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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: [email protected])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.
393
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
UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP
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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
B. SARI ET AL.
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Black Sea
Mediterranean Sea
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Stratigraphic Sections
1. Koparan Tepe2. Demirci Dere3. Karain4. Yağca5. Canavar Boğazı6. Kargalıköy7. Boztaş Tepe8. Sarp Dere9. Küçük Tepe10. Çamkuyusu
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
UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP
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B. SARI ET AL.
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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).
UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP
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B. SARI ET AL.
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Figure 3. Generalized stratigraphic column of the northern part of the Bey Dağları Autochthon. (see Figure 4 forexplanations).
UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP
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Radiolitids
Distefanella sp.
Thin-bedded
limestones
massiveStylolite
Gastropods
Caprinids
Corals
Ichthyosarcolitids
EXPLANATIONS
LITHOLOGY FOSSIL CONTENTANDSEDIMENTARY STRUCTURES
cf.=
Palaeogene
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
B. SARI ET AL.
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CenomanianTuronianConiacianSantonian
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SUBSTAGES
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NummoloculinaregularisPHILIPSON
35 78 1118 22
BiconcavabentoriHAMAOUI&SAINT-MARC
23 5
79 1113 17
22
419 {
CoxiteszubairensisSMOUT
3 5
9 19
{
MerlinginacretaceaHAMAOUI&SAINT-MARC
35 7 913 17 19
11
Moncharmontiaapenninica-compressa
16
2115
19
4
{
Murgeinaapula(LUPERTO-SINNI)
21
19{
Ch
rysa
lid
ina
gra
da
taD
'OR
BIG
NY
23 5
6
789 11 1316 17
18 20
15
22
4
19
{
1
Pseudonummoloculinaheimi(BONET)
23
59 15
6
15
4
Tro
cho
spir
aa
vnim
elec
hi
HA
MA
OU
I&
SA
INT-
MA
RC
3 567
8
1113 17
915
4
Pse
ud
oli
tuo
nel
lare
ich
eli
MA
RIE
235
6 789 1113
17 18
4
20
{
1
Pse
ud
orh
ap
ydio
nin
ad
ub
ia(D
EC
AS
TR
O)
23
5 67
89 1113
17 18
20 22
4 19 {
1
Pseudorhapydioninalaurinensis(DECASTRO)
35
6
9 1318
8
4191
BiplanatapeneropliformisHAMAOUI&SAINT-MARC
35
7
913 17 2219 4
{
1
PeneroplisparvusDECASTRO
13
20
2218
VidalinaradoicicaeCHERCHI&SCHROEDER
18 15
19 {
14
PseudocyclamminasphaeroideaGENDROT
8 10
1617
11
20
419 {
Cisalveolinafraasi(GÜMBEL)
CisalveolinalehneriREICHEL
79 13
20
13 9
19
19
Figu
re 5
.Cor
relat
ion
of st
ratig
raph
ic d
istrib
utio
ns o
f sel
ecte
d be
ntho
nic
fora
min
ifera
from
diff
eren
t Tet
hyan
loca
litie
s, in
cludi
ng th
e Be
y D
ağla
rı ca
rbon
ate
plat
form
(this
study
). D
ata
wer
e de
rived
fro
m t
he f
ollo
win
g so
urce
s; 1−
Fle
ury
(197
1) G
reec
e, 2−
Ber
thou
(19
73)
Port
ugal
, 3−
Sain
t-Mar
c (1
977)
Mes
ogea
, 4−
Chio
cchi
ni &
Man
cine
lli (1
977)
Ital
y, 5−
Sai
nt-M
arc
(198
1) L
eban
on, 6
− G
argo
uri-R
azga
llah
(198
3) T
unisi
a, 7−
Ber
thou
(198
4) P
ortu
gal,
8− B
ilotte
(198
4)Fr
ance
& S
pain
, 9−
Chio
cchi
ni et
al.
(198
4) It
aly,
10−
Tron
chet
ti (1
984)
Fra
nce,
11−
Bilo
tte (1
985)
Fra
nce
& S
pain
, 12−
Mou
llade
et a
l. (1
985)
Mes
ogea
, 13−
Schr
oede
r & N
eum
ann
(198
5) M
edite
rran
ean
regi
on, 1
4− C
herc
hi &
Sch
roed
er (1
985)
Ital
y, 15
− G
usic
et a
l. (1
988)
Cro
atia
, 16−
Fuc
ek et
al.
(199
0) C
roat
ia,
17−
Gro
shen
y &
Tro
nche
tti (1
993)
Fra
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−
Taslı
et a
l. (2
006)
Tur
key
(Tim
e sc
ale
is ad
apte
d fro
m G
rads
tein
et a
l. 19
94).
