Turkish Journal of Earth Sciences (Turkish J. Earth Sci.), Vol. 13, 2004, pp. 177-186. Copyright ©TÜB‹TAK

177

New Results on the Lithostratigraphy of the Kazda¤Massif in Northwest Turkey

MEHMET DURU, fiÜKRÜ PEHL‹VAN, YALÇIN fiENTÜRK,FATMA YAVAfi & HÜSEY‹N KAR

Department of Geological Research, General Directorate of Mineral Research and Exploration (MTA),TR-06520 Ankara, Turkey(e-mail: duru@mta.gov.tr)

Abstract: The high-grade metamorphic rocks of the Kazda¤ mountain range, termed the Kazda¤ Group, crop outas a tectonic window under the Karakaya Complex in northwestern Turkey. The Kazda¤ Group forms a doublyplunging, NE–SW-trending anticliniorium. During our regional geological mapping of the Kazda¤ Group, we havesubdivided the metamorphic rocks into four formations. The lowermost unit is the F›nd›kl› formation, whichcomprises amphibole-gneiss, marble and minor amphibolite. It crops out mainly in the southern part of the Kazda¤Massif. The marble horizons within the F›nd›kl› formation have been named the Alt›noluk and Babada¤ marblemembers. The overlying unit, comprising metadunite and orthoamphibolite, is the Tozlu formation, which in turnis overlain by the Sar›k›z marble. The uppermost unit, which crops out in the northern parts of Kazda¤ Massif, isthe Sutuven formation that comprises sillimanite-gneiss, migmatite and minor marble, amphibolite and graniticgneiss. All these formations underwent a common metamorphism and share a mutual foliation. The metamorphicrocks of the Kazda¤ Group are in tectonic contact with the surrounding Permian to Miocene rocks and are intrudedby the Oligo–Miocene granodiorites. The oldest rocks, which stratigraphically overlie the Kazda¤ Group, arePliocene and younger in age. There is no data on the chronostratigraphy of the Kazda¤ Group, but the isotopic ageof the latest metamorphism affecting the Kazda¤ Group is Oligo–Miocene. The Kazda¤ Group has attained itspresent tectonic position as a metamorphic core complex by domal uplift through post-Miocene detachment faults.

Key Words: Kazda¤, northwestern Turkey, metamorphic rocks, lithostratigraphy, extension, core complex

Kazda¤ Masifi’nin Stratigrafisinde Yeni Bulgular

Özet: Kazda¤› oluflturan yüksek dereceli metamorfik kayalar kuzeybat› Anadolu’da Karakaya Kompleksi alt›ndanbir tektonik pencere olarak yüzeyler. Kazda¤ Masifi’nin yap›s›, k›vr›m ekseni NE–SW do¤rultulu ve her iki yönedal›ml› bir antiklinoryum fleklindedir. Yapt›¤›m›z jeolojik haritalama çal›flmas›nda, amfibolit fasiyesindemetamorfizma geçirmifl olan Kazda¤ Grubu metamorfitleri alttan üste do¤ru F›nd›kl› ve Tozlu formasyonlar›,Sar›k›z mermeri ve Sutuven formasyonu olarak ay›rtlad›k. Masifin güney kesimlerinde yüzeyleyen amfibollü gnays,mermer ve yer yer amfibolit ardalanmas›ndan oluflan F›nd›kl› formasyonu içerisinde Alt›noluk ve Babada¤ mermerüyeleri tan›mlanm›flt›r. Masifin orta kesimlerinde yeralan metadunit ve ortoamfibolit kapsayan metaofiyolitikkayaçlar Tozlu formasyonu, ofiyolitler üzerinde yer alan mermer seviyesi Sar›k›z mermeri olarak ay›rtlanm›flt›r.Kazda¤› metamorfiklerinin en üst seviyelerinde bulunan sillimanit gnays, biyotit gnays, granitik gnays ve yer yermigmatit içerikli seviyeler Sutuven formasyonu olarak tan›mlanm›flt›r. Sutuven formasyonu içerisinde ayr›ca incemermer ile amfibolit seviye ve mercekleri de vard›r. Metamorfizma öncesi evrede muhtemelen tektono-stratigrafikolarak istiflenmifl olan bu formasyonlar beraberce metamorfizma geçirmifl ve birlikte foliasyon kazanm›flt›r. Kazda¤metamorfitleri çevrelerinde mostra veren Permiyen–Miyosen yafltaki kayaçlarla tektonik dokanaklar oluflturmakta,ve Oligo–Miyosen yafll› granitler taraf›ndan kesilmektedir. Kazda¤ metamorfitleri üzerinde stratigrafik dokanaklayer alan en yafll› birim Pliyosen yafltad›r. Stratigrafik yafl›n›n saptanmas›nda yeterli veri bulunamayan Kazda¤metamorfik kayaçlar›n›n son metamorfizma yafl›, önceki araflt›r›c›lar taraf›ndan jeokronolojik yöntemleOligo–Miyosen olarak belirlenmifltir. Kazda¤ Masifi, Miyosen sonras›nda geliflen s›yr›lma ve yanal at›ml› faylarla, birmetamorfik çekirdek kompleks olarak dom fleklinde yükselerek bugünkü konumunu kazanm›flt›r.

