Records of the Western AlIstrallall MlIselllll Supplement No. 58: 293-303 (2000).

Early Silurian sea-level changes in southern Turkey: Lower Telychianconodont data from the Kemer area, western Taurides

Yakut Gonciioglu 1 and Heinz W. Kozur 2

IDepartment of Geology, Maden Tetkik ve Arama Enstiti.i.si.i., Ankara, Turkey2Rezsi.i. u. 83, Budapest-Hungary

Abstract - A rich conodont fauna of the Pterospathodlls eopellllatlls Zone (lowerTelychian), the oldest Silurian fauna from the southern Taurides, wasrecovered from the middle Sapandere Formation of the upper Antalya Nappeat Kemer, western Taurides, Turkey. It is similar to European warm-waterconodont faunas of the same age. This suggests the formation was initiatedby a pre-Telychian (?Aeronian) transgression. The Ashgill of the same areacontains Perigondwana cold-water fossils, whereas early Llandovery glacio­marine deposits to the southeast contain exotic dropstones, such asmicaschists and orthogneisses. The warming after the end Ordovician-earliestSilurian glaciation caused a rapid global sea-level rise resulting in depositionof black shales during the Aeronian, followed by a drop in sea-level in thelate Telychian of southern Turkey.

INTRODUCTION

Age data for Early Palaeozoic rocks in Turkey arevery limited. They have received less attention thaneither Late Palaeozoic or Mesozoic strata. This isespecially the case for Early Silurian sediments thatconstitute important hydrocarbon source units. TheLate Ordovician-Early Silurian period inPerigondwana was marked by rapid global sea­level fluctuations as indicated by unconformitiesand transgressions. It is commonly accepted thatthese features result from waxing and waning ofice-sheets in northwest Gondwana (Scotese andMcKerrow 1990) but may, in some cases, be relatedto local tectonic events.

It is also established that the onset of the Silurianwas characterised by a regional transgression innorthwest Gondwana (Holland 1981 and thereferences therein). The most distinctive EarlySilurian deposits in this area are organic-rich, cold­water siliciclastics (black shales) associated with themelting of the South Polar ice-cap. These blackshales can be traced laterally for hundreds ofkilometres (Rutherford et al. 1997). They areregionally underlain by clastics that containdiamictites (dropstones heterometric sandstones)and overlain by shallow-water clastic-carbonatesuccessions in Arabia, Iran and southern Turkey.

In this paper we report biostratigraphical data onpoorly known Silurian sediments in the Kemer Unitof the Upper Nappe by re-examining earlierconodont data (Goncuoglu unpublished data), thefirst Early Silurian conodont data from the westernTaurides. We aim to establish a more reliablestratigraphical framework for the Early Palaeozoic

sequence in the Antalya nappes in the westernTaurides and correlate this data with informationfrom the Central and Eastern Taurides, and theEastern Mediterranean region to develop a betterunderstanding of the global sea-level changesduring the Early Silurian and their possible causes.

REGIONAL GEOLOGICAL FRAMEWORK

The very complex structure in the western BeyDaglari area to the northwest of the Antalya Bay(Figure 1) consisting of numerous tectonic slivers ofPalaeozoic and Mesozoic platform sequences,volcanic assemblages and ophiolitic rocks has beennoted in the earliest geological studies (e.g. Tietze1885). Altinli (1944) was the first to recognise thepresence of an autochthonous sequence (BeyDaglari Anticline) flanked on both sides byallochthonous nappes; these were later named theLycian nappes (Brunn et al. 1970) in the west andthe Antalya nappes (Lefevre 1967) in the east.Altinli (op. cit) revealed that detailedbiostratigraphical studies were required to separatethe tectonic units because of lithostratigraphicalsimilarities. Marcoux (1970, 1977, 1979) mapped thearea to the west of the Antalya Bay, and subdividedthe allochthonous Antalya nappes into the Early-,Middle-and Upper Nappe. Each of these werefurther subdivided into tectonic units.

