top. Approximately700-m-thick, the Middle Cenomanian−Coniacianneritic part consists of shallow-water platformlimestones, that were deposited in peritidalenvironments. The neritic limestones are capped bya 26-m-thick succession of Coniacian−Santonianhemipelagic limestones. Thin- to medium-beddedcherty pelagic limestones of the LateCampanian−Late Maastrichtian Akdağ Formationreach a total thickness of 100 m, and disconformablyoverlie various stratigraphic levels of the underlyingBey Dağları Formation. The pelagic marls of thePalaeogene locally begin with conglomerate bases,and disconformably overlie the differentstratigraphic levels of the Upper Cretaceoussequence (Figure 3).

Neritic limestones of the Katran Dağ area arerepresented by the rudist-rich (mainly caprinids)Middle to Late Cenomanian Yağca Köy Formation,which is disconformably overlain by pelagic depositsof the Karakirse Formation. The lowest part of theKarakirse Formation comprises large pebbles andblocks derived from the underlying rudist-richlimestones of the Yağca Köy Formation.

Benthonic foraminifera and rudists are the onlyfossil components used to date the neritic limestonesof the BDCP. The lower part of the neriticMiddle−Upper Cenomanian limestones is relativelyrich in benthonic foraminifera. They are abundant,but characterized by poor generic diversity probably

due to restricted environment. The upper part,which corresponds to the Turonian–Coniacianinterval, has a poor assemblage.

Two rudist formations were observed in theneritic limestones. The lower level, in theMiddle−Upper Cenomanian of the Sarp DereSection, is represented by scarce and unidentifiablecaprinids associated with radiolitids (caprinidlithosome). The upper level is dominated byhippuritids and found near the top of the platformlimestones (hippuritid lithosome). The fauna isrepresented by the dominance of V. praegiganteus,which is accompanied by rare V. inferus, H socialis,H. resecta and radiolitids in the Korkuteli area. The87Sr/86Sr values of well preserved low-Mg calcite ofthe shells of V. praegiganteus show that the age of thislevel is Late Turonian (Sarı et al. 2004). The upperrudist level, which prominently occurs in theKorkuteli area, is observed patchily throughout thenorthernmost part of the platform. The occurrenceof M. heraki, D. bassani, B. angulosus in the KoparanTepe section also supports the Late Turonian ageobtained by Sr-isotope analysis.

The post-Late Turonian faunal change (probablyin the Coniacian) from predominantly rudists andbenthonic foraminifera to planktonic foraminifera,indicates an incipient drowning of the platform andsubsequent establishment of hemipelagic conditionson the platform that lasted until the end of theSantonian. The limestones deposited in hemipelagicconditions are massive, cream-coloured, fracturedand contain rare planktonic foraminifera andabundant calcispheres. Both the neritic andhemipelagic limestones are massive and cream-coloured and similar in appearance (i.e. textures onbroken, fresh surface are the same), hence they arehard to differentiate in the field. A specialmicrofacies, containing abundant crinoids enclosedby syntaxial cement, has been observed between theneritic and hemipelagic facies in some stratigraphicsections. The crinoid grains enclosed by syntaxialcement are characteristic features of the drowningphase (Flügel 2004). Besides, there is no evidence tosupport an intense karstification before inundation.The maximum thickness of the hemipelagic levelswas measured in the Kocaboğaz Dere section and is26 m (Sarı 2006b).

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Figure 3. Generalized stratigraphic column of the northern part of the Bey Dağları Autochthon. (see Figure 4 forexplanations).

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EXPLANATIONS

LITHOLOGY FOSSIL CONTENTANDSEDIMENTARY STRUCTURES

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Figure 4. Lithology, fossil and sedimentary structure explanation for all measured stratigraphic sections.

Neritic limestones of the Bey Dağları Formationmainly accumulated in a platform interiorenvironment that existed from Middle Cenomanianto Coniacian. Microfacies analyses of neriticlimestones have indicated peritidal (tidal flat, pondsand channels), subtidal, shelf (restricted circulation),shelf lagoon (open circulation), winnowed edge,organic build up and foreslope environments (Sarı &Özer 2001; Sarı 2006b). These are represented byseveral major facies, including (a) laminated peloidalpackstone and fenestral mudstone microfacies, (b)alternating cryptalgal and laminated peloidalpackstone microfacies, (c) sparse benthonicforaminifera-bearing non-laminated peloidalpackstone/grainstone microfacies, (d) rich benthonicforaminifera-bearing wackestone/packstonemicrofacies, (e) Rudist fragments-bearing packstonemicrofacies (Sarı & Özer 2001; Sarı 2006b). Theplanktonic foraminifera-bearing Coniacian−Santonian massive limestones were deposited inhemipelagic environments (Sarı 2006a,b).

