Late Triassic and Lower Jurassic Foraminifera of the carbonate platform of the Beyaz Aladaǧ Group (Eastern Taurus, Turkey): New stratigraphic implications

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Original

article

Late

Triassic

and

Lower

Jurassic

Foraminifera

of

the

carbonate

platform

of

the

Beyaz

Aladag˘ Group

(Eastern

Taurus,

Turkey):

New

stratigraphic

implications

§

Zeki

U

¨ nal

Yu¨mu¨n

a

,

Ali

Murat

Kılıc¸

b

,

Rossana

Martini

c,

*

,

Jacques

Metzger

c

,

Mahmut

Tunc¸

d

a

EngineeringFaculty,UniversityofNamıkKemal,C¸orluTekirdag˘, Turkey

b_Department_of_Geology,_Faculty_of_Engineering,_University_of_Balıkesir,_Balıkesir,_Turkey

c_Department_of_Geology_and_{Paleontology,}_University_of_Geneva,_13,_rue_des_{Maraıˆchers,}₁₂₀₅_Geneva,_Switzerland d

DepartmentofGeologicalEngineering,UniversityofCumhuriyet,58140Sivas,Turkey

1. Introduction

TheAnatolide-Taurideblock,towhichthestudyareabelongs to, is part of a large platform that shows close stratigraphic analogieswiththe Arabianplatform (Ricou et al., 1975; Ricou, 1980;OkayandTuÿsu¨z,1999;Fig.1). Froma palaeogeographic pointofview,someauthors(Stampfli,2000;StampfliandBorel, 2002;Moix,2010)subdividethecomposite Anatolides-Taurides domainintotwodistinctterranes:theAnatolianandtheTaurus. Basedontheirdifferentgeodynamichistories,theyrecognisethe existence of a common platform from the Upper Triassic. Structurally,the Taurids Alpine chain consists of the so-called Gondwanaderivedparautochthonousnappesthatimbricatewith Neothetyan ophiolite me´lange nappes. The edifice is a conse-quenceofseveral superposednappes,theirfinalshaperesulting fromintensePalaeogenetectonicphases.

ThestudiedareasofYahyalı,Go¨ksunandDeliktas¸arelocatedin EasternTaurus(Fig.2).TheAladag˘ rangecrossesthenearlybarren

plainssouthofYahyalı.EastofAladag˘ range,theCevizMountains arepartoftheAladag˘ tectonicunit(=HadimNappe)thatincludes the Bozkir ophiolite unit and an ophiolitic me´lange under a Tertiary cover(O¨ zgu¨l, 1976).Thestratigraphical and palaeonto-logicalfeaturesoftheLowerMesozoiccarbonateunitsoftheCeviz Mountains(Yahyalı area; Kayseri,east of Aladag˘ range) extend furthereasttotheGo¨ksun(Kahramanmaras¸)andDeliktas¸(Ulas¸ -Sivas)areas(Fig.2).Severalsynchronoustransgressive–regressive eventssuggestcontinuitywithinthestratigraphyofalargezoneof theTauruschain.

Consisting of the Yahyalı-Munzur-Malatya nappes (S¸enel, 1999), the study area wasintenselyinvestigated at the end of the20thcentury(Dag˘er,1975;Aksay,1980;Tekeli,1980;Tekeli andErler,1980;Is¸ık,1981;Tekeli,1981).Blumenthal(1952),and 30 years later Tekeli et al. (1981, 1983), identiﬁed original carbonate units that underwent renewed interest with the investigationoftheGo¨ksunand Deliktas¸regionsbyYu¨mu¨nand Kılıc¸(2006)andthediscoveryofmicrofossils,especiallybenthic Foraminifera,promptingthepresentstudyintheYahyalıarea.The threestudyareasinEasternTauruscoveratotalsurfaceof450km2 (Fig.2).

Themainaimsofthispaperare: ARTICLE INFO

Articlehistory:

Received30October2012 Accepted27May2013 Availableonline29August2013 Keywords: Foraminifera Stratigraphy Triassic LowerJurassic Taurus Turkey ABSTRACT

Foraminiferahave proven tobe reliablebiostratigraphicindicators. Accordingly,Triassicand Early

Jurassic benthic Foraminifera allow usto deﬁne a biostratigraphiczonation within the carbonate

platformofKayseri(Yahyalı),Go¨ksun(Kahramanmaras¸)andSivas(Deliktas¸)regionsintheEastern

Taurus(Ceviz,Aladag˘,KamanandFelfanMountains).Sevennewstratigraphicsectionsaredescribedin

detailandtheﬁrstpreciseinventoryandillustrationofthebenthicforaminiferassemblagesfromthe

Triassicsuccessionsarepresentedoveralargegeographicarea.Thestratigraphicandpalaeontological

features of theLower Mesozoic carbonate unitsof these mountainsinclude several synchronous

transgressive–regressiveeventsthatsuggestcontinuityoftheLowerMesozoicenvironmentsovera

large parautochthonous Taurus zone. Palaeogeographic considerations about the Eastern Taurus

carbonatesaregiven,evidencingthreestagesofdevelopmentunderwentbythestudiedarea:1)astable

continentalmarginfromLowerTriassictoLowerCretaceous;2)adismantlingofthecontinentalmargin

andﬁrstemplacementofophiolitesintheUpperCretaceous;and3)adeformationofthecontinental

marginandemplacementofthePeridotiteNappeintheuppermostCretaceous(Maastrichtian).

ß2013ElsevierMassonSAS.Allrightsreserved.

§

Correspondingeditor:FabienneGiraud-Guillot. * Correspondingauthor.

E-mailaddress:rossana.martini@unige.ch(R.Martini).

Available

online

at

www.sciencedirect.com

0016-6995/$–seefrontmatterß2013ElsevierMassonSAS.Allrightsreserved.

