Presence and tectonic significance of Cretaceous rudist species in the so-called Permo-Carboniferous Göktepe Formation, central Menderes metamorphic massif, western Turkey

Int J Earth Sci (Geol Rundsch) (2003) 92:397–404DOI 10.1007/s00531-003-0333-z

O R I G I N A L P A P E R

Sacit �zer · Hasan S�zbilir

Presence and tectonic significance of Cretaceous rudistspecies in the so-called Permo-Carboniferous G�ktepe Formation,central Menderes metamorphic massif, western Turkey

Received: 17 January 2002 / Accepted: 21 March 2003 / Published online: 17 June 2003� Springer-Verlag 2003

Abstract A schist sequence of the central MenderesMassif, in which lenses of fossiliferous marbles are found,is observed in the southern flank of the Aydın Mountain,north of K�sk (Aydın), around Egrikavak village. Theserocks have been considered as Permo-Carboniferous inage and are included in the G�ktepe Formation of earlierstudies. However, some rudist species are described fromthickly bedded gray marbles that have a concordantcontact with the overlying schist sequence. Although therudists have been metamorphosed, it is observed thatsome contain fossils are well enough preserved todetermine the following rudist fauna: Hippuriteslapeirousei (GOLDFUSS), Hippurites nabresinensisFUTTERER, Hippurites cf. colliciatus WOODWARD.This rudist fauna dates the schist sequence as Santonian–Campanian. The schist sequence is overlain by a thicktectonostratigraphic pile of orthogneiss which has beeninterpreted as the Pan-African metamorphic core of theMenderes Massif. A widespread cataclastic and myloniticzone is present between the underlying rudist-bearingmarbles and the structurally overlying orthogneiss se-quence. The existing kinematic studies in the footwall andhangingwall of this tectonic contact reveal two differentphases of deformations, a contractional phase followed byan extensional phase. During the contractional event,which occurred at 36 Ma, the orthogneiss sequence wasthrust faulted northwards over the schist sequence. Thisthrust fault was later reactivated as a low-angle normalfault beneath a supradetachment sedimentary basin ofEarly-Middle Miocene age. The fossil discoveries of thisstudy and the existing kinematic studies reveal that a newstructural model for the central Menderes Massif in whichthe tectonometamorphic units form a major southwardclosing recumbent fold needs to be reviewed.

Keywords Central Menderes Massif · Stratigraphy ·Rudist · G�ktepe Formation

Introduction

The Menderes Massif is an extensional metamorphic corecomplex (Bozkurt and Park 1994; Hetzel et al. 1995) inthe western Anatolian extensional province (Seng�r1987). Two different stages of crustal extensional events,namely an extensional collapse followed by a rift stage,characterize the province (Seyitoglu et al. 1992; S�zbilirand Emre 1996; Ko�yigit et al. 1999; Bozkurt 2000; Lipset al. 2001). The Massif itself is bordered by the Izmir-Ankara Zone in the north (Seng�r and Yılmaz 1981), andby the Lycian nappes in the south (de Graciansky 1972).

A sequence of high-grade metamorphic core rocksoverlain by a low-grade metamorphic cover has long beenaccepted as the stratigraphy of the Menderes Massif(Schuiling 1962; D�rr 1975; �aglayan et al. 1980; Seng�ret al. 1984; Dora et al. 1990). However, recent studieshave provided evidence that the core sequence is not thelowest structural unit of the Menderes Massif, but isemplaced above a younger cover sequence (Candan et al.1992; Hetzel et al. 1995, 1998; Emre and S�zbilir 1997;Gessner 2000; Lips et al. 2001). This phenomena isparticularly well observed in the central Menderes Massif(Fig. 1).

Okay (2001) has claimed that the central Menderes isan inverted metamorphic sequence, and proposed a newand provocative structural model that is characterized bya large-scale recumbent anticline having a core ofPrecambrian–Cambrian orthogneiss. According to Okay,the overturned limb of the fold consists of an invertedsequence of fusulinid-bearing G�ktepe Formation and theconformably overlying schist sequence in the AydınMountain. He claimed that recrystallized dark limestonesof the G�ktepe Formation carry brachiopods, algae andfusulinid-type foraminifera attesting to a Permo-Car-boniferous age, without giving any names and figures ofthe mentioned fossils. However, we have discovered for

S. �zer · H. S�zbilir ())Engineering Faculty, Department of Geology,Dokuz Eyl�l University,35100 Bornova-Izmir, Turkeye-mail: [email protected]: +90-232-3887865

the first time some recognizable rudist species in the so-called G�ktepe Formation, which forms the southernflank of the Aydın Mountain in an area south ofEgrikavak village (Fig. 2).