The neritic limestones of the Katran Dağ area(Karain and Yağca sections) are represented by theYağca Köy Formation and have different faciescharacteristics from the other stratigraphic sectionsprobably as a result of a different palaeogeographicevolution. The sequence in the Katran Dağ areacomprises Middle Cenomanian caprinid-rich neriticlimestones and is dominated by the winnowedbioclastic rudstone/grainstone microfacies with richrudist fragments and rare corals and gastropods.Coarse bioclastic grains are well-rounded, coatedwith micrite envelopes and replaced by sparrycalcite. The microfacies indicates the dominance ofthe winnowed platform edge environment, wherelime mud is removed because of constant waveaction, at or above wave base (Wilson 1975; Flügel2004). The rudstone/grainstone microfaciesoccasionally alternate with the ‘coral framestone’,‘floatstone with rudist fragments and intraclasts’ and‘packstone with benthonic foraminifera and rareintraclasts’ microfacies (Sarı 2006b).

Measured Stratigraphic SectionsAs almost each stratigraphic section representsdifferent biostratigraphic data, biostratigraphic

characteristics of each section will be presentedseparately from north to south of the areainvestigated (see Figure 1 for location of thesections).

Koparan Tepe SectionThe occurrence of C. lehneri in the 36-m-thick lowerpart of the 230-m-thick succession suggests a MiddleCenomanian age (Figures 5 & 6). The middle part ofthe section is mostly represented by scarceoccurrences of the Cenomanian taxa P. reicheli, V.radoicicae, P. dubia, B. peneropliformis, M. cretacea, P.parvus, T. avnimelechi and B. bentori (Figure 6). Theoccurrence of C. fraasi in sample no. 03-381 suggestsa Late Cenomanian age (Figure 6). The lastoccurrence of the Cenomanian assemblage is seen insample no. 03-322. The occurrence of C. zubairensisin sample no. 03-324 indicates that the age of thislevel is also Late Cenomanian. The uppermost partof the section is characterized by the Upper Turonianrudist level (hippuritid lithosome) dominated by V.praegiganteus. The 62-m-thick interval between thelast occurrences of the Cenomanian assemblage andthe first occurrence of the rudists may correspond tothe Turonian. The benthonic foraminifera in thisinterval are very rare and include B. capitata, whichis restricted to this interval. Nummoloculina regularisis found in the middle part of this interval (sampleno. 03-313). Association of P. reicheli, V. radoicicaeand B. peneropliformis with C. lehneri in the lowerpart of the section suggests the occurrence of thesespecies in the Middle Cenomanian (Figure 5).Pseudorhapydionina laurinensis appears sevenmetres above the horizon where C. fraasi disappears.C. gradata, T. avnimelechi, N. regularis and B. bentoriappear in the uppermost part of the UpperCenomanian in this section (sample no. 03-324-03-322). The absence of bauxitic and lateritic levels, aswell as pelagic deposits suggests that platformconditions persisted from the Middle Cenomanianto the Late Turonian at least in this part of theplatform.

Demirci Dere SectionThe 7-m-thick neritic limestones underlying pelagiclimestones include C. zubairensis, suggesting a Late

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pain

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cchi

ni et

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(198

4) It

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ti (1

984)

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nce,

11−

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tte (1

985)

Fra

nce

& S

pain

, 12−

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llade

et a

l. (1

985)

Mes

ogea

, 13−

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oede

r & N

eum

ann

(198

5) M

edite

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ean

regi

on, 1

4− C

herc

hi &

Sch

roed

er (1

985)

Ital

y, 15

− G

usic

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l. (1

988)

Cro

atia

, 16−

Fuc

ek et

al.

(199

0) C

roat

ia,

17−

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shen

y &

Tro

nche

tti (1

993)

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nce,

18−

Velic

& V

laho

vic (

1994

) Cro

atia

, 19−

Chi

occh

ini e

t al.

(199

4) It

aly,

20−

Bilo

tte (1

998)

Tet

hyan

& A

dria

tic, 2

1−Ch

iocc

hini

& M

anci

nelli

(200

1) It

aly,

22−

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l. (2

006)

Tur

key

(Tim

e sc

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is ad

apte

d fro

m G

rads

tein

et a

l. 19

94).

B. SARI ET AL.

403

Mid

dle

Cen

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Upp

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ania

nB

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ĞL

AR

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03-429

03-428

03-427

03-42603-42503-42303-42103-418

03-41403-415

03-413

03-412

03-41003-40903-408

03-40703-406

03-405

03-404

03-40303-402

03-401

03-40003-39903-398

03-397

03-396

03-395

03-394

03-393

03-392

03-39103-39003-38903-38803-38703-386

03-38503-38403-38303-382

03-38103-380

03-379

03-37803-377

03-37603-37503-374

03-373

03-372

03-37103-37003-369

03-36803-367

100

102104

0

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9294

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114

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age

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mat

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ple

Num

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S-1: KOPARAN TEPE

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ycli

na

schlu

mber

ger

iP

seudoli

tuonel

lare

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iSpir

olo

culi

na

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S-1: KOPARAN TEPE continued

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UpperTuronian

116118120122124126128

130132134136

138140142144146148150

152154156

158160162164

168166

170172174176

178180

182184186188190192194196198200202204206208210212214216218220222224226228

03-366

03-36503-36403-363

03-36203-36103-36003-35903-35803-35703-35603-35503-35403-35303-35203-35103-35003-34903-34803-34703-34603-34503-34403-34303-34203-341

03-34003-33903-33803-33703-33603-33503-33403-33303-332

03-325

03-329

03-318

03-31703-316

03-31503-314

03-31303-31203-31103-310

03-309

03-308

03-30703-30603-30503-304

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

Figure 6. Stratigraphic distribution of microfossils within the Koparan Tepe section (see Figure 4 for explanations and Figure1 for location of the section).