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Fig.1.Tectonicmapofthenorth-easternMediterraneanregionshowingthemajorsuturesandcontinentalblocksandthelocationofthestudiedareas(modiﬁedafterOkay andTu¨ysu¨z,1999).

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topresent sevennewstratigraphicsections, whichhave been measured anddescribedindetail,intheYahyalıarea(Eastern Taurus)thatwasneverinvestigatedindetailbefore;

toprovideandillustratetheﬁrstpreciseaccountofthebenthic foraminiferalassemblagesfromtheTriassicsuccessionsovera largeregioninEasternTaurus,coveringtheYahyalı,Go¨ksunand Deliktas¸areas;

toproposenewstratigraphicpartitionsbasedonbiostratigraphic correlations;

to give palaeogeographic considerations about the Eastern Tauruscarbonates.

2. Materialandmethods

The study material was collected in the Triassic, and subordinately Early Jurassic successions that crop out in the Yahyalı,Go¨ksunand Deliktas¸areas.However,singularemphasis wasconcentratedin thepoorlyknown Yahyalı area. There, the mostwidespreadlithotypesarethecarbonateswithchertlevelsof the newly proposed Aktepe Formation, the platform type carbonatesoftheU¨ çag˘açTepeFormation,theplatformandlagoon carbonatesoftheCevizdag˘ıFormation,andtheshelfcarbonatesof theSırçakLimestone.Verysimilarlithologiesarepresentbothin the Go¨ksun (shelf-type carbonates) and in the Deliktas¸ areas (platform-typecarbonates).

Weperformed amicroscopicanalysis intransmittedlightof aboutthreehundredsamplesfromninestratigraphicsuccessions. Alargenumberofsamplesyieldedwell-preservedand determin-ablebenthic Foraminifera. Thefield survey,including mapping, wasdonebyZ.U.Yu¨mu¨nincollaborationwithA.M.KılıçandM. Tunç;themicropalaeontologicaldeterminationsbyR.Martini,and thecompleteiconographybyJ.Meztger.

3. Results 3.1. Yahyalıarea

IntheYahyalıarea,theseveralparautochthonousnappesthat build up the Eastern Taurus are only represented by the C¸ataloturanNappeat thebase,andtheBeyazAladag˘ Nappeon thetop.FromSouthtoNorth,thesetwoparautochthonousnappes areseparatedandoverlainbytheTethyannappescomprising: theUpperCretaceous(Senonian)Aladag˘ OphioliticMe´langethat

overliestheupperBeyazAladag˘ Nappe;

theMioceneZebilFormation,consistingofconglomeratesand sandstones, thatgenerallyburiestheentiretectonicediﬁcein thisregion.

Plio-QuaternaryglacialdepositsandQuaternaryalluvialcover alsooccur(Figs.3and4).O¨ zgu¨l(1976),dividingtheTaurusZone intotectonic units, includedtherock formationsof theAladag˘ regionintotheAladag˘ Unit.

3.1.1. C¸ataloturanNappe

ThisnappeconsistsoftheUpperPermianArkaççaFormation, concordantly overlain by the Lower Triassic (Olenekian-Lower Anisian) Ku¨çu¨ksu Formation, with the Middle Triassic (Upper Anisian)HorozkayasıDolomiteontop.IntheYahyalıarea,aLate Carboniferous-EarlyPermianhiatusinterrupttheEarly Carboni-ferousdeepwaterfaciessedimentation,afterwhichLatePermian shallowwatercarbonatesedimentationprogressivelystarts.Inthe SWpart,behindtheArkaççaRidge,theArkaççaFormation(Tekeli et al., 1983) (Pa; Figs. 3 and 4; Fig. S1(A), Appendix A) isrepresentedbya500m-thickdarkgreytogrey,mediumto

thick-beddedhard-texturedlimestoneshowingaregressivetrend. Abundant Foraminifera, for example, Paradagmarita monodi, Dagmaritachanackchiensis,Pachyphloiaovataaswellas represen-tativesofthegeneraNankinella,Reichelina,Chusenella,Kahlerina, Globivalvulina, Hemigordius, Dagmarita, Geinitzina, and Algae (Mizzia and Pseudovermiporella) confer an early Late Permian agetotheArkac¸c¸aFormation(Tekelietal.,1981).

Northwest of the study area, concordantly overlying the Arkaçça Formation,the 815m-thick Ku¨çu¨ksuFormation(Trk; Figs.3and4;Fig.S1(A)andcross-sectionC–C’)startswitha1– 1.5m-thicklevelofgrey-lightyellowooliticlimestone.Further up,theformationisrepresentedbyyellowish,greenishgreyto grey,anddarkgreymedium-tothin-thickbeddedalternating marls,claystones and clayeylimestone, endingwith a 10 m-thick light yellow limestone with brownish-grey clay levels. The microfacies of alternating clasticsand carbonates above the oolitic level vary from mudstoneto sandstone and yield abundant ostracod and bivalve shell fragments. Ferruginous cracks may cross the rock. The overall environment shows evaporitic trend from platform to intertidal zone. The Foraminifera Meandrospira pusilla (Fig. S2) and Hoyenella sinensis (Fig. S2) give an Olenekian-early Anisian age to the formation.

Inthesamearea,betweenKu¨çu¨ksuStreamandKu¨çu¨ksuHill, the295m-thick Ku¨çu¨ksuDolomite (Trh;Figs. 3and 4; Tekeli etal.,1983)overliestheKu¨çu¨ksuFormation.Itcomprisesmedium to thick layers of white-grey, light yellow-grey dolomite and dolomitic limestones (Fig. S1(B) and cross-section C–C’). Tekeli et al. (1981) foundtheForaminifera‘‘Trochammina’’ almtalensis (Fig.S3),Endotriadasp.(Fig.S4),Glomospirasp.,Duostominidaeand someInvolutinids,suggestingaMiddle–LateTriassicageforthe succession.

