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Late Devonian Conodont Fauna of the Gümüflali Formation

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Late Devonian Conodont Fauna of the Gümüflali Formation TurkishJournalofEarthSciences (TurkishJ.EarthSci.),Vol.9, 2000,pp.69-89. Copyright©TÜB‹TAK LateDevonianConodontFaunaoftheGümüflali Formation,theEasternTaurides,Turkey fiENOLÇAPKINO⁄LU&‹SMETGED‹K KaradenizTeknikÜniversitesi,JeolojiMühendisli¤iBölümü,TR-61080Trabzon,TURKEY (e-mail:[email protected]) Abstract: TheLateDevonianGümüflaliformationoftheeasternTauridesisaterrigenous-carbonaterocksequence about600mthick,consistingmainlyofquartzsandstone,quartzsiltstone,shale,andcarbonaterocks. Palaeontologicandsedimentologicdatamainlyindicateashallowsubtidaldepositionalenvironment.Thissequence generallyrepresentstheshallow-waterpolygnathid-icriodidbiofacies,andcontainsconodontfaunasthatrange fromtheUpperfalsiovalis ZoneintotheUpperpraesulcata Zone.However,theydonotcorrelatewelltotheLate Devonianstandardconodontzonationbecauseofthelackofzonallydiagnosticspeciesandtheirregularvertical distributionsofthepresenttaxa.Herein,54taxabelongingtoninegeneraaredescribedandillustratedfromthe studiedsection.Icriodusadanaensis,Icriodusfekeensis,andPolygnathusantecompressus arethenewlydescribed species. KeyWords: LateDevonian,conodont,Gümüflaliformation,easternTaurides,Turkey. GümüflaliFormasyonu’nun(Do¤uToroslar,Türkiye)GeçDevoniyen KonodontFaunas› Özet: Do¤uToroslarboyuncayayg›nyüzeylemeleriolanGeçDevoniyenyafll›Gümüflaliformasyonu,yaklafl›k600 metrekal›nl›¤aulaflanbirk›r›nt›l›-karbonatkayadizisidir.Litolojisinibafll›cakuvarskumtafl›,kuvarsmiltafl›,fleylve karbonatkayalar›n›noluflturdu¤ububiriminpaleontolojikvesedimantolojiközellikleri,çökelmeninbafll›cas›¤,gel- gitalt›ortamdageliflti¤ineiflareteder.Konodontfaunas›genelliklek›y›-yak›n›polygnathid-icriodidbiyofasiyesini temsileder,veÜst falsiovalis Zonu’ndanÜstpraesulcata Zonuiçinekadaruzananbiraral›¤›temsileder.Bununla beraber,zonbelirleyicitaksonlar›nyoklu¤uvemevcuttaksonlar›ndüzensizdikeyda¤›l›m›ndandolay›,Geç Devoniyenstandardkonodontzonlamas›iletambirkorelasyonsa¤lanamam›flt›r.‹ncelenenstratigrafikkesitteki kireçtafl›katmanlar›ndanal›nan107örnekten,9cinseaittoplam54türvealttürtan›mlanm›flt›r.Tan›mlanan taksonlardan3tanesi( Icriodusadanaensis n.sp.,Icriodusfekeensis n.sp.ve Polygnathusantecompressus n.sp.) yenitürdür. AnahtarSözcükler:GeçDevoniyen,Konodont,Gümüflaliformasyonu,Do¤uToroslar,Türkiye. Introduction northeastofthetownofFeke,Adana(Turkey),onthe Conodontbiostratigraphyisoneofthemostimportant 1/25.000KozanM35-b2topographicmap,andcrops toolsinthecorrelationofPalaeozoicandTriassicrockson outalongthevalleyofGöbelliCreekflowingthroughthe local,regional,andglobalscales.Inspiteofthepresence villageofÇürükler(Figure1).Thesectionwasmeasured ofrocksofthisageinTurkey,thestudiesoftheir usingaJacob’sstaff.Itslower32.50meterswere conodontbiostratigrahyarefew.However,somepapers sampledalongtheroadonthesouthwesternsideof havepreviouslybeenpublishedonconodontsofTurkey GöbelliCreekandtherestalongapathonthe (e.g.,Abdüsselâmo¤lu1963;Gedik1975,1977;Önder northeasternside.Throughmostofthesection,thebeds 1982;Çapk›no¤lu1991,1997;Kozur1997).Thispaper strikeN10-20ºEanddip60-70ºNW.Atotalof170 