Cenomanian age for this section (Figures 5 & 7).Chrysalidina gradata in sample no. 03-475accompanies C. zubairensis. The 5.5-m-thick lowerpart of the neritic limestones is brecciated andincludes rudist shell fragments at the lowest part ofthe section. The 1.5-m-thick uppermost part consistsof thick-bedded limestones. Thin-bedded (10−15cm) pelagic limestones, including sand to finepebble-size intraclasts derived from variousstratigraphic levels of neritic, hemipelagic andpelagic limestones, disconformably overlies neriticlimestones on a prominent erosional surface. Theplanktonic foraminifera associations indicate thatthe lower pelagic limestones are Late Campanian inage (Sarı 2006b).

Karain SectionThis section is represented by a rich caprinid,ichthyosarcolitid and radiolitid fauna (caprinidlithosome) suggesting a Middle to Late Cenomanianage. Rudists are associated with corals andgastropods, as well as scarce benthonic foraminifera(Figure 8). The uppermost part of the 120-m-thicksequence is characterized by the occurrence ofOrbitolina sp. in three samples. The presence of M.cretacea and P. laurinensis in sample no. 03-634 closeto the central part of the succession indicates an agenot older than the Middle Cenomanian (Figure 5).

The rudist fauna comprising I. bicarinatus, I.triangularis, C. schiosensis, N. gigantea, S. cf.schiosensis, S. woodwardi, Durania sp., Radiolites sp.,Sauvagesia sp., and unidentifiable radiolitids, wasstudied by Özer (1988), who also reported it fromSerinhisar (Denizli) in Turkey (Özer 1998). Thefauna has been reported from many Middle−UpperCenomanian outcrops in the circum-Mediterraneanregion (e.g., Plenicar 1963; Sliskovic 1968; Polsak &Mamuzic 1969; Bilotte 1985; Accordi et al. 1989;Lupu 1992; Cherchi et al. 1993).

Yağca SectionThe neritic limestones in the lowest part of thissection, which are the lateral equivalent oflimestones observed in the Karain section, arecharacterized by rather scarce foraminifera and a

rich rudist assemblage similar to the Karain section.A different Cenomanian assemblage is observed inthe pebbles of the Karakirse Formation (Figure 9).Pebbles and blocks of neritic limestones areembedded in pelagic matrix with planktonicforaminifera, which indicates a latestCampanian−Early Maastrichtian age (Sarı 2006b).

UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP

404

Figure 7. Stratigraphic distribution of microfossils within theDemirci Dere section (see Figure 4 for explanationsand Figure 1 for location of the section).

Canavar Boğazı SectionThe neritic part of this section is mainly representedby scarce benthonic foraminifera.Pseudorhapydionina laurinensis, known as aMiddle−Late Cenomanian species, is present insamples no. 07-627 and 97-630 (Figures 5 & 10). Theoccurrence of P. reicheli, P. dubia, B. peneropliformis,N. regularis and C. gradata in the uppermost part ofthe neritic limestones indicates that the neritic partof this section is no younger than Late Cenomanian.The uppermost part of the neritic succession,represented by the occurrence of unidentifiableradiolitid fragments, is disconformably overlain bypelagic limestones. The planktonic foraminiferaassemblage observed in the pelagic limestonessuggests a Late Campanian age (Sarı 2006b).

Kargalıköy SectionThis section is represented by cream-coloured, well-bedded (30−60 cm), indurated neritic limestones ofthe Bey Dağları Formation. This is one of the most

B. SARI ET AL.

405

03-60403-605

03-609

03-60603-60703-608

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

03-63503-63603-637

03-63803-63903-64003-64103-642

03-643

03-64403-645

03-64703-646

03-64803-649

03-650

03-65103-65203-65303-654

03-65503-65603-657

03-658

03-65903-66003-66103-662

03-66303-664

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

vaben

tori

Cuneo

lina

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nia

Mer

lingin

acr

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na

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sp.

Lit

holo

gy

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S-3: KARAİNY

AĞ

CA

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dle

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ian

?

Figure 8. Stratigraphic distribution of microfossils within theKarain section (see Figure 4 for explanations andFigure 1 for location of the section).