3.1.2. BeyazAladag˘ Nappe

IntheYahyalıarea(CevizMountains),theBeyazAladag˘ Nappe (Ayhan and Lengeranlı, 1986) is composed of a 4000 m-thick carbonatestackofEarlyMesozoicformationsformingtheBeyaz Aladag˘ Group(emend.Blumenthal,1952).Thisgroupissubdivided intofourunits(Tekelietal.,1983,1987):theAktepeFormation (lateAnisian–Carnian)atthebase,followedbytheU¨ çag˘açTepe Formation (mostlyNorian), theCevizdag˘ıFormation(Rhaetian), andtheSırçakLimestone(Jurassic-EarlyCretaceous)ontop.Itis worth noting that Yu¨mu¨n (2005) raised the Beyaz Aladag˘ Formation of Blumenthal(1952) totherankof a groupon the base of lithological,sedimentological, palaeontological and tec-tonicfeatures,togetherwiththeimportantarealdistributionofthe Beyaz Aladag˘ Formation. This author also renamed the Beyaz Aladag Formation of Tekeli et al. (1983) as the U¨ çag˘aç Tepe Formation, after the homonym type locality in the Ceviz Mountains.

ThetypesectionoftheherenewlyproposedAktepeFormation (Tra;Figs.3and4)isatCinnikoyaklar,southofAktepe,20kmouter thesouthwestcorner ofthe studyarea (Kozansheet 1/25.000-M34-b1).SectionL–L’(Figs.3andS5),cropsoutbetween37857’ 32’’N/35822’05’’Eand37857’12’’N/35823’44’’E,strikingN878W, along the2490 m-longnorthern slopesof theEmli Strait. The formation consists of carbonates with cherts, formerly called ‘‘Teknepınar Flysch’’ by Blumenthal (1952); it is lithologically different from the overlying U¨ c¸ag˘ac¸ Tepe Formation which representsthemainbodyoftheBeyazAladag˘ Group.

TwoauxiliarysectionsoftheAktepeFormationareatAktepe andatÇamyoluHill(Fig.3;cross-sectionC’–C’’).Thefirst(Aktepe; Kozansheet1/25.000-M34-b1),locatedbetween37858’05’’N/358 22’40’’Eand37858’18’’/35823’45’’E,strikingN858W,is2315 m-long. (Fig.S6(A) and cross-sectionC’–C’’). Thesecond(Çamyolu Hill;Kozansheet1/25.000-M34-b1)isbetween37857’32’’N/358

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20’41’’Eand37857’ 59’’N/35824’20’’E,strikingN858W,and measure4180m(Fig.S6(B)andcross-sectionC’–C’’).

The lower contact to both the Horozkayasi Dolomite (Trh; Fig.3)andtheAladag˘ OphioliticMe´lange(Kra;Fig.3)istectonic. TheuppercontactwiththeU¨ çag˘açTepeFormationisconcordant andtransitional.TheAktepeFormationhasanaveragethicknessof 1150m. However,it canvaryduetothetectonicnatureof the exposures.Itmostlyconsistsofmedium-thickbedsoffairlyfine andlocallydolomiticlimestone,withintercalatedlevelsofcherts. The colour is light and dark beige, grey and yellow. The microtexture is clastic, consisting of extra- and intraclasts, togetherwithpeloidsand skeletalfragments(e.g.,Foraminifera, Ostracods, Bivalves, Echinoids, Algae) in a sparry calcite or neomorficsparry calcite cement.In theuppermostbeds of the formationtheincertaesedisMicrocodiumoccurs.

The lithologies alongside the microfacies indicate an evolution of the depositional environment from basin to platform, as conﬁrmed by the presence of microcodiaceans (Microcodium),indicatingashallowmarinesetting(Nassichuk et al., 1986). Based on the presence of rich and diversiﬁed associationsof Foraminifera(seeSection3.4.;Figs. S2–S4,S7, S8), a Middle-Late Triassic (Late Anisian-Carnian) age is assignedtotheAktepeFormation(Rettorietal.,1994;Broglio Lorigaetal.,1999).

Fromalithologicpointofview,theAktepeFormationcanbe comparedtotheTeknepınarFormation,whichisexposed south-west of thestudyarea, although its deposition tookplacein a shallower environment (i.e., on the coastal region of the shelf insteadofinanopenseaasfortheTeknepınarFormation,formerly named‘‘TeknepınarFlysh’’).

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3.1.3. BeyazAladag˘ Nappe-Aladag˘ TepeFormation

TheU¨ c¸ag˘ac¸TepeFormation(Tru;Figs.3and4)isthenewname proposed here for the Beyaz Aladag˘ Formation of Tekeli et al. (1983), as this last is erected to the rank of group. This new formationisnamedafterthehomonymtypelocalityintheCeviz Mountains(Figs.S9(A)andcross-sectionB–B’,S10(A)and cross-sectionA–A’,S11(A)andcross-sectionE–E’).Accordingtoprevious

studies,theU¨ c¸ag˘ac¸cagacTepeFormation(=BeyazAladag˘ inTekeli etal.,1983,1987)consistsofLateTriassic(Norian),greyishyellow toyellow-darkbeige,medium-thickbeddedplatform-type carbo-natescontainingtheAlgaeGriphoporellacurvataand Thaumato-porellaparvovesiculifera. Texturaldifferencesoccur in thelower andupperlevels.Thelowerlevelsarecharacterisedbyincreasingly neomorphicsparrycalcite,andpoorly-washedbiosparitewithfew

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Foraminiferaand Algae.The micrite generally contains pellets, which in upper levels turns to biomicrite withpellets. On the contrary, these levels contain relatively abundant Foraminifera andAlgae(seeSection3.4.;Figs.S2–S4,S8,S12,S14).Basedonthe micropalaeontologicalcontent,theageintervaloftheU¨ c¸ag˘ac¸Tepe FormationisNorian–Rhaetian.

