The Problem of the Core—Cover Boundary of the Menderes ...journals.tubitak.gov.tr/earth/issues/yer-04-13-1/yer-13-1-2-0310-5.pdf · with a regionally metamorphosed rock succession

Turkish Journal of Earth Sciences (Turkish J. Earth Sci.), Vol. 13, 2004, pp. 15-36. Copyright ©TÜB‹TAK

15

The Problem of the Core–Cover Boundary of the MenderesMassif and an Emplacement Mechanism for RegionallyExtensive Gneissic Granites, Western Anatolia (Turkey)

BURHAN ERDO⁄AN & TAL‹P GÜNGÖR

Dokuz Eylül University, Department of Geological Engineering, TR–35100 Bornova, ‹zmir - Turkey(e-mail: [email protected])

Abstract: In previous studies, the stratigraphy of the Menderes Massif was divided into a Precambrian core andMesozoic cover associations, the core consisting of gneissic granites and high-grade schists and the cover of micaschists and platform-type marbles. It has also been proposed that the two associations are separated by anunconformity although nowhere is this relation clearly observed.

In this study, the Bafa and Kavakl›dere areas in the southern part of the massif have been examined. In theBafa area, Mesozoic mica schists with marble lenses occur in the lowermost parts of the sequence and are overlain,along a gradational boundary, by a Mesozoic carbonate succession. Gneissic granites cut the detrital parts of thisMesozoic succession and the boundary is clearly intrusive, characterised by enclaves of schist within the granitebody and seams and veins of granite cutting the surrounding mica schists. In the Kavakl›dere area, Mesozoicmetaclastics and platform marbles are underlain by the Permo-Carboniferous Göktepe Formation which consistsof black marble, chert and quartz-mica schist intercalations. The gneissic granites in this region also have intrusivecontact relations with surrounding rocks and cut the Göktepe Formation.

The granites were emplaced syntectonically during the main Menderes metamorphism which took place in LateCretaceous–Early Cenozoic time and included strongly assimilated mica schist zones and patches. These granitesare geochemically S-type, peraluminous and of syn-collisional character.

The subdivision of the stratigraphy of the massif into core and cover associations based on the position of thegneissic granites is incorrect. The Lycian Nappes were thrust northward coevally with the main Menderesmetamorphism, and the Menderes platform was recumbently folded. Along the cores of these north-verging folds,granitic melts were emplaced syntectonically and strongly assimilated, and rejuvenated the lower parts of theplatform sequence. Inversion of the metamorphic grade and vertical repetition of gneisses and mica schists in someareas are consequences of recumbent flow folding.

Key Words: gneissic granites, syntectonic granites, Menderes Massif, western Anatolia

Menderes Masifinde Çekirdek–Örtü Problemi ve Bölgesel Ölçekli Gnaysik Granitlerin Yerleflim Mekanizmas›

Özet: Menderes Masifi’nin stratigrafisi önceki çal›flmalarda Prekambrien çekirdek ve Mesozoyik örtü topluluklar›olmak üzere iki ana bölüme ayr›lm›fl, çekirdek bölümünün gnaysik granitler ve yüksek dereceli flistler, örtüserilerinin ise flisler ve platform türü mermerlerden olufltu¤u belirtilmifltir. Ayr›ca, çekirdek ve örtü topluluklar›n›nbirbirlerinden aç›sal uyumsuz dokanak boyunca ayr›ld›¤› ileri sürülmesine ra¤men bu iliflki hiçbir yerde aç›k olarakgözlenememifltir.

Bu çal›flmada Menderes Masifi’nin güney bölümünde bulunan Bafa ve Kavakl›dere alanlar› incelenmifltir. Bafaalan›nda mermer mercekleri içeren Mesozoyik yafll› mika flistler stratigrafik olarak alt düzeyleri oluflturur ve üstedo¤ru dereceli bir kuflak boyunca Mesozoyik karbonat istifine geçmektedir. Gnaysik granitler alttaki Mesozoyikk›r›nt›l› düzeyleri kesmekte, dokanak ise intrüsif özelliktedir. Granitler içinde mika flist anklavlar› bulunurken,flistlerden oluflan çevre kayalar›n› kesen granit bant ve damarlar› dokanak boyunca yeralmaktad›r. Kavakl›derealan›nda Mesozoyik yafll› metak›r›nt›l› ve mermer istifinin alt›nda siyah mermerler, çörtler ve kuvars mika flistlerdenoluflan Permo-Karbonifer yafll› Göktepe Formasyonu yeral›r. Gnaysik granitler bu alanda da çevre kayalarasokulmufl, do¤rudan Göktepe Formasyonu’nu kesmektedir.

Granitler sintektonik olarak yerleflmifl olup içirisinde ileri derecede yutulmufl mika flist zon ve yamalar› bulunur.Jeokimyasal özellikleri güney Menderes Masifi’ndeki gnaysik granitlerin S-tipi, peraluminus ve çarp›flma s›ras›ndayerleflmifl granitler oldu¤una iflaret etmektedir. Granitler, Ana Menderes Metamorfizmas› s›ras›nda GeçKretase–Erken Senozoyik döneminde çevre kayalar›n› oluflturan flistlerin içierisine sintektonik olarak

Introduction

In the western part of Turkey, the Menderes Massif –with a regionally metamorphosed rock succession ofgneissic granites, mica schists and massive marbles –forms the structurally lowest tectonic unit, upon whichtectonic slices of mélange rocks of the ‹zmir-Ankara Zonein the north and the Lycian belt in the south lie as nappes(Figure 1).