Palaeozoic sequences are the main constituents ofthe Upper Nappe, constituting the Bakirlidag,Kemer and Tahtalidag units (Marcoux 1970). In theBakirlidag Unit the sequence starts with neriticPermian carbonates followed by Scythian marls,

294

Antalya

Y. Gonciioglu, H.W. Kozur

TURKEY ~.-..... /' 0 200 km.......... / ----

-~ SYRIAMEDITERRANEAN SEA

2

Figure 1 Location and structural map of the western Antalya Bay showing the main tectonic units (modified fromSenel 1986). 1- Bey Daglari Autochthon, 2-Antalya nappes, a) Palaeozoic units, b) Mesozoic-Early Tertiaryplatform sequences, c) Late Cretaceous melange, d) Ophiolites, 3- Tertiary (Eocene-Miocene) cover, 4­Alluvium.

Early Silurian sea-level changes in southern Turkey 295

Anisian-Norian pelagic limestones and UpperNorian-Cretaceous platform carbonates,respectively, and thus differs from the other unitsbecause of an absence of Early Palaeozoicsequences. The Kemer Unit, by comparison consistsof Ordovician-Permian sediments overlain byScythian marls, Ladinian bedded cherts and LateTriassic-Cretaceous pelagic limestones (~enel 1986).Recent work (~enel et al. 1992) has shown that thePalaeozoic succession commences with MiddleCambrian carbonates. The Kemer Unit has a morecomplete Palaeozoic succession as well asdifferences in the Mesozoic sequence of other units.In the third unit of the Upper Antalya Nappe,(Tahtalidag Subunit: Marcoux 1979; Tahtali Unit:~enel 1986) Jurassic-Cretaceous neritic carbonatesunconformably cover the so-called "Ordovicianshales", the distinguishing feature being the absenceof the Early Silurian and Middle Palaeozoic-Triassicsequences (Marcoux 1977, 1979; ~enel et al.1983;~enel 1986). ~enel et al. (1992) used the nameTahtalidag Nappe as a synonym of the UpperAntalya Nappe; this is not to be confused with theTahtalidag Unit of Marcoux (1977) or Tahtali Unitof ~enel (1986).

As this brief review shows, all the tectonic unitsin the area have been distinguished by differencesin depositional features of contemporaneoussediments, or through comparisons betweenPalaeozoic and Mesozoic sequences within theunits. These sequences, however, havelithostratigraphic similarities. Moreover, the

presence of numerous structural discontinuitiesprecludes stratigraphical order as a reliable tool inisolation. Detailed biostratigraphical work on thesedimentary successions is therefore required.

STRUCTURAL SEITING ANDSTRATIGRAPHY OF THE SILURIANSEDIMENTS IN THE KEMER UNIT

The Kemer Unit is the middle thrust-slice of theUpper Antalya Nappe. It crops out as a N-Strending tectonic sliver, almost 10 km long, to theWNW of Kemer.

The succession of the Palaeozoic units is wellexposed along the Kesmebogazi, Belen Dere andSapan Dere gorges. These locations show the typicalsequence of Palaeozoic sediments in the Kemer Unitof the western Antalya nappes. The lower contactof the Palaeozoic succession in Belen Dere is a steepthrust-plane along which the lowermost unit, theSariyardere Formation, is thrust over Early Triassicmarls.

The Silurian sediments in the type-area were firstdescribed by Marcoux (1977, 1983) and later namedas Sapandere Formation by ~nel et al. (1983). Thelithology is characterised by an alternation of thick­bedded sands tones, sandy dolomites, andsubordinate sandy limestones and shales (Figures 2and 3). In the type section, to the southeast of SapanDere, the formation starts with gray-brown, thick­bedded sandstones, followed by sandstones withwell-developed cross-bedding and symmetric

1::::::::1 Sandstone mLimestone~ Gypsum

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Figure 2: "t'n~,•. ",wtlim sh()wmg the contact relations and rock units of the Sapandere Formation in its type locality

296 Y. Gondioglu, H.W. Kozur

z z

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Medium to thick bedded dolomites

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Thick bedded, grey, yellowish-brown, in the lower partcross-laminated sandstones with shale interlayer

Medium to thick bedded, yellow, greenish-grey, fine graineddolomites

Dark sandstones and mudstones

MediumJo thick bedded~gre~greenish-brow~crosslam.inat~carboJlate.,cemented sandstones witbsiltstoaeJlDdsbaleinterIayers

:::::::::::::::;::~::::::::::::::::::::::::::.......................... .. .. .. .. .. .. .. .. .. .. ..