The aim of this study is to present new palaeontolog-ical evidence supporting the Late Cretaceous age of theso-called G�ktepe Formation, and to show its importancein the tectonic evolution of the Menderes Massif.

Stratigraphy and palaeontology

The structural studies of the rocks exposed aroundEgrikavak village, an area north of K�sk (Aydın), revealtwo distinct tectonostratigraphic units that are separatedby a low-angle normal fault (Fig. 2). The structurallylower sequence has recently been named the G�ktepe

Formation by Okay (2001). It is characterized by a thick-bedded marbles at the bottom followed by a succession ofschist intercalated with marbles towards the top. Thethick-bedded marbles, up to 200 m thick, are exposedalong the Ko�ak stream southeast of Egrikavak village.

New occurrences of rudists have been found in themarbles (Fig. 3). The rudist fauna consist mainly ofhippuritids such as Hippurites lapeirousei (GOLDFUSS),Hippurites nabresinensis FUTTERER, Hippurites cf.colliciatus WOODWARD. Some indeterminable radioli-tid sections (Durania sp., Sauvagesia sp.) are alsoobserved. These hippuritid species are well known andhave been identified in Santonian-Campanian marbles ofthe southern sector of the Menderes Massif, around theAkb�k-Milas and Yatagan-Kavaklıdere areas (�zer 1993,1998; �zer et al. 2001).

Fig. 1 Simplified geologicalmap of the central and southernMenderes Massif (compiledfrom �aglayan et al. 1980; Doraet al. 1990, 1995; Gessner 2000;�zer et al. 2001; Okay 2001).Inset shows location of Fig. 1.The geology of the framed areais indicated in Fig. 2

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Hippurites nabresinensis has been reported from theSantonian–Campanian megablock limestones of theIzmir-Ankara zone (�zer 1989) and is found also fromthe Santonian–Campanian limestones of Slovenia, Croa-tia, Austria, Italy and Romania (Milovanovic 1934;Plenicar 1960, 1975; Lupu 1976; Polsak 1979; Accordi

et al. 1982). This species has also been identified inMaastrichtian limestones of Bosnia (Sladic-Trifunovic1972) and Bulgaria (Pamouktchiev 1981).

Hippurites lapeirousei is widespread in the Campani-an–Maastrichtian of the Mediterranean province (Sanchez1981). Hippurites colliciatus is found from the Santonian

Fig. 2 Detailed geological mapof the Egrikavak area, north ofK�sk (Aydın) (modified fromEmre and S�zbilir 1997 andown field observations). A–Brefers to cross section in Fig. 4

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of Austria, Italy (Apennines), Yugoslavia (Dinarids),Romania, Greece and Iran (Sanchez 1981), the Campa-nian–Maastrichtian of the Apennines (Cestari and Sirna1989), Carpathians (Andrusov 1976) and in Tunisia(Negra and Philip 1986), and from the Middle Campanianof Bulgaria (Swinburne et al. 1992), and Maastrichian ofsouthern Italy (Borgomano and Philip 1989). This speciesis also present in Upper Senonien limestones of Turkey(Karacabey 1968; �zer 1994; Steuber et al. 1998; Fenerci1999). The reported rudist species indicates a Santonian-Campanian age for the marbles of the Egrikavak area.

The rudist-bearing marbles are tectonically overlain bya thick gneiss sequence (Figs. 2, 4) that consistsdominantly of bluish augen gneiss in which an older

granitic texture can be recognized. In the sequence, rarebiotite schists and metagabro lenses were also observed(Candan et al. 1992; Oberhansli et al. 1997, 1998). East ofEgrikavak village, near Bas�ayır, a sedimentary sequenceof Early-Middle Miocene age (Emre and S�zbilir 1997;Akg�n and Akyol 1999) is exposed above both the rudist-bearing sequence and the gneiss sequence (Emre andS�zbilir 1997). The sedimentary sequence rests uncon-formably on the gneiss sequence, but is in fault contactwith the underlying rudist-bearing sequence (Fig. 2).