Anahtar Sözcükler: Kazda¤, kuzeybat› Türkiye, metamorfik kayalar, litostratigrafi, gerilme, çekirdek kompleks

Introduction

This paper reports the preliminary results of alithostratigraphic investigation of the Kazda¤ Massifwithin a wider project on the geology of the Bigapeninsula. The Kazda¤ Massif is the name given to a high-grade metamorphic complex, called the Kazda¤ Group,which crops out in the Kazda¤ Mountains in the Bigapeninsula in northwestern Turkey (Figure 1).Tectonically, the Kazda¤ Group lies in the Sakarya Zoneand exposes the lowest crustal levels in northwesternTurkey. The Kazda¤ Group was uplifted as a result ofpost-Miocene extensional tectonics, and as a consequencethe metamorphic rocks exhibit faulted contacts with the

surrounding pre-Miocene rocks. The Kazda¤ Massif isnow generally regarded as an Oligo–Miocenemetamorphic core complex (Okay et al. 1991; Okay &Satır 2000).

The Kazda¤ Group forms structurally a doublyplunging, NE–SW-trending anticlinorium. From its baseupwards it consists of amphibole-bearing gneiss withmarble intercalations, metaophiolite, marble and gneiss.The base of the Kazda¤ Group has not been observed,and the Kazda¤ Group is tectonically overlain by Permianto Miocene sedimentary, magmatic and metamorphicrocks (Figure 2). Triassic low-grade metamorphic andsedimentary rocks to the east and north of the Kazda¤

GEOLOGY OF THE KAZDA⁄ MASSIF

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Figure 1. Geological map of western Turkey illustrating the tectonic setting of Kazda¤ Massif(modified from Okay et al. 2004).

M. DURU ET AL.

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Group, which include blocks of Permo–Carboniferouslimestone olistoliths, have been described as the KarakayaFormation by Bingöl et al. (1975). West of the Kazda¤Massif lies the Çetmi Mélange, described in detail by Okayet al. (1991) and Okay & Satır (2000). The ÇetmiMélange of Late Cretaceous–Palaeocene age, comprisesmafic volcanic and volcaniclastic rocks, limestone blocks ofLate Triassic to Late Cretaceous age, and tectonic slices ofshale, greywacke, radiolarian chert, serpentinite, garnet-mica schist and eclogite. The Çetmi Mélange and theKarakaya Complex around the Kazda¤ Massif areunconformably overlain by the Miocene lacustrinesediments and volcanic rocks (Figure 2). These Miocenedeposits have tectonic contacts with the Kazda¤ Group.Oligo–Miocene granitoid rocks crop out widely within theKazda¤ Group and the surrounding rocks, showing bothintrusive and tectonic contacts with the host rocks. Allthese rocks, including the Kazda¤ Group, areunconformably overlain by the fluviatile and alluvialsediments of the Bayramiç formation of Plio-Quaternaryage (Siyako et al. 1989).