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Medium to thick bedded, cross-laminated sandstones

Medium to thick bedded, brown, grey, quartz-rich carbonate­cemented sandstones

UNCONFORMITYDark shale and siltstone alternation with sandstone interlaye

Thick bedded, yellow, greenish-grey, fine grained dolomites

Thick bedded, brown, cross-laminated, carboDate-cementedsandstonesBlack, bituminous limestoneBlack shales

Medium bedded, brown sandstones

Thick bedded, yellow, greenish-grey, fine grained dolomites

Thick bedded, grey, in the lower part cross-laminatedsandstoneThick bedded, greenish-grey, fine grained dolomites

~ Conodonts @Nautiloids ~ Brachiopods (' Graptolites

........................................

=~~~~-----~-~~~

111... H6••: "10 : ::••::•••: ••::••::•••: •••

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ORDOVICIAN

Figure 3 Section of the Sapandere Formation measured at its type locality (after ~nel 1986).

Early Silurian sea-level changes in southern Turkey

~--

1 2 He Zone Conodont

P Dza r'kod! lnhornensr' boucekl transgreejl ens Dulodus 1j

d0 branlkenSls-loehkovensls Dzar'kodl na r'emsellel dens i1 Interval ZoneI parultlmus uIt1mus

Dzarkodlna en spaformosus

OzarkodHJa snaJderlLud ford 1arl bohemleus tenuls-

L kozlowskl i Pedavls latlalatusud lelntwardlnensls Po 1yljlld LlIU 1eJes Sllur!cus10 Aneoradella ploeckenslsw scam cus

Dzarkodlna exeavataGors tl an

Kockelella v vanablllsmlssom

Polygnatholdes crassus

ludensl

If.! l-deubell Oza rkod HJa bohemlcaW Homen cHI

S e par,us nassan

I 1 1undgrem Ozarkodlna )1 tta sag1tta0

L e ng1dus-perner1k Ozarkod1na tta rhenana

U She1nwoodlan n cca rtonens 1s-belophorus Koeke 1ell a ranul1formls

Reentr1fugus-mureh1son1

!1apworth1 Pterospathodus

A amorphognatholdessplral1s Interval Zone

Ncrenulata

P 'IUopd LlIUUI ee 11 ornTel lan Ig es tom ens 1s

enspus I Pte U~f.!dLIIUUI

turrieulatusI eupelllld L

L1 gueC'l elllan Is ek 11d0 eonvolutus Pterospatflodus tenU1Sv Distomodus aese Aer'onlan 1ry magnus

trlangulatus

Icy

la naees!f? Dlstornodus kentuckyenS!

la

la natusOza r'kod 1na 7 nathanl

297

Table 1 Silurian graptolite and conodont zonations. Revised after "The Subcommission on Silurian Stratigraphy"(1995). Vertical distances not time-related. 1: System. 2. Series.

298

ripple-marks alternating with greenish to yellowish­gray thick bedded dolomites (Figure 3). The firstblack shale, 20 m above the base, contains abundantgraptolites (Monograptus sp. indet.), pyritizednautiloids and brachiopods in carbonate-bearinglayers. These have not been studied in detail. Abovethis there is a thick package of sandstone,alternating sandy dolomite and dolomite, with ablack sandstone-mudstone layer 53 m above thebase.

Conodonts were recovered at 65 m above the base(BT-80-94) from medium bedded, greenish-graydolomitic limestones (Figure 3). A diabase sill,almost 7 m wide, has caused contact metamorphismin underlying carbonates. The upper part of theSapandere Formation in its type locality consists ofmedium to thick-bedded sandstones with low-anglecross-stratification and ripple-marks.

About one km to the southwest of the type­locality, the alternation of dark shales and greenquartz-arenites with some nautiloid-bearing sandylimestone lenses corresponds to the lower 18-23 mof type section of the Sapandere Formation (H.Kozur, oral communication) and contains Aeronianconodonts (Gonciioglu et al., in prep). The upperpart of this sequence consists of dolomites andsandstones. The Telychian greenish-grey limestonesand dolomitic limestones of the type section are notpresent at this locality.