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

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anFigure 9. Stratigraphic distribution of microfossils within the

Yağca section (see Figure 4 for explanations andFigure 1 for location of the section).

important sections as it contains the remarkableroad-cut outcrop of the Upper Turonian rudist level(hippuritid lithosome) (Figure 11). The lower part ofthe 20-m-thick lithosome is dominated by V.praegiganteus, associated with rare V. inferus, small-sized hippuritids and radiolitids. Analysis of well-preserved low-Mg calcite of shells of V. praegiganteusfor 87Sr/86Sr values yielded a Late Turonian age (Sarıet al. 2004). The abundance of V. praegiganteus aswell as other rudists decreases towards the upperpart of the lithosome, in which small-sized

UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP

406

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

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age

For

mat

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Sam

ple

Num

ber

S-5: CANAVAR BOĞAZI

Cuneo

lina

pavo

nia

Chare

nti

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lina

schlu

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ger

iP

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molo

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na

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mi

Pse

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ala

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nen

sis

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iSpir

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na

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Benthonic foraminifera

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Num

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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

97-435

Mid

dle

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ud

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nel

lare

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Bo

livi

no

psi

sca

pit

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Pse

ud

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ina

Nez

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taP

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Pse

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Abundant occurrence of

Hippuritid lithosome)Vaccinites praegiganteus(

Figure 10. Stratigraphic distribution of microfossils within theCanavar Boğazı section (see Figure 4 forexplanations and Figure 1 for location of thesection).

Figure 11. Stratigraphic distribution of microfossils within theKargalıköy section (see Figure 4 for explanations andFigure 1 for location of the section).

hippuritids and radiolitids are common. The lowerpart of the section has a Middle−Late Cenomanianforaminiferal assemblage. There is nopalaeontological data for the level between the lastoccurrence of the Cenomanian assemblage and thefirst occurrence of rudists. The uppermost part of theneritic succession between the last occurrence of therudists and the first occurrence of the?Coniacian−Santonian planktonic foraminifera isalso barren and may questionably correspond to thelatest Turonian or Coniacian. The rare planktonicforaminifera content of the 10-m-thick hemipelagiclevel at the uppermost part of the section maysuggest a Coniacian-Santonian age (Sarı 2006b). Theboundary relationship between the neritic and thehemipelagic limestones in this section is not clear.

Boztaş Tepe SectionThis section includes an assemblage containing P.dubia, P. laurinensis and C. gradata at the base of thesection (Figure 12). This association indicates aMiddle to Late Cenomanian age. The rest of thesuccession has long-ranging taxa. The firstoccurrence of M. apenninica-compressa in sample no.97-193 indicates the Coniacian (Figure 5). Theuppermost part of the section is made up of massiveneritic limestones that are cut by an erosional surfaceand overlain by pelagic conglomerates. Theplanktonic foraminifera observed in the matrix ofthe conglomerates with pelagic matrix and theoverlying pelagic limestones indicate the MiddleEocene (Sarı 2006b). The absence of any pelagicinterlayer or any sedimentary structures showingsubaerial exposure throughout the 625-m-thicksequence indicates that the platform environmentwas not interrupted in this part of the platform.

Sarp Dere SectionOnly in the Sarp Dere section were the caprinids(rudists) determined in the whole Bey DağlarıAutochthon outside the Katran Dağ area. Caprinidsobserved in the middle part of the section as scarceunidentifiable individuals associated with rareradiolitids (Figure 13) indicate a Cenomanian age.The poor benthonic foraminifal assemblagedetermined in the lowest part of the section is

B. SARI ET AL.

407

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

97-18097-179

97-178

97-177

97-175

97-17497-17397-17297-16897-16697-16597-164

97-16197-16297-163

Con

iaci

anB

EY

DA

ĞL

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I

MiddleEocene

Pse

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nin

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ger

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on

cha

rmo

nti

aa

pen

nin

ica

-co

mp

r ess

aP

seu

do

cycl

am

min

asp

ha

ero

idea

Nez

zaza

tasi

mp

lex

Pse

ud

on

um

mo

locu

lin

ah

eim

i

Cu

neo

lin

ap

avo

nia

Nez

zaza

tin

ella

Pse

ud

ocy

cla

mm

ina

Mil

ioli

dae

Rot

alid

ae/D

isco

rbid

aesp

. (no

n)

sp.

Ata

xoph

ragm

iida

esp

.

?Tur

onia

nM

iddl

e-U

pper

Cen

oman

ian

Upp

erT

uron

ian

Figure 12. Stratigraphic distribution of microfossils within theBoztaş Tepe section (see Figure 4 for explanationsand Figure 1 for location of the section).

typically Middle−Late Cenomanian Bey Dağlarıassemblage, as observed in the other stratigraphicsections. The appearance of P. sphaeroidea in sampleno. 97-9 in the uppermost part of the successionindicates a Coniacian age. The top surface of theneritic limestones is erosional and they are overlainby thin-bedded pelagic limestones of the AkdağFormation containing a rich planktonicforaminiferal assemblage suggesting a LateCampanian−Early Maastrichtian age (Sarı 2006a).

Küçük Tepe SectionSamples from the lower part of this section containMiddle−Late Cenomanian assemblages (Figure 14).The occurrence of P. sphaeroidea in sample no. 97-68allows the Turonian−Coniacian boundary to bedrawn. The uppermost neritic limestones,represented by a rudist level with abundantradiolitids, are disconformably overlain by pelagiclimestones of the Akdağ Formation containing richplanktonic foraminifera assemblages suggesting aLate Campanian−Early Maastrichtian age (Sarı2006a).