describesconodontfaunasobtainedfrom107samplesof sampleswerecollected,butonly107samplesyielded asinglestratigraphicsectionoftheUpperDevonian conodontfaunas.Thesampleswereprocessedusing GümüflaliFormationoftheeasternTaurides,and standardacidizingtechniqueswith10percentformic correlatesthisfaunatotheglobalstandardLateDevonian acid.Residueswerewashedthroughnestedsievesof63, conodontzones(Ziegler&Sandberg1990).Thestudied 100and850microns,butconodontswereonlypicked sectionislocatedinthevillageofÇürükler,about9km fromtheresidueonthe100-micronsieve. 69 LATEDEVONIAN CONODONTSFROMEASTERNTAURIDES (Figure2).Coralsareabundantinthelimestones,and BLACKSEA N brachiopodsandbryozoansinbothlimestonesandother lithologies.Thebasalportionoftheformationismadeup ofdarkgreylimestonesinterbeddedwithshaleormarly TURKEY shale.Themiddlepartconsistsofanalternationof AEGEAN Feke SEA Adana limestoneandshalewithquartzsandstoneandsiltstone 40km interbeds.Theupper85metersisdominatedbydark MEDITERRANEANSEA grey,silty-sandy,spiculiticlimestones. Göbelli C›v›kl› Creek Thecarbonaterocksrangefrommudstoneto boundstone.Manysampleshavepackstoneand ÇR170 grainstonetexture(Figure2).Skeletalgrainsand K›z›lyer Çürükler ÇR27 Aksu Fekeda¤› River ÇR1 Girvanella-oncoidsaretheabundanttypes.Pelletsand intraclastsarescarce.Brachiopods(shellsandspines), echinoderms(crinoids,echinoids),bryozoans, cyanophyceanalgae(generally Girvanella sp.),coralsand ostracods( Cryptophyllus sp.andothers)arethemost abundantskeletalparticles.Non-carbonatecomponents Göksu River aregenerallyrepresentedbydetritalquartzthatlocally reaches30volume%insomesamples.Dolomitization, micritization,silicification,pyritization,andlimoniteand N hematiteimpregnationwerethemostwidespred diageneticevents.Geopetalstructures,shelteringeffects andstyloliticstructuresarethemostwidespread 2km sedimentologicstructures.Abundantbioturbationfabrics FEKE areindicatedbythearrangementofbioclastsinacircular patternandbythedifferentpackingofparticles.Borings Figure1. Locationmapforthestudiedstratigraphicsection. areespeciallyabundantinbrachiopodshells.Fossil contentandsedimentologiccharacteristicsofthe Lithostratigraphy GümüflaliFormationindicateashallowsubtidal depositionalenvironment(Çapk›no¤lu1990,1991). TheDevoniansequenceoftheeasternTaurideshasbeen dividedintothreeformationinthepreviousworks:the LowerDevonianAy›tepesiformation(limestone-shale- Biostratigraphy sandstone),theMiddleDevonianfiafaktepeformation TheGümüflaliFormationisdominatedbyconodont (dolomiticlimestone),andtheUpperDevonianGümüflali speciesofthepolygnathid-icriodidbiofacies,together formation(sandstone-shale-limestone)(Özgül etal. withafewspeciesofthepalmatolepid-polygnathid 1973;Metin etal. 1983).TheGümüflaliFormation,on biofacies.Conodontsaregenerallynotabundant,and whichthisstudyisbased,hasbeennamedforan manypartsofthesectionyieldedfewornospecimens. approximately600-m-thickterrigenous-carbonaterock Becauseoftheinfluenceofbiofacies,thescarcityor sequenceoverlyingthefiafaktepeFormation(Figure2). absenceofzonallydiagnostictaxaandtheirregular Inthestudyarea,ithasafaultedcontactatitsbase,and verticaldistributionsofmanytaxa,thestandardLate thetopislithologicallygradationalintotheoverlying Devonianconodontzones(Ziegler1962;Ziegler& LowerCarboniferousZiyarettepeFormation.The Sandberg1984,1990)arenotreadilyapplicabletothe