The Sapandere Formation is underlain by a sharpcontact with the Sariyardere Formation (~nel et al.1983). This mainly consists of an alternation ofbrown, greenish-black and gray sandstones,siltstones and shales. Its type locality, in the SariyarDere, is almost 12 km south of Sapan Dere. Thetype section of the Sariyardere Formation ischaracterised by well developed cone-in-conestructures and diabase sills and dykes. Marcoux(1983) assigned the upper part of the type section ofthe Sariyardere Formation to the Sort TepeFormation, established by Dean et al. (1981, in Deanand Monod 1990) and he reported casts ofbrachiopods together with Piacoporia that suggesteda Late Ordovician (Ashgill) age for the unit. NoSilurian rocks been reported in contact with theSariyardere Formation at this locality. ~nel et al.(1983) and ~nel (1986) correlated the very similarclastic rocks underlying the Sapandere Formationin the Kesmebogazi and Sapan Dere sections withthe Sariyardere Formation, but noted the absence ofdiabase dykes in the latter locality. ~nel et al. (1983)and ~nel (1986) suggested a conformable contactbetween these two units and a Late Ordovician agefor the clastics based on this correlation. We believe,however, that the previously identified SariyardereFormation at these localities belong to the EarlyOrdovician upper Seydi~ehir Formation, andtherefore do not use the term Sariyardere Formationin this context.

Y. Gonciioglu, H.W. Kozur

The Sapandere Formation is unconformablyoverlain by the Middle-Late DevonianHocaninsuyu Formation. The unconformity isaccentuated by truncation of the underlying layersand oxidation on the unconformity surface (~nel

1986). Significantly, an evaporite -bearing Devoniansequence is only encountered in this area.

CORRELAnON WITH OTHER UNITS

To date Early Silurian units are described fromonly a few localities in the western Taurides(Tahtali Unit: ~nel et al. 1983), central Taurides(Akseki-Murti<;i: Demirta~li et al. 1977) and easternTaurides (Saimbeyli-Tufanbeyli area, Dean andMonod 1990).Demirta~li (1984) distinguished the Egripinar and

Hirmanli formations in the Akseki-Murti<;i area,part of the Geyikdag Autochthon. The EgripinarFormation consists of a lower thick-bedded, yellowto buff arkosic sandstone and conglomeratesequence overlain by a turbiditic sandstone­siltstone member yielding an Early Silurianmiospore association. The conformably overlyingHirmanli Formation primarily consists of very thin­bedded, pyrite-bearing siliceous black shalesalternating with very fine laminated black shaleswith Early Silurian graptolites (Monograptus cf. M.spiralis Geinitz, Monograptus cf. M. aculus Lapworth,Climacograptus cf. C. scalaris Risinger, Rastrites sp.).It is assumed these very fine laminated shales weredeposited in a deep, restricted basin (Demirta~li

1984).In the eastern Taurides (Saimbeyli-Tufanbeyli

area), the equivalents of the Sapandere Formationwere subdivided by bzgiil et al. (1973) into threeformations. The lower part (Halityayla Formation)consists of sandstones and conglomeratesinterlayered with heterometric sandstones ofprobable glacio-marine origin. They are overlain bylate Aeronian black shales, the Puscutepe ShaleFormation (Dean and Monod 1990). The uppermostformation (Yukariyayla Formation) consists oflower limestones and upper turbiditic clastics. Thelower limestone bands are rich in nautiloids. Deanand Monod (1990) suggested a late Aeronian agefor these limestones, whereas Gonciioglu and Kozur(in press) report latest Telychian to earliest Wenlockconodonts from these beds.