In previous studies, the stratigraphy of the MenderesMassif has been considered to consist of two major rockassociations; the lower part was named the “core” andthe upper part the “cover” of the massif (Schuiling 1962;Dürr 1975; Dora et al. 1992). The core is consideredPrecambrian in age and the cover Palaeozoic, Mesozoicand Tertiary. The core comprises various types ofgneisses and high-grade schists (Schuiling 1962) and thecover Palaeozoic and Mesozoic schists and marbles. Theintrusion age of the orthogneisses of the core successionhas been determined by radiometric methods to rangefrom 570 to 520 Ma (Hetzel & Reischmann 1996; Loos& Reischmann 1999; Koralay et al. 2001) and 566 to541 (Gessner et al. 2004).

Although the metamorphic rocks of the MenderesMassif crop out extensively in western Turkey, theboundary of the so-called core and cover associations hasnot been observed anywhere nor described unequivocally.In the Kavakl›dere area, the boundary was reported as anunconformity characterised by conglomerate horizonswith clasts of leucocratic magmatic rocks which wereinterpreted to be derived from the underlyingPrecambrian granites (Konak et al. 1987). In the Selimiyeregion along the southern flank of the massif, the sameboundary was described as a shear zone (Bozkurt 1994,1996; Bozkurt & Park 1994, 1997a, 1997b, 1999,2001; Hetzel & Reischmann 1996; Loos & Reischmann1999; Bozkurt & Sat›r 2000; Bozkurt & Oberhänsli2001; Lips et al. 2001; Whitney & Bozkurt 2002), andas an incipient detachment zone along which a younggranite intruded by Bozkurt & Park (1994, 1997a,1997b). There also claims that this contact is a south-

facing thrust fault (Ring et al. 1999, 2001; Gessner et al.2001a, 2001b, 2001c; Régnier et al. 2003). On theother hand, more recently it is suggested that the contactwas contractional with top to the N–NNE sense ofshearing, then inverted to extensional with top to theS–SSW sense of shearing during Eocene–Oligocene times(Lips et al. 2001; Whitney & Bozkurt 2002).

Boray et al. (1973), after mapping a large regionbetween Milas and Tavas along the southern edge of themassif, pointed out that the contact relationship betweenthe core and cover series could only be resolved afterdeciphering the origin of the core gneisses.

The stratigraphy of the upper parts of the massif,which is called the cover succession, is relatively betterknown (Figure 2). The cover series consists, in its lowerhalf, of a very thick succession of mica schists, quartz-mica schists, quartzites, black cherts and lenses of darkgrey marbles. Carboniferous and Permian ages have beendetermined from the fossil contents of marbles in theKavakl›dere area (Önay 1949; Konak et al. 1987; Güngör& Erdo¤an 2001). This Palaeozoic succession isunconformably overlain by a Mesozoic sequence (Konaket al. 1987) which starts at its base with purple to violetsandstones, conglomerates and phyllites (Figure 2).There are thin lenses of dolomitic limestones and maficvolcanic lenses (Güngör & Erdo¤an 2001) in the upperparts of this detrital Triassic succession, whichgradationally passes upward into a thick platform marblesuccession.

Around Milas, the detrital Triassic section includeslenses of quartz conglomerates (Konak et al. 1987) and,around Selçuk, dark gray thinly bedded chertsinterbedded with phyllites, pelagic marbles and maficvolcanic intervals are present (Güngör & Erdo¤an 2001).

The Mesozoic marbles in the southern part of themassif consist of gray and light grey dolomites anddolomitic marbles in the lower part and white to darkgray massive marbles in the upper part of the series(Boray et al. 1973; Dürr 1975; Konak et al. 1987; Özer

GRANITIC GNEISSES OF THE MENDERES MASSIF, W TURKEY

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yerleflmifllerdir. Bu nedenle gnaysik granitlerin konumu esas al›narak yap›lan çekirdek ve örtü s›n›flamas› yanl›flt›r.Likya naplar›, bu s›rada kuzeye do¤ru itilmifl, buna ba¤l› olarak Menderes platformu bölgesel ölçekli k›vr›mlarladeformasyon geçirmifltir. Granitik ergiyikler kuzeye devrik k›vr›mlar›n çekirdekleri boyunca yerleflmifl ve ayn›zamanda platformun alt bölümlerini ergime ve yutmalar yoluyla mobilizasyona u¤ratm›flt›r.

Anahtar Sözcükler: gnaysik granitler, sintektonik granitler, Menderes Masifi, Bat› Anadolu

B. ERDO⁄AN & T. GÜNGÖR

17

Selçuk

Söke

Milas

‹ZM‹R

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normal Fault

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E47º E28º

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‹ZM‹R-ANKARAZONE

Kufladas›

Figure 2 Figure 10

Figure 1. Map showing main tectonic belts of western Anatolia and the location of the study areas.


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1998; Özer et al. 2001). These upper sections includeemery lenses which are interbedded with massive, UpperCretaceous rudist-bearing marbles (Dürr 1975; Özer1998). In the uppermost part of the platform-typemarbles, there are bioclastic and intraformationallimestone breccias that pass gradationally upward intored, green and grey, Campanian–Maastrichtian pelagicmarbles (Dürr 1975; Konak et al. 1987; Özer 1998).The pelagic marbles grade into phyllites and schists withblocks of carbonate rocks, mafic volcanic rocks andperidotites (Konak et al. 1987; Güngör 1998; Güngör &Erdo¤an 2001; Özer et al. 2001).