B. SARI ET AL.
403
Mid
dle
Cen
oman
ian
Upp
erC
enom
ania
nB
EY
DA
ĞL
AR
I
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
2
46
8101214
16
18202224
26
28
30
32
3436
3840
4244
4648
5052
5456
58
6062
64666870
72
7476
78
80
82
84
86
8890
9294
9698
106108
112110
114
Lit
holo
gy
Thi
ckne
ss(m
)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
S-1: KOPARAN TEPE
Dic
ycli
na
schlu
mber
ger
iP
seudoli
tuonel
lare
ichel
iSpir
olo
culi
na
Anta
lyna
Cuneo
lina
pavo
nia
Vid
ali
na
radoic
icae
Nez
zaza
taco
nic
aN
ezza
zata
sim
ple
xC
isalv
eoli
na
lehner
iP
seudorh
apyd
ionin
adubia
Pse
udonum
molo
culi
na
hei
mi
Bip
lanata
pen
eropli
form
isN
ezza
zata
Cis
alv
eoli
na
fraasi
Nez
zaza
tinel
lapic
ard
iP
seudorh
apyd
ionin
ala
uri
nen
sis
sp.
sp.
Mil
ioli
dae
sp.
gr.U
pper
Cen
oman
ian
Tur
onia
n
BE
YD
AĞ
LA
RI
Lit
holo
gy
Thi
ckne
ss(m
)
Sta
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
S-1: KOPARAN TEPE continued
Dic
ycli
na
schlu
mber
ger
iP
seudoli
tuonel
lare
ichel
iC
oxi
tes
zubair
ensi
sC
uneo
lina
pavo
nia
Nez
zaza
taco
nic
aN
ezza
zata
sim
ple
xP
seudorh
apyd
ionin
adubia
Bip
lanata
pen
eropli
form
isN
ezza
zata
Nez
zaza
tinel
lapic
ard
iP
seudorh
apyd
ionin
ala
uri
nen
sis
Mer
lingin
acr
etace
aP
ener
opli
sparv
us
Pse
udonum
molo
culi
na
Pse
udorh
apyd
ionin
aC
hry
sali
din
agra
data
Tro
chosp
ira
avn
imel
echi
Num
molo
culi
na
regula
ris
Bic
onca
vaben
tori
Boli
vinopsi
sca
pit
ata
Mil
ioli
dae
sp.
sp.
sp.
Nez
zaza
tida
e
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
roduesP
aibudaninoidypah
ainovapani loenu
Cxelp
misatazazze
Nr
allenoutiloduesP
ilehc ieriabuz
setix oC
sisneatadar g
anidila syrhC
rcanignilre
Maecate
atazazzeN
racipallenitazazze
Ndi
anilucoloripSacinoc
atazazzeN
rene patanal pi
Bsi
mrofilpo
.p s
.ps
0
1
2
3
0
1
2
3
4
5
6
7
8
9
10
03-489
03-490
03-49103-49203-49303-494
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
Lithology
)m(ssenkcihT
egatsbuS/egatS
noitamroF
e lpmaS
rebmu
N
Benthonic foraminiferaS-2: DEMİRCİ DERE
nainamone
CreppU
IRAL
ĞAD
YEB
ĞADKA
dekrow er
nainapma
CreppU
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
pavo
nia
Mer
lingin
acr
etace
aN
ezza
zata
sim
ple
xP
seudorh
apyd
ionin
adubia
Pse
udorh
apyd
ionin
ala
uri
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: KARAİNY
AĞ
CA
KÖ
Y
Mid
dle
-U
pper
Cen
oman
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
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
ag
rad
ata
Dic
ycli
na
sch
lum
ber
ger
iN
ezza
zata
con
ica
Nez
zaza
tasi
mp
lex
Pse
ud
od
om
iad
rori
men
sis
Pse
od
oli
tuo
nel
lare
ich
eli
Pse
ud
orh
ap
ydio
nin
ad
ub
iaS
pir
olo
culi
nasp. sp
.M
ilio
lida
eT
extu
lari
dae
Benthonic foraminiferaS-4: YAĞCA
Mid
dle-
Upp
erC
enom
ania
n
KA
RA
KİR
SE
YA
ĞC
AK
ÖY
Upp
erC
ampa
nian
-L
ower
Maa
stri
chti
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
ge/S
ubst
age
For
mat
ion
Sam
ple
Num
ber
S-5: CANAVAR BOĞAZI
Cuneo
lina
pavo
nia
Chare
nti
aD
icyc
lina
schlu
mber
ger
iP
seudonum
molo
culi
na
hei
mi
Pse
udorh
apyd
ionin
ala
uri
nen
sis
Bic
onca
vaben
tori
Nez
zaza
tinel
lapic
ard
iSpir
olo
culi
na
Vid
ali
na
radoic
icae
Nez
zaza
taco
nic
aN
ezza
zata
sim
ple
xP
seudoli
tuonel
lare
ichel
iP
seudorh
apyd
ionin
adubia
Bip
lanata
pen
eropli
form
isN
um
molo
culi
na
regula
ris
Chry
sali
din
agra
data
Pen
eropli
ssp. sp
.
Mil
ioli
dae
sp.