Çamkuyusu SectionThe approximately 400-m-thick lower part of thesequence is almost barren and only sample no. 04-41contains a poor assemblage, including a few species;C. gradata, N. picardi and P. reicheli. The lower partof the second half includes a relatively richassemblage. The last occurrences of C. gradata and P.reicheli in sample no. 04-65 determine theCenomanian−Turonian boundary. The firstoccurrence of P. sphaeroidea in sample no. 04-69suggests a Coniacian age. The approximately 200-m-thick upper part of the section is represented only bylong-ranging taxa. The sequence includes rare non-diagnostic rudists and non-rudist bivalvesthroughout.

Benthonic Foraminiferal BiostratigraphyDetailed investigations of ten measured stratigraphicsections from the BDCP (Figures 6 through 15) showthat the lower part of the platform limestones(Middle−Upper Cenomanian) is represented by

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Sam

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97-45

97-4497-43

97-4297-4197-4097-39

97-38

97-37

97-36

97-35

97-34

97-9b

97-997-8

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

97-1397-1297-11

97-10

97-21

Tur

onia

n-

?C

onia

cian

BE

YD

AĞ

LA

RI

AK

DA

Ğ

Pse

udonum

molo

culi

na

hei

mi

Bic

onca

vaben

tori

Pse

udocy

clam

min

aP

seudorh

apyd

ionin

adubia

Chry

sali

din

agra

data

Nez

zaza

tinel

lapic

ard

iP

seudoli

tuonel

lare

ichel

iSpir

olo

culi

na

Nez

zaza

taP

seudorh

apyd

ionin

ala

uri

nen

sis

Tex

tula

ria

Cuneo

lina

pavo

nia

Boli

vinopsi

sca

pit

ata

Pse

udocy

clam

min

asp

haer

oid

eaB

eloru

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.

Figure 13. Stratigraphic distribution of microfossils within theSarp Dere section (see Figure 4 for explanations andFigure 1 for location of the section).

relatively rich benthonic foraminiferal assemblages,while the upper part (Turonian−Coniacian) containspoor assemblages. These data are consistent withother previously described Mediterraneansuccessions (Figure 5). Numerous studies of theUpper Cretaceous benthonic foraminiferalbiostratigraphy have been carried out in theMediterranean region since the beginning of thesecond half of the last century. The data werecompiled by Arnaud et al. (1981) and Schroeder &Neumann (1985). Bilotte (1998) presented thedistributions of important Tethyan benthonicforaminiferal species. Correlation of thestratigraphic distribution of the important benthonicforaminiferal species, derived from 22 publishedpapers, is summarized in Figure 5. The species in thischart are only those that were also observed in theBDCP. Correlation of the biozonations offered forthe Upper Cretaceous neritic successions of theBDCP is given in Figure 16.

Benthonic foraminiferal assemblages determinedin the BDCP successions are dominated by long-ranging species. The presence of shorter-ranging,stratigraphical index species, the first (FO) and/orthe last occurrence (LO) of the taxa and the co-existence of two or more taxa are all important infiner biostratigraphic subdivision. The benthonicforaminiferal biozones were established usingrecommendations of the NASC (1983) and the ISG(Salvador 1994).

Psedolituonella reicheli-P. dubia ConcurrentRange Zone has been defined from theMiddle−Upper Cenomanian platform limestones.The biozone includes the C. lehneri Subzone and C.zubairensis subzone, which correspond to the Middleand Upper Cenomanian respectively (Figure 17).The biozones identified in this study are brieflydescribed below from oldest to youngest (Plates 1 to4):

P. reicheli-P. dubia Concurrent Range Zone. Thisbiozone is determined from the FO of P. reicheli andthe LO of P. dubia (Figure 17). Pseudolituonellareicheli and P. dubia are selected as biozone markers,because they are the commonest species observed inthe BDCP and are also widely recorded from theCenomanian shallow-water limestones of thecircum-Mediterranean region. The biozone is

B. SARI ET AL.

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97-47

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97-55

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97-66

97-67

97-68

97-69

97-70

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97-73

97-74

S-9: KÜÇÜK TEPE

97-75

BE

YD

AĞ

LA

RI

Mid

dle

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Cen

oman

ian

Chry

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din

agra

data

Nez

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Pse

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nen

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Pse

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molo

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na

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culi

na

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mi

Monch

arm

onti

aapen

nin

ica-c

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asp

haer

oid

ea

sp.

sp.

sp.

Con

iaci

an

L.Maast.-U.Camp.

?T

uron

ian

AK

DA

Ğ

Figure 14. Stratigraphic distribution of microfossils within theKüçük Tepe section (see Figure 4 for explanationsand Figure 1 for location of the section).

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)

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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

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04-51

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400

420

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)

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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

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04-64

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ian

Figure 15. Stratigraphic distribution of microfossils within the Çamkuyusu section (see Figure 4 for explanations and Figure1 for location of the section).