The regional metamorphism of the Menderes Massif isof the high temperature–medium pressure Barroviantype and is dominantly in the greenschist facies, but inextensive areas it reaches up to amphibolite facies, and ischaracterised by almandine-staurolite-sillimanite-kyanitemineral assemblages (Evirgen & Ataman 1982; Bozkurt1996; Whitney & Bozkurt 2002; Régnier et al. 2003).The eclogite and granulite facies are also reported in closeassociation with gneissic granites and gneisses, and thesehigh-grade metamorphic events have been considered tobe Precambrian (Candan 1994a, 1994b, 1995, 1996;Candan et al. 1998, 2001). It was previously suggestedthat the main metamorphism of the massif was related tocollision in the Early Cenozoic which resulted in the burialof the Menderes platform beneath the load of the LycianNappes and the maximum depth of the burial wasconsidered to be up to 15 km (fiengör & Y›lmaz 1981).The massif was then later exhumed by detachment faultsduring Miocene time (Bozkurt & Park 1994, 1997a,1997b, 1999; Emre & Sözbilir 1995; Hetzel et al.1995a, 1995b, 1998; Koçyi¤it et al. 1999; Bozkurt2000, 2001a, 2001b, 2002, 2003; Seyito¤lu et al.2000, 2002; Ifl›k & Tekeli 2001; Gessner et al. 2001b;Ifl›k et al. 2003; Özer & Sözbilir 2003; Rimmelé et al.2003a, 2003b; Ring et al. 2003; Bozkurt & Sözbilir2004). The E–W-trending graben systems of westernAnatolia are thought to have been initiated in the EarlyMiocene and are still active (Seyito¤lu et al. 1992). But,recent works suggest that the grabens commenced toexistance during the Pliocene and the extension inwestern Anatolia is expressed by two-stage episodic event(see Koçyi¤it et al. 1999; Bozkurt 2000, 2001a, 2001b;Bozkurt & Sözbilir 2004 for further information).

In the present study, the stratigraphy of the core andcover series of the Menderes Massif was studied in the

Bafa and Kavakl›dere areas (Figure 1), and the contactrelations of these two successions were examined. Inthese two different areas, 1/25,000 scale geologicalmapping has been done. The so-called core rocks aretypically gneissic granites in the Bafa area, forming thepronounced granitic topography of the BeflparmakMountains. The contact of the gneissic granites is clearlyobserved and is traceable laterally for long distances. Themap pattern and detailed characteristics of this boundaryprovide evidence that bears on the genesis andemplacement mechanism for granites in the massif. TheBafa area is also of particular interest because the gneissicgranites and the stratigraphically well-known Mesozoiccarbonate succession occur in close proximity to oneanother, and well-defined stromatolitic dolomites of thelower Triassic, and rudist-bearing middle and bioclasticand pelagic facies of the uppermost part of the carbonatesuccession are recognized in spite of metamorphism.

In the Kavakl›dere area, our mapping began in thevicinity of Göktepe (Figure 1), where the cover series hasbeen dated palaeontologically in some detail (Önay 1949;Konak et al. 1987). In the present study, the rock unitscropping out near Göktepe were traced toward thegranite contact. Although the metamorphic gradeincreases and fossils are not preserved near the granitebody, the units are still recognisable on the basis oflithological and facies characteristics.

In this study, we also collected 18 relativelyhomogeneous samples from the gneissic granites in theBafa area and analysed them geochemically to elucidatetheir tectonic settings.

Bafa Area

The Bafa area is located in the southwestern part of theMenderes Massif (Figures 1 & 2). The northern part ofthe study area is underlain by gneissic granites and, in thesouthern and western parts of the area, a thick successionof mica schists and marbles crops out (Figures 3 & 4).

Metasedimentary Succession

Along the Zobran Peninsula (Figure 3), a nearly completeMesozoic carbonate succession is present. The lowerparts of this succession consist of yellowish-greydolomite, green calc-schist and grey mica schist, and thisintercalation passes gradationally downward into mica


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20

Qa

Qa

R

LAKE BAFA

1 km

M

gneissic granites

mica schists

massive marbleswith emery deposits

E X P L A N A T I O N

locations of well-exposedintrusive contact

E

Y

N

Y’

X

X’

Zobran PeninsulaCretaceousJurassic

Triassic

E: emeryM: megalodonR: rudist

N27o33’

N 37o33’

E 27o25’

E 27o25’

XX’

emery deposit

megalodon fossilsmica shists enclaves

granit seams

rudist fossils

marble lense

Bend

in s

ectio

n

WSW ENE SW NEY

Y’

WSW

26

3834

3225

24

29

28

25

25 2554

58

34

23

38

25

35

34

18

48

4234

37

34

16

19

35

41

38

32

3534

ENE

Figure 3. Geologic map and cross sections for the northern margin of the Lake Bafa area. See Figure 2 for location.

schist and quartz-mica schist with scarce lenses of yellowmarble (section X–X’ in Figure 3). There the lowermostmica schists of the platform sequence are cut by thegneissic granites. This crosscutting relationship will bedescribed below. Overlying this lower metaclasticsuccession are light grey dolomites and laminateddolomitic marbles. Primary stromatolitic laminations arestill recognisable in the dolomitic horizon (Figure 4a). Thestromatolitic dolomite horizon contains massive light-grey marble beds. From one of these massive marblebeds we have collected thick-shelled bivalve fossils,probably Megalodon sp. (Figure 4b), which may indicatea Late Triassic–Jurassic age. The upper parts of thesuccession consist of grey and dark-grey massive marbleswith poorly preserved rudist remains (section X–X’ inFigure 3). Interbedded with massive marbles is a 20-m-thick emery lens that extends laterally for 300 m. Thispart of the carbonates resembles the Upper Cretaceouszone of the Mesozoic Menderes platform (Figure 2). Theuppermost part of the Mesozoic carbonates is shown inFigure 5, in which massive grey marbles host an emerylens and contain poorly preserved rudists. These marblesare overlain by intraformational limestone conglomerateswhich pass gradationally upward into pink pelagicmarbles. This uppermost section of the Mesozoiccarbonate platform is typical in the Menderes Massif, andthe red limestones yield Maastrichtian foraminifers andnannoplankton (Özer et al. 2001). In the map area, thered and pink pelagic limestones are overlain by greenmica schists with quartz conglomerate lenses whichresemble the Selçuk Formation of Late Cretaceous-