3.1.4. BeyazAladag˘ Nappe-Cevizdag˘ıFormation

NamedaftertheCevizMountain(Kozansheet 1/25.000-M34-b2),thisunit consistsofuppermostTriassic(Rhaetian)platform andlagooncarbonates.TheCevizdag˘ıFormation(Yu¨mu¨n,2005) (Trc;Figs.3and4)iswellexposedintheupperslopesoftheCeviz rangethatstretchesinSW–NEdirectionacrossthesouthwestof thestudyareaand,furthernorth,inthewesternpart.Italsobuilds up the north-eastern slopes of the Sırc¸ak Mountain and the Gu¨venolug˘uHill(Kozansheet1/25.000-M34-b2),whichispartof theHorozMountain(Fig.3).TheCevizdag˘ıFormationalsocrops outattheKuskayasiHill(Kozansheet1/25.000-M34-b1)in the west.Atotalareaof20km2_in_the_study_area_consists_of_this_unit

thatspreadswiderwest,outsidethestudyarea.

ThetypesectionoftheCevizdag˘ıFormationislocatedinthe U¨ çag˘açHill(Kozansheets1/25.000-M34-b1andM34-b2).The 2925 m-long stratigraphic cross-section (Figs. 3, S10(B) and cross-sectionA–A’)wasmeasuredatU¨ çag˘açHill,between378 54’40’’N/358210 _30’’_E_and₃₇₈_53’_20’’_N/358_23’_13’’_E,_in_a

N608Wdirection.

Three auxiliary sections of the Cevizdag˘ı Formation were measuredattheU¨ çag˘açkırıHill,HorozMountainandOrtaçalHill, respectively.Thefirstone,2737.5m-long,issituatedintheCeviz Mountain(Kozansheet1/25.000-M34-b2),coordinates37855’23’’ N/35824’50’’Eand37854’05’’N/35824’11’’E,strikingN228W (Figs.3,S11(B)andcross-sectionE-E’).Thesecondone,2312.5 m-long,isfromtheHorozMountain(Kozansheet1/25.000-M34-b2) between37857’55’’N/35824’29’’Eand37856’53’’N/35825’26’’E, strikingN408W (Figs. 3,S9(B) and cross-section B–B’).The last section,5937.5 m-long, is south ofthe OrtaçalHill(Kefenalan; Kozansheet1/25.000-M34-b2),between37856’57’’N/35821’52’’ Eand37855’52’’N/35825’43’’E,strikingN708W(Figs.3,S13(A) andcross-sectionD–D’).

ThelowercontactwiththeU¨ çag˘açTepeFormationismarkedby a sudden change in lithology (Fig. S11) resulting in a steeper topography.TheuppercontactwiththeoverlyingSırçakLimestone isconcordant andtransitional;itencompasses acolour change, whichbecomes muchclearer, andan increaseof thelimestone hardness.TheCevizdag˘ıFormationhasanevaluatethicknessfrom 386and550m,accordingtothelocalitieswhereitcropsout.The successioniscomposedofmedium–thickbedded(2–5m) lime-stones;inthelowerparttheyaredarkbeige-brownyellow,getting lighterupwards.Microtexturevariesfrommudstone-wackestone to boundstone in the lower part of the series, to bioclastic wackestone towards the upper part. The components mainly consistofbioclasts,especiallyForaminiferaandMicrogastropods, togetherwiththeAlgaeMacroporellareticaandThaumatoporella parvovesiculifera(seeSection3.4.;Figs.1–3).A smallamountof intraclastsandpelletsalsooccur.Megalodontbivalves occasion-allyalsooccur.Thecementisofmicrocrystallinecalciteduetoa lowmetamorphism.

Themicrocomponentsclearlyreﬂectthestandardpropertiesof ashallowwaterenvironment(Wilson,1975)thatevolves,fromthe lowertotheupperpartoftheformation,intoarestrictedplatform orlagoon.Probablythesedimentationtookplaceabovethestorm wave base. Oolitic limestone in the basal levels of the Sırc¸ak Limestone,thatconcordantlyoverlietheCevizdag˘ıFormation,isa furtherimportantindicatorforshallowingconditionstowardsthe top of the Triassic. The foraminiferal associations indicate the uppermostNorian(Sevatian)toRhaetianbasedonthepresenceof

theforaminiferindexTriasinahantkeniandtheAlgaeMacroporella retica.

TheCevizdag˘ıFormationiscomparabletothelowerKurudere memberoftheMunzurLimestone,deﬁnedbyO¨ zgu¨l(1983)inthe Felfan Mountains, and with the middle part of the Andırın LimestoneintheKamanMountains.Thesethreeseriesallconsist ofshallowwatercarbonateswithAlgaeandmegalodonts,passing upwardstotheLowerJurassic(Liassic)SircakLimestone. 3.1.5. BeyazAladag˘ Nappe-Sırc¸akLimestone

Tekelietal.(1983)namedtheshelfcarbonatesthatformthe uppermostpartoftheBeyazAladag˘ NappeastheSırçakLimestone (JKrs;Figs.3and4).ItcropsoutinthesouthernpartoftheSırçak Mountain,EastoftheAladag˘ range(Eastern Taurus)and inthe southernslopesoftheCevizMountain(Fig.3).Weprecisethatthis last outcropwas first included in the BeyazAladag˘ Formation (=U¨ çag˘açTepeFormationinthiswork)byBlumenthal(1952).

TheSırc¸akLimestonerestsontheUpperTriassic(uppermost Norian to Rhaetian) Cevizdag˘ı Formation concordantly and transitively.TowardssouthitiscoveredbytheUpperCretaceous Aladag˘ OphioliticMe´lange,andtosoutheast and northeastitis overlainbytheMioceneclasticrocksoftheZebilFormationwith anangulardiscordance(Figs.3and4).