Early studies on the Kazda¤ Group in the 1950s and1960s described the metamorphic rock types withoutproviding details on its lithostratigraphy (Geis 1953;Kaaden 1959; Schuiling 1959; Gümüfl 1964; Aslaner1965). The first detailed study on the Kazda¤metamorphic rocks was by Bingöl (1968, 1969), whosubdivided the metamorphic rocks into three units: at thebase he recognised a basic-ultrabasic series ofmetadunite, metagabbro and amphibolite, which isoverlain by a “silico-aluminous” series of schist andgneiss; and the uppermost unit is a carbonate seriesconsisting of marble. Bingöl (1968, 1969) also provideddetailed information on the petrology and geochemistryof the Kazda¤ Group. Gözler et al. (1984) classified theamphibolite-facies metamorphic rocks, from the baseupwards, as migmatite, gneiss, marble, amphibolite andmetadunite-serpentinite, and indicated that the high-grade metamorphic rocks pass upward into lower gradeones. Sulzer (1990), in his detailed structural andpetrofabric study of the Kazda¤ Group, differentiated amylonitic paragneiss-migmatite-amphibolite series at thebase, to which he speculatively assigned a Palaeozoic age.This series was reportedly overlain by metaophioliticrocks of unknown age and, at the top of the sequence,orthogneisses of presumed Mesozoic age occur. Sulzer(1990) claimed that this whole sequence was tectonicallyassembled during the Early Tertiary in a subduction-zone

setting. Okay et al. (1991) and Okay & Satır (2000)described a thick, extensional mylonite zone above thegneisses of the Kazda¤ Group; they stated that thecontacts of the Kazda¤ Group with the surrounding pre-Miocene rocks are tectonic and that the Kazda¤ Groupforms an extensional metamorphic core complex ofOligo–Miocene age, and was exhumed for the first time inthe Plio-Quaternary. Isotopic age data from the Kazda¤Group have been provided by Bingöl (1968), Okay et al.(1996), and Okay & Satır (2000). These data indicate anearly high-grade metamorphism of Mid–Carboniferousage, strongly overprinted by a second phase of high-grade metamorphism in the Oligo–Miocene which wasrelated to extension in the Aegean region.

Lithostratigraphy of the Kazda¤ Group

During our regional geological mapping of the Kazda¤Group, we have subdivided the metamorphic rocks intofour formations (Figure 3). These are, from the baseupward: the Fındıklı formation, consisting of amphibole-bearing gneiss and marble; the Tozlu formation, whichcomprises the metaophiolite; the Sarıkız marble; and theSutuven formation comprising gneiss and migmatite.These formations are described below.

Fındıklı Formation

The Fındıklı formation, which is named for the first timein this study, consists of an intercalation of amphibole-bearing gneiss and marble. In previous studies the Fındıklıformation was included in the amphibolite unit of themetaophiolite (Bingöl et al. 1975). The Fındıklı formationcrops out in the basal parts of the Kazda¤ anticlinoriumon the southern flanks of Kazda¤ Mountain in the area ofthe Fındıklı, fiahin and Mıhlı streams (Figure 4). The nameof the formation comes from the Fındıklı stream, and itstype locality is east of the Arıtaflı village within the Fındıklıstream. The lower contact of the Fındıklı formation is notexposed; it is covered by the Tozlu and Sutuvenformations.

The Fındıklı formation consists of a regularintercalation of amphibole-bearing gneiss and marblehorizons. The gneiss horizons are 10- to 150-m thick andare made up of bluish green, fine- to medium-grained,well-banded gneiss, and has transitional contacts with themarbles. The upper part of the Fındıklı formation is madeup of an augen-gneiss horizon, 10- to 30-m thick.

GEOLOGY OF THE KAZDA⁄ MASSIF

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Figure 3. Generalised stratigraphic section of the Kazda¤ Group.

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Amphiboles are ubiquitous in gneisses of the Fındıklıformation; the next most common mafic minerals areepidote in the lower levels, mica in the intermediatelevels, and garnet in the upper parts of the formation.

The marbles in the Fındıklı formation form six toseven horizons, 10 to 75 m in thickness (Figures 4 & 5).The structurally highest marble horizon immediatelybelow the metaophiolites forms a distinct marker horizonand is named the Babada¤ marble member. The othermarble horizons in the Fındıklı formation are ascribed tothe Altınoluk marble member. The marble occurs aswhite, fine- to medium-grained, thin- to medium-bandedrocks with a sugary texture. The Babada¤ marble horizondiffers from the other marble horizons by being moremassive and coarser grained.