B. SARI ET AL.

411

CenomanianTuronianConiacianSantonian

Cam

p.

STAGES

INFORMALSUBSTAGES

Alb

.

Lo

w.

Mid

.

Up

.

Mid

.

Mid

.

Mid

.

Up

.

Up

.

Up

.

Lo

w.

Lo

w.

Lo

w.

Lo

w.

Up

.

Fle

ury

(1980)

Gre

ece

Alt

ıner

&D

ecro

uez

(1982)

South

ern

Turk

ey

Gar

gouri

-R

azgal

lah

(1983)

Cen

tral

Tunis

ia

Bil

ott

e(1

985)

Spai

n-F

rance

Chio

cchin

i&

Man

cinel

li(1

977),

Chio

cchin

iet

al.

(1984)

(Ita

ly)

Mo

ull

ade

etal

.(1

98

5)

Mes

og

ea

Vel

ic&

Vla

hovic

(1994)

Cro

atia

Tas

lıet

al.(2

006)

South

ern

Tu

rkey

This

Stu

dy

South

wes

tern

Turk

ey(B

eyD

ağla

rıC

arbonat

eP

latf

orm

)N

ort

her

nP

art

Sai

nt-

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c(1

981)

Leb

anon

CsB1CsB2CsB3CsB4

Sellialveolinaviallii gr.biozone

Broeckinabalcanicabiozone

Pseudocyclamminasphaeroideabiozone

Murg

ella

lata

bio

zone

?

C4-1C4-2

C4

-3a

C4

-3b

C5-1C5-2

Pseudodomiaviallii

P.l

auri

nen

sis

Cis

alv

eoli

na

fall

ax

Hip

puri

tes

NummoloculinaregularisMerlinginaPseudorhapydionina

Pse

udodom

iavi

all

ii

Undif

fere

nti

ated

Num

mofa

lloti

aapula

Pse

udorh

apyd

ionin

aN

um

molo

culi

ne

Ost

raco

da

and

Mil

ioli

dae

P.

dubia

P.

lauri

nen

sis

and

C.gra

data

P.

reic

hel

ian

d

Sim

pla

lveo

lina

sim

ple

x

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etace

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.(C

.)co

nic

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ace

a

Orbitolina(Conicorbitolina)conica

CEN-1CEN-2

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ii

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Biconcavabentoricenozone

OstracodaandMiliolidae

IntervalZone

Moncharmontiacompressa

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uli

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un

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ifer

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Str

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raphic

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Mediumtothick-beddedshallowwater(innerplatform)limestones

Planktonicforaminifera-bearingmassivehemipelagiclimestones

Dis

con

form

ity

NO

TT

OS

CA

LE

Dic

ari

nel

laco

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vata

inte

rval

zone

(par

t)

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ari

nel

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met

rica

range

zone

Abundan

tocc

urr

ence

of

the

rudis

tbiv

alve

(Touca

s).

(mea

nnum

eric

alag

e:)

(Sar

ıet

al.,

2004).

Vacc

init

espra

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ante

us

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ysi

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chem

ical

lyw

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pre

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ies

for

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ues

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yie

lded

aL

ate

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e89.1

1-

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0M

a

87

86

Pel

agic

lim

esto

nes

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do

tru

nca

na

calc

ara

tara

ng

ezo

ne

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ula

mm

ina

pic

ard

i

Num

molo

culi

na

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d

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ord

iell

aco

nic

a

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rbin

ella

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ella

i

and

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cchin

iet

al.

(1994),

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cchin

i&

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cinel

li(2

001),

(Ita

ly)

Acc

ord

iell

aco

nic

a

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rbin

ella

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ella

i

and

Nez

zaza

tinel

laaeg

ypti

aca

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molo

culi

na

irre

gula

ris

cf.

and

cf. C

.gra

data

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reic

hel

ian

d

P.

dubia

P.

lauri

nen

sis

and

Ost

raco

da

and

Mil

ioli

dae

Cap

rinid

lith

oso

me

(Mid

-Lat

eC

enom

ania

n)

P.reicheli-P.dubiaConcurrentRange

Zone

C.

zubair

ensi

sS

ubzo

ne

C.

lehner

iS

ubzo

ne

M.apenninica-compressa

P.sphaeroidea

?

Figu

re 1

6.Ch

art s

how

ing t

he b

enth

onic

fora

min

ifera

l bio

zona

tions

pre

viou

sly o

ffere

d fo

r the

per

i-Med

iterr

anea

n U

pper

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tace

ous p

latfo

rm li

mes

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elat

ion

of t

hese

bio

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tions

with

the

est

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hed

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er C

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ceou

s be

ntho

nic

fora

min

ifera

l bio

zona

tion

for

the

nort

hern

par

t of

the

Bey

Dağ

ları

Carb

onat

ePl

atfo

rm. (

Tim

e sc

ale

is ad

apte

d fro

m G

rads

tein

et a

l. 19

94).

UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP

412

Figu

re 1

7.Lo

cal r

ange

s of t

he b

enth

onic

fora

min

ifera

obs

erve

d in

the

Upp

er C

reta

ceou

s car

bona

te su

cces

sions

of t

he B

DCP

.

defined from the Koparan Tepe section, in which it is176.5 metres thick (Figure 7). The FO and the LO ofP. reicheli are documented in samples no. 03-424 and03-324, respectively. This species is rare throughoutthe section. The FO and the LO of P. dubia areobserved in samples no. 03-417 and 03-322respectively.

The Pseudolituonella reicheli-P. dubia ConcurrentRange Zone includes many Cenomanian (i.e., P.parvus, T. avnimelechi, V. radoicicae, B. bentori, B.peneropliformis, N. regularis, P. reicheli and C.gradata) and Middle−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 thebiozone cannot be recognized properly in otherstratigraphic sections due to the rareness of thespecies and/or reduced thickness of neriticlimestones in some stratigraphic sections. The P.reicheli-P. dubia Concurrent Range Zone includestwo subzones:

Cisalveolina lehneri subzone: This biozone isdefined by the total range of the nominate taxon inthe Koparan Tepe section, where it is 35.5 metresthick (Figures 6 & 17). The species has its FO and LOin samples no. 03-417 and 03-398, respectively(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). Cisalveolina lehneri is recordedfrom Middle Cenomanian successions in thecircum-Mediterranean region (Chiocchini et al.1984, 1994; Schroeder & Neumann 1985). Hence, theage of the interval corresponding to this biozoneshould be Middle Cenomanian in the Koparan Tepesection (Figure 6).

Coxites zubairensis Subzone: This biozone isdefined from the FO to the LO of the nominate taxonin the Demirci Dere section, in which the biozone is4.5 metres thick (Figures 7 & 17). The biozonecontains C. pavonia, N. simplex, P. reicheli, C.gradata, M. cretacea, N. picardi, N. conica and B.peneropliformis in this section (Figure 7): Coxiteszubairensis is also present in sample no. 03-324 in the

Koparan Tepe section. The species is associated withD. schlumbergeri, P. reicheli, N. conica, N. simplex, P.dubia, B. peneropliformis, M. cretacea, C. gradata andT. avnimelechi (Figure 6). Coxites zubairensis isrecorded from the Upper Cenomanian successionsof the circum-Mediterranean region (Saint-Marc1977, 1981; Chiocchini et al. 1984, 1994): hence theage of this biozone in the Demirci Dere section isLate Cenomanian in (Figure 7).

Other Stratigraphically Importat Taxa: TheFO of the two important species M. apenninica-compressa and P. sphaeroidea is also used to date thepost-Cenomanian limestones of the BDCP (Figure17). The FO of M. apenninica-compressa is acceptedas Late Turonian (de Castro 1966; Gusic & Jelaska1990; Chiocchini & Mancinelli 1977; Chiocchini etal. 1994; Korbar & Husinec 2003). Moncharmontiaapenninica-compressa was observed in twostratigraphic sections in this study. The FO of thespecies in sample no. 97-200 in the Boztaş Tepesection indicates a Late Turonian age (Figure 12).The species is associated with P. sphaeroidea insample no. 97-68 from the Küçük Tepe section(Figure 14).

The FO of Pseudocyclammina sphaeroidea is usedby some to mark the Turonian–Coniacian boundary(Bilotte 1984, 1998; Fucek et al. 1990), while othersplace it within the Coniacian (Chiocchini &Mancinelli 1977; Bilotte 1985; Grosheny &Tronchetti 1993; Chiocchini et al. 1994). P.sphaeroidea was observed in four stratigraphicsections where its FO determines theTuronian−Coniacian boundary (Figures 12−15 &17)

In addition to the biozones and the ‘index’species, the LOs of some taxa are also useful todetermine the Cenomanian−Turonian boundary inthe absence of zone marker species. Many taxa areaccepted as Cenomanian species in the peri-Mediterranean region (Figure 5) of which some,such as B. peneropliformis, C. gradata, P. laurinesis, B.bentori, M. cretacea, N. regularis and T. Avnimelechi,have been observed in the Bey Dağları successionsand are used to mark the Cenomanian−Turonianboundary. M. cretacea and P. laurinensis are knownMiddle−Late Cenomanian species (Figure 17).

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ConclusionsDetailed investigations of the ten measuredstratigraphic sections logged from the inner platformlimestones have yielded new data to construct theUpper Cretaceous (MiddleCenomanian−Coniacian) benthonic foraminiferalbiostratigraphy of the Bey Dağları carbonateplatform (BDCP). These data have been integratedwith the data obtained from rudists and planktonicforaminifera biostratigraphy and Sr-isotopestratigraphy. The lower part of the platformlimestones (Middle−Upper Cenomanian) isrepresented by relatively rich benthonicforaminiferal assemblages, while the upper part(Turonian−Coniacian) contains poor assemblages.These data are consistent with several otherMediterranean successions. The benthonicforaminiferal assemblages determined in the BDCPare dominated by long-ranging species. The shorter-ranging, stratigraphical index species have beenselected to establish biostratigraphic framework andto date the Upper Cretaceous platform limestones ofthe BDCP, based on the distributions of these speciesin the circum-Mediterranean region.