The succession is composed of light yellow-light beige, medium-thickbeddedhard-texturedlimestone.Themicrotexture of the biomicritic Sırçak Limestone is principally packstone, subordinately grainstone, with Foraminifera, Bivalves and the AlgaeThaumatoporellaparvovesiculifera(seeSection3.4.;Figs.S3 andS14);fewpelletsandintraclastsalsooccur.Inthelowerbeds, ooliteshavebeenobserved(Fig.S13(B)andcross-sectionD–D’). Upwards,recrystallizationincreasesduetoalowmetamorphism. The depositional environment matches to facies zone 7 of Wilson(1975), showing that initially sedimentationtook place mainlybelowstormwavebase,andthenenvironmentshallows towardsthetop.Moreover,theoolitictexturefoundatthebaseof the Sırçak Limestone clearly indicates the general shallowing-upwardtrendthataffectsthesequencesinthewholestudyareaat theendoftheTriassic.AlthoughinthepreviousstudiesaJurassic– Early Cretaceous age assignment was proposed for the Sırçak Limestone,anearlyLiassic–LateCretaceousageisproposedhere accordingtotheForaminiferaandAlgae.

3.2. Go¨ksunarea

In the Go¨ksun area (Fig. 5), the Go¨ksun Ophiolite (Upper Cretaceous)representsthebaseofa stackofsevensedimentary units,eachotherseparatedby tectonicunconformitiesshowing angular discordances. The four lower units are the Palaeozoic YoncayoluFormation,theUpperPermianÇayderesiFormation,the LowerTriassicAlicliFormation,andtheUpperTriassicÇamdere Formation. These units form the Keban-Malatya Group; it is discordantlyfollowedbytheAndırınLimestone(UpperTriassicto LowerCretaceous),theUpperMioceneSalyanFormation,andby thePlioceneNadirFormation(Yu¨mu¨nandKılıç,2002).Thewhole sequence of tectonically independent sedimentary units lies buried under Quaternary alluvium (Fig. 6). Lithologically, the Upper Triassic successions of theKeban-Malatya Group in the Go¨ksunarea,brieflydescribed below,areclosely comparableto thoseoftheBeyazAladag˘ GroupintheYahyalıarea.

3.2.1. C¸amdereFormation(Keban-MalatyaGroup)

Outcropping in the northeast part of the Goksun district (Kahramanmaras),theC¸amdereFormation(Trc)mainlyconsistsof locallyrecrystallizedlimestones(Fig.S15andcross-sectionA–A’). BivalveshellfragmentsandForaminifera(seeSection3.4.)have beenmentionedinthissuccessiontogetherwiththedasycladale

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Clypeinabesici(Yılmazetal.,1993).Accordingtothefossiliferous content, the age of the Çamdere Formation is Late Triassic. ThereforeUpperTriassiclevelsarepresentintheKeban-Malatya Unit.Itis worthnotingthattheÇamdere Formationwasfirstly namedasPalaeozoicmarbleintheMalatyaMetamophic.Lateron, itwasaddedtotheÇayderesiFormationbyYılmazetal.(1993)and morerecently,ithasbeennamedasÇamdereFormationbyYu¨mu¨n andKılıç(2002)fromtheÇamderevillageofGo¨ksun.

3.2.2. AndırınLimestone

The Upper Triassic–Jurassic shelf-type carbonates of the AndırınLimestone(Mza)cropoutinthesouthandsoutheastof theGo¨ksundistrict(Kahramanmaras¸).Inthelower-middlepartof the succession, the thick layers of grey-beige limestones and cherts, locally recrystallized, contain a rich and diversiﬁed association of Foraminifera (see Section 3.4.), along with the Algae Thaumatoporella parvovesiculifera and rarer megalodont shells. Upwards, the limestone becomes light yellow and biomicriticwithrelativelyabundantmegalodontshellsandfew Foraminifera,suggestingashallowingtrend.Ooliticlevelsalso occur, especially in the Jurassic upper part of the succession. AccordingtoYu¨mu¨nandKılıc¸(2006),themicropalaeontological

associationconfersaLateTriassictoJurassicagetotheAndırın Limestone(Fig.6).

Lithologically,thisunitresemblestheupperpartoftheSırc¸ak Limestone(Yahyalıarea;BeyazAladag˘ Nappe)andtheupperlevels oftheMunzurLimestone(Deliktas¸area;Ulas¸-Sivasregion).The shallowingthatoccursineachofthethreeseries(Yahyalı,Go¨ksun and Deliktas¸) is interpreted as a feature related to the Upper Triassic-Lower Jurassic transition,suggesting theexistence ofa regionalindicatorofthecarbonatesedimentationwithinasingle largebasin.ItisworthnotingthatoriginallytheAndırınLimestone wasnamedAndırınCarbonatesbyAyas¸og˘lu(1970),Pampaland Kurtman(1983)and Perinc¸ekand Kozlu(1983)referring tothe carbonaterockspresentinthesouthwestpartofthestudyarea. 3.3. Deliktas¸area

East of Deliktas¸, southeast of Ulas¸ (Sivas), raise the Felfan Mountains, fashioned by a tectonic stack of several tectonic elements (Fig.7). Atthebase,thepilestartswiththe Permian-Lower Cretaceous Munzur Limestone (Mzm), lying under the Upper Cretaceous Yes¸iltas¸yayla Me´lange (Ky), a polymictic me´lange in a clastic matrix. A north-plunging tectonic contact Fig.5.GeologicalmapoftheGo¨ksunareashowingthelocationofthemeasuredsection(A-A’)(modiﬁedafterYu¨mu¨nandKılıc¸,2002).