Tozlu Formation

The Tozlu Formation, which consists of meta-ophioliticrocks, has been named by Bingöl et al. (1975). It cropsout in the summit region of Kazda¤ (Figure 5), and itstype locality is in the Tozlu Yayla. The Tozlu formationconsists mainly of metadunite and amphibolite. Theserock types are typically intimately intermixed; however,there is a tendency for the amphibolites to dominate inthe lower and upper levels of the formation, and themetadunites in the central part. Tight to isoclinal foldingis widespread in the banded amphibolites andmetadunites. Coarse-grained amphibolites generally havestreaky or spotted textures resulting from thepreferential distribution of hornblende and plagioclase inthe rock. These orthoamphibolites, which have developthrough the metamorphism of gabbroic and other basicmagmatic rocks, have been referred to in former studiesas metagabbros (Bingöl 1968, 1969; Bingöl et al. 1975).

In previous studies, meta ophiolites of the Tozluformation were regarded as the base of the Kazda¤Group. However, our mapping has shown that the Tozluformation lies above the Babada¤ marble member of theFındıklı formation, probably with a pre-metamorphictectonic contact, and is overlain by the Sarıkız marble(Figures 4 & 5).

Sarıkız Marble

The Sarıkız marble, which consists predominantly ofmetacarbonates, was named by Bingöl et al. (1975). TheSarıkız marble has an atoll-like outcrop pattern (Figure 4)

as a result of the antiformal structure of the Kazda¤Group, and crops out mainly on the Sarıkız and Nenekırıhills and at the Ayazma locality.

The Sarıkız marble starts above the metaophiolites ofthe Tozlu formation with a thin paragneiss layer. At a fewlocalities, such as immediately north of Tozluyayla on theKazda¤ road, metaconglomerates with clasts derivedfrom the ophiolites have been recognised, althoughbecause of high-grade metamorphism and strongdeformation it is difficult to be certain on the nature ofthe protolith. The paragneisses pass gradationally upwardinto marbles, which form a single horizon 25- to 100-mthick. The marble is fine- to medium- grained, and ismedium- to coarse-banded. The carbonates locallycontain siliceous nodules 3- to 5-cm long. The uppercontact of the Sarıkız formation with the Sutuvenformation is sharp.

Sutuven Formation

Gneisses in the uppermost part of the Kazda¤ Group havebeen named the Sutuven formation. The Sutuvenformation corresponds to the “silico-aluminous series” ofBingöl (1968, 1969) or the Boza¤açtepe formation ofBingöl et al. (1975). The Sutuven formation rests with asharp contact on the Sarıkız marble and Fındıklıformation. It is in fault contact with surrounding Permianto Miocene rocks, and is intruded by Oligo–Miocenegranodiorites.

The type locality of the Sutuven formation is in theSutuven waterfall north of the village of Zeytinli. Most ofthe northern parts of Kazda¤ is underlain by the Sutuvenformation. The Sutuven formation comprises mainlygrey, dark grey, and brown, well-banded quartzo-feldspathic gneisses. These gneisses, which constitute thedominant lithology, comprise thin marble, amphiboliteand granitic gneiss horizons and lenses. Furthermore,migmatisation is widely observed in gneisses of theSutuven formation. Gneisses of the Sutuven formationare petrologically characterized through the presence ofbiotite, sillimanite, garnet, and hornblende along withubiquitous quartz and feldspar.

The continuous, NE–SW-trending orthogneiss band inthe northern and northwestern parts of Kazda¤ cuts thegneisses of the Sutuven formation but at the same timeshows banding and lineation subparallel to that of theneighbouring gneisses. The Oligo–Miocene granodiorites,

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which crop out northwest of the Kazda¤ Group, generallydo not show any banding or lineation. This suggests thatthe orthogneisses intruded the Sutuven formation priorto the last phase of metamorphism. However, Okay &Satır (2000) have mapped banding and lineation in theOligo–Miocene Evciler granodiorite along its southerncontacts with the Sutuven formation; the banding andlineation in the granodiorite are reportedly subparallel tothat in the neighbouring gneisses.