The contact between these two tectonostratigraphicsequences is the previously documented south-dippingB�y�k Menderes detachment fault (also termed theBas�ayır detachment by Emre and S�zbilir 1997, and

Fig. 3 Field photographs illus-trating several rudist sectionsfrom the marbles, south ofEgrikavak village. 1 Marblesconsist of many hippuritid sec-tions. Some sections (arrows)show the characteristic siphonalpillar features of Hippuriteslapeirousei (GOLDFUSS).Scale bar 5 cm. 2 Marbles withhippuritid sections (arrows).Scale bar 4 cm. 3 Hippurites cf.colliciatus WOODWARD.Transverse section of the lowervalve. Note the preservation ofridge costae (arrows). Scale bar5 cm. 4 Marbles including hip-puritid sections (thin arrows)and transerve section of thelower valve of Hippuritesnabresinensis FUTTERER(thick arrow). Scale bar 1 cm. 5Hippurites lapeirousei (GOLD-FUSS). Transverse section ofthe lower valve. Scale bar 1 cm.6 Hippuritid section showingpartly preserved siphonal pillars(arrows). Scale bar 1 cm. 7Hipputitid sections belongingprobably to Hippuriteslapeirousei (GOLDFUSS) (ar-rows). Scale bar 1 cm. 8 Hip-purites lapeirousei(GOLDFUSS). Transverse sec-tion of the lower valve. Noteslightly developed siphonal pil-lars. Scale bar 4 cm. 9 Marbleswith many hippuritid section,Scale bar 4 cm. 10 Marblesshowing the transverse sectionof the lower valve of Hippuriteslapeirousei (GOLDFUSS) (ar-rows). Scale bar 3 cm. 11Hippurites nabresinensis FUT-TERER. Transverse section ofthe lower valve. The siphonalpillars are clearly observed.Scale bar 2 cm

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the G�ney detachment by Ring et al. 1999) that definesthe northern margin of the Miocene supradetachmentbasin (Lips et al. 2001). The B�y�k Menderes detachmentfault is characterized by semiductile to brittle faultbehavior (Lips et al. 2001). The ductile fabrics indicatea northward tectonic transport of the hangingwall gneisssequence (Fig. 4) above the rudist-bearing sequence andpre-date subsequent top-to-south detachment faulting(Lips et al. 2001).

Discussion and conclusion

The stratigraphy of the Menderes Massif was basedprincipally on the metamorphic sequences of the �inesubmassif where a Pan-African core sequence is overlainby a Palaeozoic-Mesozoic metasedimentary cover se-quence. The core sequence is characterized by polyphasedeformational events (Dora et al. 1995) and consists ofmetagranite, paragneiss, schist and migmatite. The oldestdated geological event in the core rock assemblage wasthe intrusion of the granites at ~550 Ma (Loos andReischmann 1999; Hetzel and Reischmann 1996; Hetzelet al. 1998). These granites were subsequently trans-formed to augen gneisses within the �ine submassif.

The overlying metasedimentary cover sequence con-sists, from bottom to top, of garnet micaschist, mica schistand quartzite with intercalations of Permo-Carboniferousblack marble, a thick succession of Mesozoic emery- andrudist-bearing marble, and Palaeocene flysch-like sedi-

ments (D�rr 1975; �aglayan et al. 1980; Seng�r et al.1984; Okay 1985, 1989; Konak et al. 1987; Dora et al.1995; �zer 1998, 1999; �zer et al. 2001).

This study reveals the presence of rudist species of aSantonian-Campanian age in the cover series of thecentral Menderes Massif (Fig. 5), north of K�sk (Aydın);these rocks were originally mapped and correlated withthe Permo-Carboniferous G�ktepe Formation by Okay(2001). Equivalent units consisting of a schist sequencewith marble intercalations and rudist-bearing marbles arealso well exposed in the southern sector of the MenderesMassif around Yatagan-Kavaklıdere (�zer 1998; �zer etal. 2001).