?Palaeocene age (Erdo¤an & Güngör 1992; Güngör1998). Above these Upper Cretaceous mica schists is acarbonate nappe, in the lateral continuation of whichmany emery lenses have been excavated. This is a goodexample of imbrication within the carbonate section ofthe Menderes platform along its southern border.

Within the lower parts of the Mesozoic carbonates,there is a mafic volcanic lens (Figure 5), and this horizonwas reported to be Late Triassic in age in the Kavakl›derearea by Güngör & Erdo¤an (2001). The Mesozoiccarbonates vary in thickness laterally and interfinger withmica schists along strike as shown in Figures 3 & 5.

Gneissic Granites

Gneissic granites crop out to the north and northeast ofLake Bafa (Figure 2). The granites are homogeneous andspheroidally weathered; ~N–S-trending vertical crossjoints are recognisable at long distances and form themost diagnostic structure of the gneissic granites. Planarand linear fabrics are present in every outcrop and thesame penetrative foliation and lineation are observed inall road cuts within the Beflparmak Mountains. Theintensity of deformation is uniform throughout thegneissic gneisses, from the border zone to areas manykilometres within the granite body. Deformation of thegranites was described by Bozkurt & Park (1997b) andGessner et al. (2001a).

The granites preserve holocrystalline texture withlarge K-feldspar porphyroclasts and slightly deformed


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MMM

aaa bbbFigure 4. Photographs of the (a) primary structures in the carbonate section of the Menderes Massif and (b) megalodon fossils (M) (Zobran

Peninsula). Hammer in (a) is 33-cm long; pencil in (b) is 13-cm long.

megacrysts (up to 5 cm in length) (Figure 6a, b). Theserocks are two-mica granites and are generally leucocratic.In places, biotite content increases and, thus, the graniticrocks become melanocratic. The compositional changesare diffuse and are not related to different phases ofmagma emplacement. In the contact zone and within thegranite body, widespread engulfment and resorption ofthe mica schists (country rocks) are observed. The micaschists are strongly melted and digested by the granites,

and constitute more than 50 volume percent of theoutcrops of the granitic mass in the Çine region. Alongthe contact zone of the granites in the Zobran Peninsula,resorbed mica-schist enclaves are characteristic (Figure7a, b). Near the resorbed zone, the granite ismelanocratic because of high biotite content, andbecomes leucocratic away from the resorption zones,indicating strong digestion of the country rocks by thegranitic melts.


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LAKE BAFA

Qa

Qa

Bucak

E X P L A N A T I O NQa

gneissic granites


red, pelagic marbles, mica schists

mica schists and phylliteswith metaconglomerate lenses

dolomites and massive marblesalluvium

1 km

N

thrust fault

locations of well-exposed intrusive contact

v v vv v

R poorly-preserved rudist fossils

Tr

MaastrichtianCretaceousJurassicTriassic

?Palaeocene

14

1438

46

16

51

38

5147

44 46

38

4432

46

40

38

44

28

43

32

41

36

26

35

22

v v vv v

R

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E27o32’

N37

o 27’

N37

o 27’

42

inferred thrust fault under alluvium

strike and dipof foliationstrike and dipof beds

44

24

mica schists with mafic volcanic lenses

E

Figure 5. Geologic map of the eastern margin of the Lake Bafa area. See Figure 2 for location.

Although the contact zone of the granite is ill-preserved, there are areas where intrusive andcrosscutting relations are clearly observed (locationsmarked with stars on Figures 3 & 5). The granitesintrude and cut the surrounding mica schists; they alsoinclude schist enclaves of variable sizes (Figure 8a). Someenclaves have sharp boundaries (Figure 8b) where mostare consumed by the granites (Figure 8c). As seen inFigure 8d, enclaves of mica schist are also cut by thingranitic veins.

Within the country-rock mica schists, there are fine-grained, leucocratic granitic seams, and toward the

granite contact the frequency of these seams increases, asis seen to the NW of Bucak village (Figure 5).

The contact along the Zobran Peninsula is intrusiveand is characterised by abundant enclaves of schist. Atthis location, a yellow dolomitic marble lens is cut andengulfed by the granite at the contact (Figure 4a). Thesemica schists and yellow marble lenses pass gradationallyupward into Mesozoic platform-type marbles suggestinga Triassic or Jurassic age for this metaclastic succession.The granites cut these metaclastic rocks and wereemplaced syntectonically during metamorphism anddeformation. The fold vergence of granitic seams


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aaa bbb

lglglg

msmsms

lglglg

msmsms

Figure 6. Photographs of mica-schist enclaves (ms) within coarse-grained leucocratic granite (lg). Note the large feldspar porphyroclasts in theleucogranites. Hammer is 33-cm long.

Figure 7. Photographs of partly digested mica-schist enclaves (ms) within melanocratic granite (mg). The scale bar is 15-cm long.

aaa bbb

mgmgmg

msmsms

mgmgmg msmsms

indicates northward tectonic transport, and the northernlimbs of mesoscopic folds are strongly attenuated (Figure8d).