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separatestheYes¸iltas¸yaylacomplexfromtheoverlying serpenti-nite,peridotite, gabbro,pyroxenite, verliteandlherzoliteof the CretaceousGu¨nes¸Ophiolite(Kg).Anangularunconformitydivides thelatterfromtheoverlyingOligocene-Miocenesandstone,clayey limestone,marls,lacustrinelimestoneandﬁne-layeredlimestone oftheAltınyayla(Ta)andKulmac¸dag˘ıformations(Tk).Finally,an angularunconformity underlies theUpper Pliocene–Quaternary polygenicgravelsandblocksoftheO¨ renliceFormation,allburied underQuaternaryalluvium(Fig.8).

Exposed20km southeastof Ulas¸(Sivas),Munzur Limestone consistsofPermian–LowerCretaceousplatform-typecarbonates. NamedaftertheMunzur Mountainsby O¨ zgu¨l etal. (1981),the MonzurLimestonewasalreadyobservedbyAktimuretal.(1988, 1990)intheSivasarea.AjuniorsynonymoftheMunzurLimestone isYılanlıdag˘ Formation(Go¨kten,1993).

InthisworkweonlyconsidertheNorian–Rhaetianportionofthe MunzurLimestone(Fig.S16).Thesuccessionstartswithapinkishto grey, thick-bedded or massive hard-textured, megalodont Fig.6.CompositestratigraphicsectionoftheGo¨ksunarea(modiﬁedafterYu¨mu¨nandKılıc¸,2002).

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shell-bearinglimestone,locallydolomitized.Levelsrich in echino-dermsandcoralsalsooccur.Recrystallizedcalciteinﬁllingsandcalcite veinsﬁllupkarsticcavities atmicro-andmacro-scales. Frequent changes in colour typify this limestone. The middle part of the successionisfairlycharacterisedbyaveryhard-textureddarkgrey limestone,havingrecrystallizedkarsticcavitiesandjoints.Intheupper

part, a light grey, thick-bedded hard-textured limestone, slightly recrystallized,yieldraremegalodonts.

Overall,themicrofaciesoftheMunzurLimestonepassesfrom micriteatthebasetomicrospariteupwards.Granularcomponents aremainlyrepresentedbyvariousbioclastsandintraclastsaswell assmallamountsofpelletsandlithoclasts.Foraminiferaalsooccur; Fig.7.GeologicalmapoftheDeliktas¸area(modiﬁedafterYu¨mu¨nandKılıc¸,2006).

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however,strongrecrystallizationpreventstheiraccurate determi-nation(seeSection3.4.).Thedeepermarineenvironment ofthe micrite seems to become shallower upwards, recalling similar featuresofthe AndırınLimestone (Go¨ksun area; Keban-Malatya Group)andtheCevizdag˘ıFormation(Yahyalıarea;BeyazAladag˘ Nappe),oncemoresuggestingsimilardepositionalconditionsofthe carbonatesofthethreestudyareaswithinthesamebasin.

3.4. Foraminiferassociations

IntheTriassicandEarlyJurassicsuccessionsoftheBeyazAladag˘ Nappe,intheYahyalıarea,arichandwell-preservedassemblageof benthicForaminiferahasbeenidentified.Verysimilar foraminif-eralassociationshavealsobeenfoundinthecoevalsuccessionsof the Keban-Malatya and Munzur nappes, in the Go¨ksun and Fig.8.CompositestratigraphicsectionoftheDeliktas¸area(modifiedafterYu¨mu¨nandKılıç,2006).

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Deliktas¸areas,respectively.Theseassociationsarereportedbelow, instratigraphicorder,forthethreestudyareas.

3.4.1. Yahyalıarea

ThemicrofaunacharacterisingtheAktepeFormationismainly composed of: Agathammina austroalpina Kristan-Tollmann and Tollmann,1964(Fig.S4),Aulotortusexgr.sinuosus(Weynschenk, 1956) (Figs. S2 and S7), Diplotremina astroﬁmbriata Kristan-Tollmann, 1960 (Fig. S4), Diplotremina cf. D. astroﬁmbriata Kristan-Tollmann,1960, Endotriadakuepperi(Oberhauser,1960) (Fig. S8), Endotriadella wirzi (Koehn-Zaninetti, 1968) (Fig. S8), Endotebaexgr.controversaVachardandRazgallah,1988(Fig.S8), Endotebanella kocaeliensis (Dager, 1978), Endotebanella cf. E.tricamerata (Salaj, 1967)(Fig. S8),‘‘Trochammina’’ almtalensis Koehn-Zaninetti,1969,Agathamminaspp.(Fig.S4),Ophthalmidium spp.(Fig.S3),Endotebanellaspp.(Fig.S8),Endotriadaspp.(Figs.S4 andS8),Milioliporidae(Fig.S3),andLagenida(Fig.S3),providinga LateAnisiantoCarnianage.

ThemiddlepartoftheU¨ çag˘açTepeFormationyields:Auloconus permodiscoides (Oberhauser, 1964) (Fig. S7), Aulotortus ex gr. sinuosus(Weynschenk,1956)(Fig.S7),Aulotortusfriedli (Kristan-Tollmann, 1962) (Fig. S2), Agathammina austroalpina Kristan-TollmannandTollmann,1964,Nodosariacf.N.ordinataTrifonova, 1965,?MilioliporacuvillieriBronnimannandZaninetti,1971(Fig. S12),Endotebaexgr.controversaVachardandRazgallah,1988(Fig. S8),Auloconus spp.,Aulotortus spp.,Gandinellasp. (Fig. S3),and Glomospirellaspp.,withrepresentativesofLagenidaand Textular-idae(Fig. S14). The AlgaeGriphoporellacurvata(Gu¨mbel, 1872) (Fig.S4)andThaumatoporellaparvovesiculifera(Raineri,1922)(Fig. S4) are alsopresent. The co-occurrence of Auloconus permodis-coides,Aulotortusexgr.sinuosusandAulotortusfriedliaswellas their relative abundance indicate a Norian-Rhaetian age. The presencewithinthelowerpartoftheU¨ çag˘açTepeFormationof Griphoporella curvata, which is restricted to the Norian, char-acterisesthe‘‘GriphoporellacurvataAcmeZone’’(Mancinellietal., 2005).