CONODONT DATA

One conodont sample of the Sapandere Formation(Bt-80-94, location and sampling point in the sectionare indicated in Figures 1 and 3) from the SapanDere section (type section of the SapandereFormation) yielded a rich and well preservedconodont fauna (CAI = 1-2.5). More than 100specimens were recovered. The insoluble residues

Early Silurian sea-level changes in southern Turkey 299

Figure 4 All illustrations are from sample Bt-80-94.I, 2, Apsidognathus sp. of the A. tuberculatus Walliser group, Paelement, upper view. 1, x 140, rep.-no. 27-11/1-25. 2, x 150, rep.-no. 27-11/1-3. 3-7, Distomodusstaurognathoides (Walliser). 3, Pa element, upper view, x80. rep.-no. 27-11/1-1; Se element. 4: x 150, rep.-no.27-11/1-16. 5, x 150, rep.-no. 27-11/1-24. 6, x 110, rep.-no. 27-11/1-14. 7, x 150, rep.-no. 27-11/1-23. 8-10:Pseudooneotodus tricornis Drygant; Fig 8: upper view, x250, rep.-no. 27-11/1-7. 9, lateral view, x 250, rep.-no.27-11/1-10.10, upper view, x 150, rep.-no. 27-11/1-6.

300 Y. Gonciioglu, H.W. Kozur

Figure 5 All illustrations are from sample Bt-80-94. 1, 3, 4, 6, 7, Pterospathodus eopennatlls Miinnik. 1, Pa element, lateralview, x 140, rep.-no. 27-11/1-5. 3, Pa element, upper view, x 150, rep.-no. 27-11/1-4. 4, Pa element, lateralview, x 120, rep.-no. 27-11/1-2. 6, Pb1 element, x 200, rep.-no. 27-11/1-18. 7, Se element, x 150, rep.-no. 27­11/1-17.2,5, Pseudooneotodlls beckmanni (Bischoff and Sannemann). 2, upper view, x 300, rep.-no. 27-11/1-8.5, lateral view, x 250, rep.-no. 27-11/1-9.

Early Silurian sea-level changes in southern Turkey 301

Figure 6 All illustrations are from sample Bt-80-94.1, 2, Oulodus n. sp. A sensu Over and Chatterton 1987, x 140. I, Seelement, rep.-no. 27-11/1-11. 2, ?Pa element, rep.-no. 27-11/1-19. 3-5, 7, Oulodlls fluegeli (Walliser). 3, Seelement, x 150, rep.-no. 27-11/1-21. 4: Pb element, x 200, rep.-no. 27-11/1-22. 5, Sa element, x 150, rep.-no. 27­11/1-15.7, Se element, x 80, rep.-no. 27-11/1-20. 6, Decoricollus cf. fragilis (Branson and Mehl), x 200, rep.-no.27-11/1-12.8, Dapsilodus sp., x 120, rep.-no. 27-11/1-38.

302

also include some foraminifers, ostracodes andbrachiopods. All conodonts illustrated on Figures4-6 are from sample Bt-80-94, Pterospathoduseopennatus Zone of lower Telychian (lower part ofupper Llandovery), middle Sapandere Formationfrom the Sapan Dere section, NW of Kemer, UpperAntalya Nappe, western Taurides, southern Turkey.

The following species were determined (Figures4-6): Apsidognathus sp. of the A. tuberculatusWalliser group, Dapsilodus sp., Decoriconus cf. fragilis(Branson and Mehl), Distomodus staurognathoides(Walliser), Oulodus fluegeli (Walliser), Oulodus n. sp.A Over and Chatterton Pseudooneotodus beckmanni(Bischoff and Sannemann), Ps. tricornis Drygant andPterospathodus eopennatus Miinnik. The apparatusesof some of these species can be reconstructed. Pt.eopennatus is the index species of the Pt. eopennatusZone of the lower Telychian (early LateLlandovery). D. staurognathoides occurs from theAeronian to the lower part of Telychian. Frompersonal communication with Dr. P. Mannik,Tallinn, a form that we had originally determinedas Oulodus sp. is Oulodus n.sp. A Over andChatterton. This corroborates an age of Pt.eopennatus Zone. Thus, the middle SapandereFormation at its type locality can be assigned to theearly Telycian (late Llandovery, Early Silurian).

DISCUSSION AND CONCLUSIONS

Dated Llandovery is rare in the Tauride­Anatolide Composite Terrane; conodont data werepreviously unpublished. In the eastern Taurides,conodonts of the P. amorphognathoides Zone of latestLlandovery to earliest Wenlock were found in theYukanyayla Formation (Gonciioglu and Kozur, inpress). The conodont fauna from Kemer is thereforethe oldest known Silurian conodont fauna from thesouthern Taurides.