The contact between the granite and the structurallyoverlying mica schists dips 40º–50º southward nearBucak (Figure 5), whereas it dips eastward or is nearlyvertical in the Zobran Peninsula; farther north the sameboundary is vertical or overturned (Figure 3). Along theoverturned boundary, the granite is intrusive into themica schists and leucocratic aplitic veinlets occurcharacteristically in the mica schists. Similar relationshipshave also been documented by Mittwede et al. (1995a,

1995b, 1997). Also, about 5 km away from the granitecontact, a leucocratic granite apophysis is intrusive intothe schists containing a lense-shaped marble (Figure 2).The marble-bearing schists, at this location, are similar tomarble-schist intercalations of the Mesozoic association.

Toward the contact of the granitic body in the Bafaarea the grade of metamorphism increases most notablyin the mica schists (Baflar›r 1970). The schists aretypically rich in pink almandine and contain coarse micaminerals (biotite and muscovite) within a 300 m-widezone along the granite contact. The index of crystallinityin the mica schists is markedly high. Close to the granite


24

aaa

bbb ddd

SSS

NNN

SSS

SSS

ccc

gggggggggggg

gggggg

msmsms

msmsms

msmsms

msmsms

Figure 8. Close-up views from the gneissic granite and mica schist contact in the Lake Bafa area. (a) Igneous contact between gneissic leucocraticgranites (gg) and the country-rock mica schists. The granites crosscut the main foliation in the schists; (b) leucocratic metagranites (gg)also occur as vein-like bodies intrusive into mica-schist enclave (ms); (c) a close-up view of the intrusive relationship between coarse-grained leucocratic granite and mica schist. Note local occurrence of thin granite seams (S, arrowed) crosscutting the main foliation inthe schists; (d) a sill-like leucocratic granite seam oriented parallel to the foliation in the schist. The field relations are consistent withsyntectonic emplacement. The folded structure is obvious; it is asymmetric with northern limbs thinned, indicating northward tectonicmovement. Man in (a) is 1.70-m tall and hammer in (b-d) is 33-cm long.

contact there are garnet felses (Figure 9), which are micaschists with red almandine crystals up to 8 mm indiameter; garnets make up 40–60% of the rock. Thegarnet felses are exposed along the entire boundary ofthe gneissic granites along the southern flank of theMenderes Massif; they are formed in association with theintrusive body. Both biotite-rich mica schists withabundant granite veinlets/lenses, and red almandine-bearing garnet-mica schists typically occur near thegranite contact. Granite lenses (10–20 cm in diameter)first appear in the mica schists within a 300-m-wide zonealong the granite contact and become abundant towardsthe granite.

Another characteristic feature of the contact zone isthat the boundary is nowhere sharp, but rather irregularwith mica-schist patches/zones interfingering withgranites at all scales. Within such zones, aplitic veins,granitic veinlets concordant with foliation in the schistsand crosscutting granitic veins are common all along thegneissic granite–mica schist contact with no exception.

Both the granites and surrounding mica schists arefoliated, but the boundary zone preserves its primaryintrusive nature, and no sheared zones are present assuggested by Bozkurt & Park (1994), who proposed thatthis zone corresponds to a south-facing extensional shearzone and that the southern Menderes Massif is anincipient core complex. In the area between Lake Bafa andBa¤aras›, the boundary between the schists and thegneissic granite is not only diffuse and gradational, butalso trends NNE and become vertical and is overturned

locally (Figure 3); this observation is not consistent withthe geometry of a proposed south-dipping detachment.

Kavakl›dere Area

In the Kavakl›dere area (Figure 1), a geological map ofthe Göktepe area (about 25 km east of Kavakl›dereoutside of the map area shown in Figure 10) and its closevicinity was prepared. In the Göktepe area, MenderesMassif comprises low-grade metamorphic (lowergreenschist facies) rocks; the metamorphic grade is solow that fossils are preserved and can be observed easilyon weathered surfaces. The metamorphic sequencecommences with black limestones, phyllites, cherts andpink-grey quartzites that make up the fusulinid-bearingPermo-Carboniferous Göktepe Formation (Figure 2).Black limestones that form the uppermost part of theGöktepe Formation, just below the overlying Mesozoicsuccession, yielded Epimastopora sp., Gymnocodiumbellerophontis, Gymnocodium sp., Globivalvulina sp.,Mizzia velebitana, Protonodosaria sp., Pacyphloia ovata,Stafella sp., Nankonella sp., Baisalina sp., Hemigordiussp., Agathammina parilla, Dagmarita chanakchiensis,Dackeralla sp. Frondina permica fossils which areconsistent with a latest Permian age. The crystallinelimestones, however, contain coral, fusulinid and crinoidremains of possibly Carbonifereous–Permian age (Önay1949; Konak et al. 1987). The black cherts are thinlybedded, and are interbedded with phyllites andlimestones. The unit is overlain by Upper Triassic violetsandstones, quartz conglomerates and phyllites thatgrade upward into a thick platform-type dolomiticlimestone succession. In the lowermost part of thedolomitic limestones, there is a mafic volcanic horizonwhere volcanic rocks are intercalated with thinly beddedyellow limestones (Güngör & Erdo¤an 2001). Thelimestone intercalations yielded Lamelliconus multispirus,Lamelliconus sp., and Aulotortus sp. fossils that suggest aLate Triassic age. The platform carbonates host emerylenses, and are interbedded with rudist-bearing UpperCretaceous limestones (Özer et al. 2001). Atop thecarbonate succession, there are thinly bedded pelagicmarbles and mica schists with mafic volcanic andmetaserpentinite blocks (Konak et al. 1987). This unitcomprises the uppermost part of the Menderes platformand is of Late Cretaceous age (Konak et al. 1987;Erdo¤an & Güngör 1992; Özer 1998). The fossiliferousPalaeozoic units in the Göktepe region continue laterally


25

Figure 9. Close-up view of garnet-fels along the contact betweengneissic granite and mica schist to the north of Irmadanvillage (Figure 10). Diameter of lens cap is 5 cm.