The benthonic foraminiferal assemblagesidentified from the neritic limestones have allowedestablishment of one biozone and two subzones. The

P. reicheli-P. dubia Concurrent Range Zone is definedfrom the Middle−Upper Cenomanian part of thesuccession and includes two subzones. The C. lehneriand C. zubairensis subzones are characterized by therange of the nominate taxa and correspond to theMiddle Cenomanian and Upper Cenomanian,respectively. Moncharmontia apenninica-compressaand P. sphaeroidea are the stratigraphically importanttaxa for the post Cenomanian part of the Bey Dağlarısuccessions and they indicate the beginning of theUpper Turonian and the Coniacian, respectively.

All the data mentioned above show that theneritic accumulation on the BDCP continuouslypersisted from the Middle Cenomanian to theConiacian.

AcknowledgementsWe thank Antun Husinec for his invaluable reviewthat improved the manuscript considerably. İsmailİşintek is thanked for his advice and discussions onbenthonic foraminiferal biozonations. The fieldworkhelp of Akif Sarı, Ümit Kasım, Evren Yücel andGörkem Oskay is also appreciated. This work wasfinancially supported by a TÜBİTAK project no.102Y062, which is also gratefully acknowledged.English of the final text is edited by John A.Winchester.

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PLATE I

1- Cisalveolina lehneri; Koparan Tepe section; sample no. 03-416.2- Cisalveolina lehneri; Koparan Tepe section; sample no. 03-413.3- Cisalveolina lehneri; Koparan Tepe section; sample no. 03-413.4- Cisalveolina fraasi; Koparan Tepe section; sample no. 03-381.5- Cisalveolina fraasi; Koparan Tepe section; sample no. 03-381.6- Orbitolina sp.; Karain section; sample no. 03-660.7- Vidalina radoicicae; Koparan Tepe section; sample no. 03-418.8- Vidalina radoicicae; Koparan Tepe section; sample no. 03-416.9- Bolivinopsis capitata; Koparan Tepe section; sample no. 03-296.

The bar below each photomicrographs is 500 μm. g

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1

5

3

4

2

6

7 8 9

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PLATE II

1- Biplanata peneropliformis; Koparan Tepe section; sample no. 03-349.2- Biplanata peneropliformis; Canavar Boğazı section; sample no. 97-633.3- Merlingina cretacea; Koparan Tepe section; sample no. 03-324.4- Merlingina cretacea; Koparan Tepe section; sample no. 03-324.5- Biconcava bentori; Canavar Boğazı section; sample no. 97-631.6- Biconcava bentori; Koparan Tepe section; sample no. 03-322.7- Nezzazata simplex; Koparan Tepe section; sample no. 03-416.8- Nezzazata simplex; Koparan Tepe section; sample no. 03-416.9- Nezzazata simplex; Demirci Dere section; sample no. 03-478.10- Nezzazata conica; Yağca Section; sample no. 03-671 (from a reworked association).11- Trochospira avnimelechi; Koparan Tepe section; sample no. 03-324.12- Nezzazatinella picardi; Koparan Tepe section; sample no. 03-310.13- Nezzazatinella picardi; Boztaş Tepe section; sample no. 97-185.

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1 23 4

5 6 7

8

9

10

11

12 13

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PLATE 3

1- Chrysalidina gradata; Canavar Boğazı section; sample no. 97-634.2- Chrysalidina gradata; Sarp Dere section; sample no. 97-38.3- Pseudorhapydionina laurinensis; Koparan Tepe section; sample no. 03-378.4- Pseudorhapydionina laurinensis; Canavar Boğazı section; sample no. 97-627.5- Pseudorhapydionina laurinensis; Canavar Boğazı section; sample no. 97-627.6- Pseudorhapydionina dubia; Koparan Tepe section; sample no. 03-416.7- Cuneolina pavonia; Koparan Tepe section; sample no. 03-419.8- Dicyclina schlumbergeri; Yağca Section; sample no. 03-671 (from a reworked association).9- Dicyclina schlumbergeri; Yağca Section; sample no. 03-671 (from a reworked association).10- Pseudolituonella reicheli; sample 03-478.

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1 2 3

4 5

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7 8 9 10

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PLATE 4

1- Coxites zubairensis; Koparan Tepe section; sample no. 03-324.2- Coxites zubairensis; Demirci Dere section; sample no. 03-474.3- Coxites zubairensis; Demirci Dere section; sample no. 03-479.4- Moncharmontia apenninica-compressa; sample 97-191.5- Moncharmontia apenninica-compressa; sample 97-200.6- Pseudonummoluculina heimi; Canavar Boğazı section; sample no. 97-627.7- Pseudonummoluculina heimi; Koparan Tepe section; sample no. 03-368.8- Nummoloculina regularis; Koparan Tepe section; sample no. 03-416.9- Pseudocyclammina sphaeroidea; Boztaş Tepe section; sample no. 97-193.

B. SARI ET AL.

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