The end of the Triassic succession is represented by the Cevizdag˘ı Formation, bearing a well-preserved and diversiﬁed microfaunathatincludestheforaminiferindexTriasinahantkeni Majzon, 1954 (Fig. S12) along with Auloconus permodiscoides (Oberhauser, 1964) (Figs. S7 and S12), Aulotortus communis (Kristan,1957)(Fig.S2),Aulotortusexgr.sinuosus(Weynschenk, 1956) (Fig. S7), Nodosaria ordinata Trifonova, 1965 (Fig. S3), Auloconusspp., Aulotortus spp., representatives ofLagenida and Textularidae,aswellastheAlgaeMacroporellareticaZanin-Buri, 1965andThaumatoporellaparvovesiculifera(Raineri,1922).While AuloconuspermodiscoidesandAulotortuscommunishavea Norian-Rhaetian range, Triasina hantkeni is conﬁned tothe uppermost Norian(Sevatian)toRhaetian,andMacroporellareticaisrestricted totheRhaetian.Thus,thisassociationperfectlymatcheswiththe ‘‘TriasinahantkeniRangeZone’’(Mancinellietal.,2005).

ThelowerpartoftheSırçakLimestone,whichconcordantlyand transitivelyoverliesthe(uppermostNoriantoRhaetian)Cevizdag˘ı Formation,contains:Mayncinacf.M.termieriHottinger,1967(Fig. S14),Orbitopsellapraecursor (Gu¨mbel,1872)(Fig.S14), Siphoval-vulinaspp.(Figs.S3andS14),Textularidae(Fig.S14),togetherwith Thaumatoporellaparvovesiculifera(Raineri,1922).Thisassociation pointstoanearly–middleLiassicage.However,consideringthe presenceofOrbitopsellapraecursorintheSırçakLimestone,aswell as its stratigraphic distribution confined to the Pliensbachian (Septfontaine,1984;Septfontaineetal.,1991),ayoungeragefor thisformationisnotexcluded.

3.4.2. Go¨ksunarea

TheForaminiferafromtheLateTriassicsuccessioninGo¨ksun (Keban-MalatyaNappe)arepoorcomparingtothecoevalonein

theYahyalıarea(BeyazAladag˘ Nappe).IntheC¸amdereFormation only Aulotortidae have been found, that is, Aulotortus ex gr. sinuosus Weynschenk, 1956, and Aulotortus friedli (Kristan-Tollmann, 1962). Therefore, the formation is attributed to an undifferentiatedUpperTriassic.

Surprisingly, the overlying Andırın Limestone yields, in its lower and middle part, relatively abundant Foraminifera, for example,Aulotortusfriedli(Kristan-Tollmann,1962),Endotriadella wirzi (Koehn-Zaninetti, 1968), Ophthalmidium spp., Variostoma spp., Aulotortus spp., as well as representatives of thefamilies Lagenida, Milioliporidae and Trochamminidae. Protopeneroplis striataWeynschenk,1950,OphthalmidiidaeandValvulinidaehave beenfoundintheupperpartoftheAndırınLimestone.According toYu¨mu¨nandKılıc¸(2006),thisforaminiferalassociationconfersa LateTriassictoJurassicage.

3.4.3. Deliktas¸area

Inthisarea,theUpperTriassic–JurassicportionoftheMunzur Limestone contains relativelyabundant Foraminifera. However, theyareoftenstronglyrecrystallizedanddeterminationsatthe speciﬁc level remain highly speculative. Based on the general morphologiesandsizes,representativesofthefamilies Aulotorti-dae,Triadodiscidae,Duostominidae,Milioliporidaeand Trocham-minidaehavebeenconﬁdentlyrecognised.

4. Discussionandconcludingremarks

4.1. TriassicenvironmentsandTriassic-Jurassiccontinuity

Sedimentological and biostratigraphic study of the Lower Mesozoicsuccessionsof theBeyazAladag˘ Groupin theYahyalı area(EasternTaurus),andtheircomparisonwithcoevalseriesin theGo¨ksun(Keban-Malatyagroup)and Deliktas¸(Munzur Lime-stone)areas,clearlyindicatethattheMiddle–LateTriassicAktepe Formation deposited in a single large basin including deep to platformenvironments.TheupperpartoftheAktepeFormation contains quite abundant Algae Microcodium suggesting that a shallowenvironmentnearwatersurfacetookplacemostprobably closetotheCarnian–Norianboundary.Thisdatumiscorroborated bytheupto500m-thickNorianbasalpebbleunitoftheU¨ çag˘aç TepeFormation(O¨ zgu¨l,1983).Higher,thesuccessionevolvesinto platform-type carbonates with abundant and well-preserved Foraminifera,correspondingtotheNorian‘‘Aladag˘ fauna’’inthe literature, whilst shallow water to lagoonal carbonates with Foraminifera and Algae characterise the Rhaetian Cevizdag˘ı Formation. TowardstheupperpartoftheCevizdag˘ı Formation, thetransitiontotheshelfcarbonatesoftheLowerJurassicSırçak Limestone is smooth. These depositional conditions are then maintained all alongtheLower Jurassic,exceptsomelocal and shortdeepening.

O¨ zgu¨l(1983) comparedtheMiddle toUpper Triassic–Lower Jurassic successions from this study to coeval sections in the Aladag˘ andBolkarMountainunits.TheAladag˘ Nappe,startingwith LowerTriassicstromatoliticandooliticlimestones,consistshigher upofturbiditesupto1000minthickness,followedbyAnisian carbonateserieswithplantfragments.AbovetheseAnisianunits discordantly follow Carnian–Norian conglomerates, while the Rhaetian–Liassictransitionisconcordant.However,inhis general-isedcolumnarsectionoftheAladag˘ unit,O¨ zgu¨l(1997)recognised noLadinian–CarnianintervalwithintheTriassicGevneFormation (O¨ zgu¨l,1976).ThediscoveryofLadinianandCarnianintheAktepe Formation (this work) modiﬁes our viewpoint of the general character of the Aladag˘ unit. Accordingly, the depositional environment of thecarbonates in this unit deepens from west toeast.