26

gneissic granites

?Palaeocene

CretaceousJurassic

Triassic

Perm

o-Ca

rbon

ifero

us

Maastrichtian

strike and dip of foliation thrust faultvertical fault villagestrike and dip of bed28

NW SE

X X’

granite seams

not to scale

mica schists withmafic volcanicintercalations


red, pelagic marbles

mica schists andphyllites with meta-conglomerate lenses

mica schists andblack marbles,metaconglomerate,quartz schists

EEE

2 km

N

MeskenMeskenMeskenYukar›köyYukar›köyYukar›köy

Tilkiler

Eyli

IrmadanKaplanc›kKaplanc›kKaplanc›k

Kad›köyKad›köyKad›köy

‹smail Da¤›

EXPLANATION

location of the well-exposed intrusive contact

E

E

E

E

E

E

E

E

syncline

x

x’

garnet felses

21

28

42

38

44

44

41

3228

35

30

31

24

21

27

18

42

3648 28

3636

44

42

40

36

42

35

32

45

32

N37

o 24’

E28o15’

N37

o 24’

E28o15’

18

18

Figure 10. Geologic map of the Kavakl›dere area.

toward the granite contact (Figure 10). Near the gneissicgranite, the metamorphic grade increases dramaticallyand there are no reported fossils; nevertheless, theirfacies and stratigraphic order are easily recognised.

In the map area (Figure 10), ‹smail Da¤› is underlainby Mesozoic marbles, the upper parts of which containemery zones. Atop these carbonates, pink pelagic marblesand metaserpentinite-bearing Late Cretaceous micaschists are present. West of Kaplanc›k village (Figure 10)below the Mesozoic carbonates, there are mafic volcaniclenses within the metaclastic rocks, which resemble theUpper Triassic detrital unit of the Göktepe area (Güngör& Erdo¤an 2001). Below the metaclastic rocks lie blacklimestones, black cherts, dark-grey mica schists andquartzite intercalations – typical facies of the Permo-Carboniferous Göktepe Formation. In this area,limestones are recrystallised.

At the base of the Göktepe Formation, there areconglomerate horizons around Mesken and Yukar›köyvillages (Figure 10), which were interpreted, by Konak etal. (1987), as basal conglomerates of the cover series.However, these conglomerate horizons are laterallydiscontinuous and lensoidal in shape, pinching out in thequartz-mica schists of the study area. The discontinuousconglomerate lenses are repeated both vertically andlaterally and they are not confined to a distinct horizon.They appear to be formed as channel-fills in the quartz-mica schist matrix and do not resemble a basal

conglomerate. These metaconglomerates include light-grey, elongate and deformed blocks and clasts (Figure11a). Original textures are still preserved in the deformedparticles (Fig 11b) and thin-section study shows that theyare porphyritic-volcanic rock fragments. Phenocrysts ofeasily recognisable euhedral feldspar and quartz grainsare set in a light-grey matrix. The pebbles display typicalvolcanic texture (Figure 11b), and the rocks are identifiedas porphyritic rhyolites. We speculate that these pebblesare similar to rhyolitic volcanic rocks of the LowerCambrian succession known as the Sand›kl› porphyroids(Erdo¤an et al. 1997, 2000, 2001) in the Sand›kl› areaof the Afyon province which lies in Taurus MountainRange (Gutnic et al. 1979). The conglomerates arepolygenic and comprise dark grey chert and quartziteclasts in addition to the leucocratic rhyolites. (there arealso quartz-tourmaline [probably tourmalinite] pebbles!)

The quartz-mica schists continue stratigraphicallydownward until the gneissic granites, where the granitesare intrusive. Along the contact, the granites containabundant enclaves of metaclastic rocks. To the west, thegranite cuts the conglomerate horizons and intrudes thePermo-Carboniferous Göktepe Formation. For example,along the old Çine-Yata¤an road, the granite intrudes theblack chert, phyllite and limestone intercalations of thePermo-Carboniferous Göktepe Formation.

The contact zone of the gneissic granites is bestobserved along a section shown in Figure 10. Thick


27

QQQQQQ

FFF

MxMxMx

MxMxMx

QQQ

MxMxMx

aaa bbb

Figure 11. (a) A close-up view of metaconglomerates in the metasedimentary sequence of the Menderes Massif in the Kavakl›derearea (hammer is 33-cm long); and (b) photomicrograph showing porphyritic texture of the felsic metavolcanic pebbles inthe metaconglomerates. Please note that quartz (Q) and feldspar phenocrysts (F) are surrounded by a microcrystallinematrix (Mx), and a large quartz phenocryst in the central part of the photograph is resorbed (arrowed). Originalundeformed matrix of the volcanic rock is preserved in this embayed area (see arrow). Width of photo is 2 mm.

quartz-mica schists below the Göktepe Formation areexposed at this location. Toward the contact zone, seamsof leucocratic gneissic granite appear in the schists andtheir frequency increases toward the granite; finally, atthe contact, large enclaves of mica schist occur in thegranite. Crosscutting relationships are clearly seen alongthe contact where granitic veins are common and intrudeboth the enclaves and the country rocks. As in the Bafaarea, garnet felses are present in the contact zone.Foliation is characteristic both in the contact zone andwithin the granite body. The granites are of the two-micatype and the relative amounts of white and black micasvaries over short distances so that the colour of thegranite changes from light grey to dark grey. Thesechanges are seen even around engulfed enclaves withdiffuse boundaries.