Benthonic foraminifera
Mid
dle
-U
pper
Cen
oman
ian
AK
DA
ĞB
EY
DA
ĞL
AR
I
Upp
erC
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
97-435
Mid
dle
-U
pper
Cen
oman
ian
Upp
erT
uron
ian
?C
onia
cian
-L
. San
toni
an
BE
YD
AĞ
LA
RI
Cu
neo
lin
ap
avo
nia
Dic
ycli
na
sch
lum
ber
ger
iM
erli
ng
ina
cret
ace
aN
ezza
zati
nel
lap
ica
rdi
Pse
ud
oli
tuo
nel
lare
ich
eli
Bo
livi
no
psi
sca
pit
ata
Pse
ud
ocy
cla
mm
ina
Nez
zaza
taP
ener
op
lis
Pse
ud
orh
ap
ydio
nin
ad
ub
iaP
seu
do
rha
pyd
ion
ina
lau
rin
ensi
s
sp.
sp.
sp.
Mil
ioli
dae
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
AR
I
MiddleEocene
Pse
ud
orh
ap
ydio
nin
ad
ub
iaP
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ion
ina
lau
rin
ensi
s
Ch
rysa
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von
iaN
ezza
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nel
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ica
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ud
oli
tuo
nel
lare
ich
eli
Bo
livi
no
psi
sca
pit
ata
Dic
ycli
na
sch
lum
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ger
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rmo
nti
aa
pen
nin
ica
-co
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r ess
aP
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am
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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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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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97-55
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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
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BE
YD
AĞ
LA
RI
Mid
dle
-U
pper
Cen
oman
ian
Chry
sali
din
agra
data
Nez
zaza
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nic
aN
ezza
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sim
ple
xN
ezza
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nel
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ard
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adubia
Spir
olo
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Tex
tula
ria
Vid
ali
na
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icae
Cuneo
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pavo
nia
Pse
udorh
apyd
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ala
uri
nen
sis
Pse
udonum
molo
culi
na
Pse
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culi
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mi
Monch
arm
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udocy
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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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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
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600
620
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660
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holo
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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
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YD
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iaci
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BE
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LA
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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.
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CenomanianTuronianConiacianSantonian
Camp.STAGES
INFORMALSUBSTAGES
Alb.
Low.
Mid.
Up.
Mid.
Mid.
Mid.
Up.Up.
Up.
Low.
Low.
Low.
Low.
Up.
Greece
AltıDecrouez
(1982)
Southern
Turkey
Gargouri-
CentralTunisia
Spain-France
(1984)
(Italy)
(1985)
Mesogea
VVlahovic
(1994)
Croatia
Taslı
SouthernTurkey
SouthwesternTurkey
ğları
Saint-Marc
(1981)
Lebanon
CsB1CsB2CsB3CsB4
Sellialveolinaviallii gr.biozone
Brbiozone
oideabiozone
Murge
llalata
biozone
?
C4-1C4-2
C4-3a
C4-3bC5-1C5-2
P.laurinen
sis
Cisalveo
lina
fallax
Hippu
rites
egularisMerlinginaPseudorhapydionina
Pseu
dodo
mia
viallii
Undif ferentiated
Pseu
dorhap
ydionina
Num
moloculine
Ostracoda
and
Miliolidae
P Pand
Peich
eli
and
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simplex
Petacea
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conica
CEN-1CEN-2
C3aC-4CEN-5 B.
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lcan
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()
B.P.
balcan
ica
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Pseudorhapydioninadubia
cenozone
essa
geri
cenozone
Globotruncanidae
Foraminiferal
biozones
Stratigraphic
column
Disconformity
NOTT
Dicarinella
conc
avata
(part)
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asym
etric
a
bivalve
(Toucas).V
preserved
Pelagic
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trun
cana
calcarata
Valvulam
mina
picardi
Num
moloculina
heim
iand
Accordiella
conica
Rotorbinella
scarsellai
and
(1994),
(Italy)
Accordiella
conica
Rotorbinella
scarsellai
and
Nezzazatin
ella
aegy
ptiaca
Num
moloculina
irreg
ularis
cf.and
cf. P
eich
eli
and
P Pand
Ostracoda
and
Miliolidae
P.reicheli-P.dubia
Zone
ensis
Subzone
Subzone
compressa
Poidea
?
Figu
re 1
6.Ch
art s
how
ing
sum
mar
ized
stra
tigra
phic
rang
es o
f sele
cted
ben
thon
ic fo
ram
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r the
per
i-Med
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ous p
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), an
d th
e es
tabl
ished
Upp
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s be
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fora
min
ifera
l bio
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for
the
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he B
ey D
ağla
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rbon
ate
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(tim
e sc
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is ad
apte
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m G
rads
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et a
l. 19
94).
UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP
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D.sc
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Figu
re 1
7.Lo
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enth
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fora
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the
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.
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).
B. SARI ET AL.
413
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
UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP
420
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
UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP
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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
6
7 8 9 10
UPPER CRETACEOUS BENTHONIC FORAMINIFERA FROM THE BDCP
424
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.
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1
2
34
5
6
7
8
9