Discussion and Conclusions

In this study the Kazda¤ Group, consisting of high-grademetamorphic rocks, has been subdivided into fourformations. These are, in ascending order, the Fındıklıand Tozlu formations, the Sarıkız marble and the Sutuvenformation. In previous studies the metaophiolites, whichmake up the Tozlu formation, were regarded either asthe structurally lowest unit in the Kazda¤ Group (Bingöl1968, 1969; Bingöl et al. 1975) or as the uppermostunit (Gözler et al. 1984). Our geological mapping hasshown that the metaophiolites are underlain by anamphibole-bearing gneiss – marble unit (Fındıklıformation) and are overlain by the Sarıkız marble.

Metamorphism in the Kazda¤ Group has been datedusing zircon Pb-Pb and mica Rb-Sr and K-Ar methods ongneisses from the Fındıklı and Sutuven formations. Thezircon Pb-Pb data from the gneisses yieldMid–Carboniferous ages (308 ± 16 Ma, Okay et al.1996), whereas the biotite and muscovite Rb-Sr and K-Ar ages are Oligo–Miocene (19–22 Ma, Bingöl 1968,1969; Okay & Satır 2000). These isotopic data have beeninterpreted as indicating two periods of high-grademetamorphism; the initial one during theMid–Carboniferous and a later one in the Oligo–Miocene.The P-T conditions of the high-grade metamorphism have

been estimated as 640 ± 50 °C and 5 ± 1 kbar (Okay &Satır 2000).

The metaophiolites of the Tozlu formation and theSarıkız marble pinch out toward the west, where theSutuven formation directly overlies the Fındıklı formation(Figures 2 & 4). This relationship suggests the presenceof tectonic contacts between the Fındıklı and Tozluformations, and between the Sarıkız marble and theSutuven formation. However, any such tectonic contactsmust pre-date the last phase of high-grademetamorphism, since foliation and lineation in theseformations are all subparallel.

Metamorphic rocks of the Kazda¤ Group form ananticlinorium with an axis that trends NE–SW. Thecontacts of the Kazda¤ metamorphic rocks with thesurrounding sedimentary, magmatic and metamorphicrocks are generally low-angle normal faults ofdetachment-fault character. The detachment faults dipnorthward to the north of the Kazda¤ anticlinorium, andsouthward to the south of the Kazda¤ anticlinorium. Thedetachment faults are cut by strike-slip faults on thenorthwestern and southeastern limbs of theanticlinorium. In so far as clasts of the Kazda¤metamorphic rocks are found only in the Pliocenedeposits, the exhumation of Kazda¤ can be identified as aPliocene event, as suggested by Okay & Satır (2000).

Acknowledgements

This study was conducted as a part of a joint MTA-‹TÜproject entitled “The Economic and EnvironmentalGeology of the Biga Peninsula”. We thank Aral Okay,Neflat Konak, Behçet Akyürek and Yurdal Genç fordiscussions in the field.

M. DURU ET AL.

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ASLANER. M. 1965. Etude geologique et petrographique de la regiond’Edremit-Havran. Maden Tetkik ve Arama Enstitüsü, PublicationNo. 119.

B‹NGÖL, E. 1968. Constribution a l’ etude geologique de la partie centraleet Sud-Est du masif de Kazda¤ (Turquie). PhD Thesis, Universitede Nancy, France.

B‹NGÖL, E. 1969. Kazda¤ Masifi’nin merkezi ve güneydo¤u kesimininjeolojisi [Geology of central and southeastern parts of the Kazda¤Masif]. Maden Tetkik ve Arama Enstitüsü (MTA) Dergisi 72,110–123 [in Turkish with English abstract].

B‹NGÖL, E., AKYÜREK, B. & KORKMAZER, B. 1975. Biga Yarımadasınınjeolojisi ve Karakaya formasyonunun bazı özellikleri [Geology ofBiga Peninsula and characteristics of Karakaya formation].Cumhuriyetin 50. Yılı Yerbilimleri Kongresi Tebli¤ler Kitabı,Maden Tetkik ve Arama Enstitüsü Yayını, 70–76 [in Turkish withEnglish abstract].

GEIS, H. 1953. Kuzey Kazda¤ın Jeolojik Yapısı [Geology of NorthernKazda¤]. Maden Tetkik ve Arama Enstitüsü, Report No. 2250 [inTurkish, unpublished].

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