Geochemistry of the Gneissic Granites

Eighteen samples of granitic rocks from the Bafa areawere analysed (Table 1). Homogeneous granitic outcropsaway from assimilated mica-schist zones were chosen forsampling. Three samples were collected from the apliticphases of the granites that occur in the contact zone andwithin the country-rock mica schists. Two samples weretaken from the typical augen gneisses, 2 km away fromthe contact zone within the granite body. Five samples ofgrey and four samples of leucocratic granite werecollected along a traverse that began at the contact zoneand continued 10 km into the granitic body. An additionalthree samples from tourmaline-bearing, muscovite-richand biotite-rich granites were collected.

The major-oxide analyses were made by atomicabsorption spectrophotometry, and the trace elementswere analysed by X-ray fluorescence in the geochemistrylaboratory of the Geological Engineering Department ofDokuz Eylül University.

In the nomenclatural diagram of Debon & Le Fort(1983) that uses normative values of Si, Ca and alkalicomponents, two aplite samples are defined as tonalite,and the rest (including the third aplite) cluster within thegranite field (Figure 12a). In the diagram of Maniar &Piccoli (1984) which uses major-oxide contents, all of thesamples plot as peraluminous granites (Figure 12b).

The tectonic setting of the samples appears to be syn-collisional based on their major-and trace-elementcontents (Figure 12c, d). The major-oxide compositionsof the samples support an S-type classification of the

granites (Figure 12e) on the diagram of Chappell & White(1974) in agreement with the results of Bozkurt et al.(1992, 1993, 1995).

In both the nomenclature and tectonic-discriminationdiagrams, the granite samples cluster together and do notshow pronounced scatter, indicating close geochemicalaffinity and genetic relationships, as indicated also by fieldstudies.

Discussion and Conclusions

In the Kavakl›dere area, the lowermost part of theMenderes metamorphic rocks consists of a very thickquartzite and mica schist intercalation. There arelensoidal channel-fill conglomerate horizons in the upperpart of this detrital succession. The conglomerates includeabundant rhyolite pebbles which were probably derivedfrom Lower Cambrian units of the Taurus Range(Erdo¤an et al. 1997, 2000, 2001). Although therhyolite clasts are deformed, they still display preservedprimary textures and there is no indication of an earlierhigh-grade metamorphism as envisaged for the so-calledcore association (Konak et al. 1987; Candan 1994a,1994b, 1995, 1996). Overlying the metaclastic sequenceis an alternation of quartzites, mica schists, black marblesand black cherts belonging to the Late Palaeozoic GöktepeFormation. The Mesozoic succession overliesunconformably the Göktepe Formation and isrepresented by a sequence of detrital sediments andplatform-type marbles. In the Bafa area, only the detritaland overlying carbonate rocks of the Mesozoic successionare present.

The gneissic granites syn-tectonically intruded thelower parts of the Triassic detrital sequence in the Bafaarea and the Upper Palaeozoic sections of the Kavakl›derearea during the main Menderes metamorphism, whichoccurred in Late Cretaceous–Early Cenozoic time. Thegranites strongly assimilated the country-rock micaschists, and kilometers-long, strongly resorbed schistpatches are abundant in the granite body. In mostoutcrops, it is quite difficult to estimate how much initialmelt and how much country rock were involved in theproduction of the final granite bodies. The geochemicalstudies we have done, as well as earlier work (Bozkurt etal. 1993, 1995), indicate a peraluminous, S-typeclassification of the granites, suggesting an origin from asedimentary source.


28


29

biot

itele

ucoc

ratic

mus

covi

teto

urm

alin

eap

lite

auge

n gn

eiss

gran

itegr

anite

auge

n gn

eiss

gran

itegr

anite

95-3

995

-40c

95-4

395

-67

95-6

495

-61

95-4

3b95

-45

95-4

695

-47

95-4

995

-59

95-6

395

-65

95-6

695

-48

95-6

295

-68

SiO

271

.88

70.1

272

.79

74.2

377

.74

70.9

374

.95

74.6

076

.49

76.4

973

.82

74.9

373

.21

74.7

278

.74

81.1

673

.84

75.5

3

Al2O

313

.86

14.5

314

.02

13.2

511

.65

14.9

413

.89

13.1

013

.51

12.9

313

.45

13.1

014

.15

12.8

211

.22

11.0

214

.92

13.2

5

Fe2O

3(t)

3.46

3.53

1.69

1.51

1.39

1.80

1.00

2.08

1.30

2.08

1.47

1.59

1.03

1.33

0.94

n.d

0.64

0.82

MgO

1.10

1.06

0.43

0.25

0.23

0.31

0.66

0.36

0.38

0.44

0.44

0.30

0.36

0.15

0.10

n.d

0.28

0.14

CaO

0.17

0.22

0.34

0.44

0.39

0.73

0.26

0.45

0.25

0.48

0.32

0.31

0.27

0.45

0.32

0.20

0.60

0.27

Na 2

O2.

463.

693.

093.

262.

833.

073.

892.

873.

692.

663.

142.

873.

433.

002.

586.

166.

773.

52

K2O

5.12

4.45

6.08

6.39

5.02

7.04

4.20

5.18

5.61

5.58

6.36

5.80

6.62

5.96

5.14

0.57

1.53

5.18

TiO

20.

490.

480.