The conodont fauna from the middle SapandereFormation allows an age diagnosis of considerableprecision for this part of the Formation; early lateLlandovery (early Telychian) P. eopennatus Zone.The conodont data are in agreement with Marcoux(in Dean and Monod 1990), who considered thenautiloid-bearing sandstones below the conodontsample as Telychian in age. The Siluriantransgression began in the Antalya nappessomewhat prior to the Telychian, between Ashgilland middle Llandovery. This corresponds to thegeneral transgression on the southern part of theTauride-Anatolide Composite Terrane (Gonciioglu1997) and in SE Anatolia, mostly over LateCambrian to Arenig Seydi~ehir shales or facialequivalents. Siliciclastic Ashgill beds are sometimesalso present (~rtTepe Formation; Marcoux 1983).

Post-Tremadoc Ordovician fossils have a distinctPerigondwana cold-water association. Whenpreserved glacio-marine deposits with exotic

Y. Gonciioglu, H.W. Kozur

dropstones (e.g. orthogneisses and micaschists) arepresent in the Ashgill to early Aeronian interval.The late Llandovery (Telychian) conodont fauna,however, is a warm-water fauna.

The widespread dolomites in the lower SapandereFormation are of probable middle Llandovery age.At Ovacik at the Mediterranean coast, they containmiddle Llandovery graptolites (Dean et al. 1991).These are the oldest dated Silurian rocks of thesouthern Taurides.

Glacio-marine deposits with exotic dropstones arealso reported from the Ovacik (EgripinarFormation; southern Central Taurides) andTufanbeyli (Halityayla Formation, EasternTaurides) areas within the lowermost part of thetransgressive Silurian series. Acritarch data fromthe upper part of Halityayta Formation indicate apost-Rhuddanian to ?early Aeronian age (Dean andMonod 1990).

In the Middle East, transgressive clastic rocksoverlying glacial sediments are known from centralSadie Arabia (Sarah Formation, Mahmoud et al.1992) stratigraphically corresponding with thelowermost clastics of the Sapandere Formation or tothe Halityayla Formation and the EgripinarFormation in the eastern and central Taurides,respectively. The black shales conformablyoverlying the clashes (Qusaiba Member of theQualibah Formation; McGillvray and Husseini1992) are diachronous. In the subsurface of theRiyadh area, its age is early Rhuddanian, whereasfurther to the northwest (Qasim area), outcroppingearly Aeronian graptolites have been found. Thegraptolite-bearing black shales in the Tauridescorrelate well with this unit. As with the Taurides,the black shales in Saudi Arabia are followed by anupward-coarsening late Llandovery sequence, thelower part rich in nautiloids corresponding to the"Orthoceras Limestone" in the upper part of theSapandere Formation. This regional shallowing atthe end of Llandovery is also recorded in Jordan(Berry and Boucot 1972).

The warming event after the Ashgill to lowermostAeronian glacio-marine sediments were depositedwas obviously very fast. The middle Llandoverytransgression on the Tauride-Anatolide CompositeTerrane, as documented in the Kemer area, WesternTaurides was possibly connected with this (eustaticsea-level rise). The late Llandovery in southernTurkey, however, is represented by a shallowingupwards sequence, similar to the Middle East. Thislate Telychian regression seems to be a major eventat the northwest Gondwana margin (LoydeIl1998).

ACKNOWLEDGEMENTS

The area concerned was mapped by Dr. M. ;;enelwhom we thank for his support with field data. Dr.P. Mannik, Tallinn, provided very important

Early Silurian sea-level changes in southern Turkey

taxonomic and biostratigraphic evaluation of theconodonts. The regional geological implications ofthe data were kindly reviewed by. Prof. Or. M. C.Goncuoglu, Ankara. The second author thanksTUBITAK for the NATO-CP grant. We acknowledgethe contribution of Mr A. Oner and the TurkishPetroleum Corporation for the SEM photographs.We are grateful to the unnamed assessors andeditors of the paper for their suggestions andlinguistic improvements. This work is a contributionto the IGCP Project 351 and to IGCP Project 421 NorthGondwana M id- Palaeozoic bioeven t/biogeographypattems in relation to crustal dynamics.

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Manuscript received February 1999; accepted October 1999.