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Togetherwithﬁelddataandforaminiferalcontents,allthese observationsclearlyshowthat:

the stratigraphic and palaeontological features of the Lower MesozoiccarbonateunitsoftheCevizMountains(Yahyalıarea; Kayseri,eastofAladag˘ range)extendfurthereasttotheGo¨ksun (Kahramanmaras¸)andDeliktas¸(Ulas¸-Sivas)regions(Fig.2); several synchronous transgressive–regressive events suggest

continuitywithinthestratigraphythatcoversalargezoneofthe Tauruschain;

no interruption of sedimentationaffectedthe carbonate plat-form.Indeed,thewidelyoccurringooliticlevelsandtherelative abundanceof Algae(e.g.,Thaumatoporella parvovesiculifera)in the middleLiassic prove that a shallowingenvironment took placeatthattimebutnoapparenthiatusoccurred.

4.2. PalaeogeographicconsiderationsabouttheEasternTaurus carbonates

Following the literature, Turkeyconsists of six major litho-sphericfragments:theRhodope-Strandjablock,theIstanbulzone, theSakaryazone,theAnatolide-Taurideblock,theKırs¸ehirMassif, andtheArabianPlatform(Fig.1;S¸engo¨randYılmaz,1981;S¸engo¨r etal.,1982;Okayetal.,1994;OkayandTuÿsu¨z,1999).Thefirst threezonesclearly showLaurasianaffinitiesand areclassically referred to as the Pontides. Boundaries are the Izmir–Ankara– ErzincansuturebetweentheKırs¸ehirMassifandtheAnatolide– Taurideblock.ThislatterisincontactwiththeArabianPlatform alongtheAssyrian–Zagrossuture.Althoughseparatedfromitby this suture, the Anatolide–Tauride block shows a Palaeozoic stratigraphysimilartothatoftheArabianPlatform,andhenceto thenorthernmarginofGondwana.

The Kırs¸ehir Massif, which mainly consists of Cretaceous metamorphic and granitic rocks, is in contact along the con-troversialIntra-TauridesSuture(ITS)withtheAnatolide–Tauride block,whiletheIntra-PontidesSuture(IPS)constitutestheformer plateboundarybetweentheSakaryaandtheIstanbulzones(Okay and Tu¨ysu¨z, 1999). For S¸engo¨r and Yılmaz (1981), Neotethyan ophiolites mark sutures that bound blocks, continents and platforms.

ThestudyarealiesintheAladag˘ range,inthewesternpartof the Eastern Taurus belt, where the following three stages developed:

stable continental margin from Lower Triassic to Lower Cretaceous;

dismantlingofthecontinentalmarginandﬁrstemplacementof ophiolites(UpperCretaceous);

deformationofthecontinentalmarginandemplacementofthe PeridotiteNappeintheMaastrichtian(Tekeli,1980).

Duringthestableperiod,carbonateplatformdepositionstarted in the Eastern Taurus from the Upper Anisian and may have extended until the Lower Cretaceous. During this timespan, carbonate deposition encompasses three phases of platform evolutionintheAladag˘ range,spacedbytwointervalsofshallow waterconditions(attheCarnian–Norianboundaryandbetween the Rhaetian and the middle Liassic, respectively) to non-deposition(middleLiassic-Dogger).

In the Lower Triassic, a huge platform extended from the ArabianplatetothesouthernedgeofthePaleotethysOceanuntil theUpperTriassicclosureofthislatter.Thisplatformincludedthe carbonates of the Eastern Taurus of the northern side of Gondwana.SimultaneouslytheopeningoftheNeotethyscaused thedetachmentofGondwanianfragments,leavinghoweverthe

sedimentationareaoftheEasternTauruswithintheGondwana shelf, as witnessed by the Lower Jurassic microfacies with foraminiferalikeOrbitopsellapraecursor,typicalforthesouthern TethyanshelfofGondwana.

TheﬁrstshallowingstageneartheCarnian–Norianboundary may bein unisonwith a global eustatic cycle and, during the Norian,platformconditionsprevailed.Duringthesecond shallow-ing stage at the Rhaetian–Liassic transition, the increasing of Foraminifera and the widespread distribution of the Algae Macroporella reticacharacterise theRhaetian. IntheLiassic, the Thaumatoporella parvovesiculifera peak and several oolitic lime-stone levels characterize the Eastern Taurus Lower Jurassic microfacies. Finally, the Late Cretaceous ophiolites and the Alakırc¸ayserpentinite-gabbroMe´lange becameimbricatein the Eastern Taurus carbonate stacks during Palaeogene tectonic phases.

Acknowledgments

WethankProf.FrancisHirsch(NarutoUniversity,Japan)andDr. Yavuz Bedi (General Directorate of Mineral Research and Exploration,Turkey)fortheirkindhelpanddiscussions through-outthisproject.ThisstudywaspartlysupportedbytheNational SwissScienceFoundationgrant200020-137661toR.M.Reviewers, Profs.S.O¨ zerandR.Rettori,aswellastheeditors(G.Escargueland F.Giraud-Guillot),arethankedfor theirhelpfulsuggestionsand comments,whichgreatlyimprovedthismanuscript.

AppendixA.Supplementaryinformation

Supplementaryinformation(Figs.S1–S16,including stratigra-phicsections, measured cross-sections and foraminifer illustra-tions) associated with this article can be found, in the online version,at:http://dx.doi.org/10.1016/j.geobios.2013.05.002. References

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