The type G�ktepe Formation was described from theG�ktepe region, north of Mugla, where it consists ofbituminous and fossiliferous dark marble intercalated inschist and quartzite (�nay 1949; Schuiling 1962;�aglayan et al. 1980). In this type area, Carboniferousand Permian fossils were found and described from themarbles. Equivalent units were also defined in theBabadag region, southwest of Denizli (Okay 1985) wherean alternation of micaschist, quartzite and black marbledefine the Karıncalıdag Formation (Okay 1985, 1989).The black marbles contain gastropods, crinoids andforaminifera, indicating a Permo-Carboniferous age. Thisunit is conformably overlain by Mesozoic dolomiticmarble of the Yılanlı Formation.

The contact relationship between the Pan-African coreand the overlying Paleozoic-Mesozoic cover sequence inthe southern Menderes Massif has not yet been resolved.

Fig. 4 Geological cross sectionshowing the contact relation-ships between the rudist-bearingfootwall rocks and the struc-turally overlying gneiss se-quence (see Fig. 2 for locationof the section). Note the reacti-vated nature of the B�y�kMenderes detachment fault. Thefootwall rocks were mapped asthe Permo-Carboniferous G�k-tepe Formation in Figs. 2 and 4of Okay (2001)

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According to D�rr (1975), �aglayan et al. (1980), Seng�ret al. (1984), Konak et al. (1987) and Dora et al. (1990,1995), the basal part of the cover sequence in the southernMenderes Massif is characterized by a metaconglomeratethat contains clasts derived from the core series. However,Bozkurt and Park (1994) claimed that the so-called coremetagranite is, in fact, a synextensional granite intrudedinto the overlying cover schist along a top-to-southextensional shear zone during the Late Oligocene.Recently, Ring et al. (1999) argued for the same contactas a thrust fault.

The contact between the core and the cover sequencehas also been observed on the central Menderes Massif,but with a reverse stratigraphic order, where the oldercore units were emplaced on the younger cover sequence(Fig. 5; Candan et al. 1992; Emre and S�zbilir 1997;Hetzel et al. 1998; Lips et al. 2001; Okay 2001). Tectonicklippen of the gneissic basement have been reported ontop of the cover sequence in the central submassif, southof Salihli (Hetzel et al. 1995; Emre and S�zbilir 1997) andnorth of Aydın (Candan et al. 1992; Emre and S�zbilir1997). Although the contact south of Salihli has beendescribed and accepted as a detachment fault (Hetzel etal. 1995; Emre and S�zbilir 1997; Hetzel et al. 1998; Lipset al. 2001; S�zbilir 2001), the contact north of K�sk hasbeen interpreted both as a thrust fault (Candan et al. 1992;Dora et al. 1995; Okay 2001) and a low-angle normalfault (a reactivated thrust fault, Emre and S�zbilir 1997;Lips et al. 2001; Gessner et al. 2000).

Northward tectonic transport by thrust faultingthroughout the core sequence has been documented byHetzel et al. (1998), Ring et al. (1999) and Lips et al.

(2001). The timing of this tectonic event was interpretedto be Pan-African (Ring et al. 1999) or Alpine (Hetzel etal. 1998; Lips et al. 2001) in age. The presence of rudistsin the underlying marble indicates that the emplacementof the gneiss sequence over the rudist-bearing coversequence must have occurred after the Late Cretaceous,probably at ~35–40 Ma, a time of imbrication of theMenderes sequence by northward directed thrusting (Lipset al. 2001). During the extensional collapse of the Lycianorogen (Collins and Robertson 1997, 1998, 1999) in thelatest Oligocene to Early Miocene (Seyitoglu et al. 1992),some of these thrust faults were reactivated as low-anglenormal faults (or detachment faults) beneath majorsupradetachment basins. Lacustrine supradetachment ba-sin fill deposits rest unconformably on the hangingwallgneiss sequence, but are in fault contact with theunderlying rudist-bearing footwall sequence. This suggestthat the gneiss klippen together with the overlyingsynextensional sedimentary sequence have been trans-ported as extensional allochthons (Emre and S�zbilir1997) towards the south along the B�y�k Menderesdetachment fault.

Acknowledgements This study was supported by the Scientific andTechnical Research Council of Turkey, project no YDAB�AG-279. The authors would like to thank Dokuz Eyl�l University fortheir financial contribution to fieldwork. An earlier version of themanuscript were improved by critical and helpful reviews by G. A.Davis and B. Clark Burchfiel.

Fig. 5 Stratigraphic columnarsection of the study area and itscorrelation with that of Okay(2001)

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