lithologicsequenceconsistsgenerallyofthin-medium GümüflaliFormation.However,someofthemhavebeen bedded,lightgreyquartz-sandstoneandquartz-siltstone, described. darkgreymarlandlaminatedshaleandlimestones,and containsarichmacrofaunaconsistingmainlyof Thelowestsample(Table1,sampleÇR2)ofthe brachiopods,bryozoansandsolitaryormassivecorals studiedstratigraphicsectionisofFrasnianage,noolder 70 fiENOLÇAPKINO⁄LU&‹SMETGED‹K EXPLANATION Rc ÇR170 ÇR120 MRc f m F1 F9 ......................... ......................... COVERED F2 F10 F3 F11 ......................... ÇR110 ......................... S F4 F12 F5 F13 COVERED S F6 F14 ......................... F7 F15 COVERED ÇR160 ......................... F8 F16 COVERED ......................... Rc COVERED .......................... H ÇR100 ......................... f Limestone Siltstone ......................... Rc .......................... ............. ......................... MRc ............. ......................... Shaleandmarl Sandstone ......................... H ÇR90 .......................... H F1:Mudstone .......................... F2:Bioclasticwacke-/packstone ......................... .......................... F3:Coralbafflestone ......................... F4:Coral-bioclasticwackestone ÇR80 ......................... ......................... ÇR150 .......................... F5:Gastropodpackstone F6:Oncoid-bioclasticpack-/grainstone M .......................... .......................... F7:Bioclasticpack-/grainstone ......................... F8:Brachiopodpack-/grainstone m m m m m F9:Brachiopod-echinoderm ÇR70 M .......................... pack-/grainstone ......................... PMRc F10:Brachiopod-echinoderm-bryozoan ÇR60 ......................... .......................... pack-/grainstone ......................... M Rc F11:Ostracodgrainstone .......................... F12:Dasycladaceanalgal-bioclastic P M packstone M Rc F13:Stromatoporoidal-bioclastic ÇR50 M packstone PHMRc .......................... F14:Pelletoidal-bioclasticgrainstone ......................... .......................... F15:MudstonebearingUmbellinasp. ......................... andpelletoidal-intraclastic ......................... Rc .......................... grainstonewithUmbellinasp. m m m m Rc F16:Spiculiticwacke-/packstone m m m m ÇR40 ......................... .......................... ......................... .......................... RcSyntaxialrimcement ......................... P HHematiteimpregnation m m m m m ......................... SSilicification ÇR140 MR PPyritization ÇR30 MMicritization M P Dolomitization S Geopetalstructure H 20m P ÇR20 Rc Shelteringeffect M m m m m m Burrowing ÇR130 .......................... Rc SCALE 10 m m m m m Rc Boring ÇR10 PH H M Stylolite SMPRc 0 m m m m .......................... ÇR1 f Rc Laminatedstructure Figure2. Lithologicdevelopmentofthestudiedstratigraphicsectionandthesamplelocations. 71 LATEDEVONIAN CONODONTSFROMEASTERNTAURIDES thantheupper falsiovalis zonebecauseofthepresence 18).SampleÇR47(Table2)includesthelowest ofIcriodus subterminus YOUNGQUIST,1947,whichfirst occurrenceof Polygnathusbuddingtoni SAVAGE,1987, appearswithintheupper falsiovalis zone(Sandberg& whichdoesnotoccurbelowthelowerhassi
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