180.

180.

130.

240.

190.

180.

240.

210.

210.

160.

100.

130.

100.

210.

000.

.00

MnO

0.01

0.01

0.01

0.01

0.01

0.01

0.01

0.01

0.01

0.01

0.01

0.01

0.01

0.01

0.01

n.d

0.01

0.01

LOI

1.39

1.32

0.67

0.40

0.42

0.69

0.80

0.74

0.60

0.83

0.66

0.75

0.42

0.61

0.41

n.d

0.63

0.73

Tota

l99

.94

99.4

199

.399

.92

99.8

199

.76

99.8

599

.57

102.

810

1.78

99.8

899

.82

99.6

99.1

899

.56

99.3

299

.22

99.4

5

Nb

17.4

19.1

11.9

7.9

12.9

13.6

17.8

12.0

16.7

12.3

9.8

11.3

17.4

20.4

12.5

10.7

22.4

16.1

Rb

159.

414

2.6

184.

022

7.6

269.

723

0.1

152.

632

7.1

163.

317

7.3

165.

225

0.3

327.

136

2.9

327.

93.

550

.735

2.3

Sr47

.864

.573

.757

.729

.779

.355

.054

.682

.262

.079

.956

.550

.038

.427

.265

.498

.930

.2

Y48

.338

.027

.046

.140

.754

.441

.332

.335

.742

.635

.037

.143

.657

.052

.94.

13.

838

.6

Zr20

1.3

165.

284

.591

.275

.410

7.1

131.

793

.213

0.7

115.

197

.082

.670

.311

0.3

87.9

123.

242

.249

.2

Ba59

4.2

574.

634

6.1

244.

213

2.4

535.

329

5.5

326.

136

7.1

347.

750

2.0

291.

730

1.3

168.

194

.2-

487.

729

.0

U2.

314

.711

.712

.513

.2-

15.5

40.1

9.5

4.4

11.6

11.0

40.1

4.2

3.6

6.4

26.4

15.0

Th-

--

--

-6.

24.

1-

-9.

38.

94.

1-

-10

.4-

7.5

Ga

21.2

19.0

34.7

20.0

17.5

20.8

18.5

19.4

21.2

15.6

13.8

20.1

22.9

19.4

12.6

17.9

17.9

23.5

Not

e: F

e 2O

3(t)

= T

otal

iron

Tabl

e 1.

W

hole

-roc

k an

alyt

ical

res

ults

of

maj

or o

xide

s an

d tr

ace

elem

ents

of

the

gnei

ssic

gra

nite

s in

the

Baf

a ar

ea.


30

a

300

200

100

0-400 -300 -100 100

tonalite

gran

odio

rite

adam

ellit

e

granite

dioritesyenogranite

gabbro

P=K-(Na+Ca)

Q=S

i/3-(

K+N

a+2C

a/3)

mon

zodi

orite

monzo

diorite

monzogab

bro

monzo

nite

c82746658

1

10

Rb

ppm

VAG

100

1000

Syn-COLG

SiO2 wt%

d

2000

1500

1000

500

00 30002500200015001000500

Mantle fractionates

pre-plate collision

post-collision upliftlate-orogenic

anorogenic

syn-collision

post-orogenic

R1=4Si-11(Na+K)-2(Fe+Ti)

R2=

6Ca+

2Mg+

Al

b

peraluminousmetaluminous

peralkaline

1.51.00.50.4

1.0

1.5

2.0

2.5

A/CNK

A/N

K

e

3.0

1.0

0.00.0 1.2

S-type granitoids

I-type granitoids

Na2O+K2O+Al2O3

Al 2

O3/

CaO

+Na 2

O+K

2O m

olar

augen gneiss

granitegranite with abundant muscovite

granite with tourmaline

geucocratic gneissic granite

aplite

granite with abundant biotite

Figure 12. Geochemical discrimination diagrams for Menderes granites based on major- and trace-element contents. (a) Q vs Pdiscrimination diagram after Debon & Le Fort (1983); (b) Maniar & Piccoli (1989); (c) Rb vs SiO2 diagram after Pearceet al. (1984); (d) tectonic discrimination diagram after Batchelor & Bowden (1985); (e) total alkali diagram after Chappell& White (1974).


31

Figu

re 1

3.Sc

hem

atic

cro

ss s

ectio

ns il

lust

ratin

g m

echa

nism

of

gran

ite e

mpl

acem

ent

in t

he M

ende

res

Mas

sif.

Saka

rya

Cont

inen

t

NS

Mes

ozoi

c pl

atfo

rmca

rbon

ates

Tria

ssic

met

acla

stics

Pala

eozo

ic an

d ol

der

met

acla

stics

fast

ero

sion

fast

ero

sion

‹zm

ir-An

kara

Oce

an

shea

r zo

nes

Bloc

kySe

lçuk

Form

atio

nBl

ocky

Selçu

k Fo

rmat

ion

a

SM

esoz

oic

plat

form

car

bona

tes

fast

ero

sion

Saka

rya

Cont

inen

t

N

Lycia

n Na

ppes

bM

élan

ge r

ocks

of t

he ‹z

mir-

Anak

ara

Zone

dire

ctly

ove

rlay

the

plat

form

car

bona

tes

of th

eM

ende

res

Mas

sif (B

aflar

›r &

Kon

uk 1

981;

Erd

o¤an

& G

üngö

r 19

92)

Mél

ange

roc

ks o

f the

‹zm

ir-An

akar

a Zo

ne d

irect

ly o

verla

y th

e gn

eiss

ic gr

anite

s of

the

Men

dere

s M

assif

(Kay

a 19

81; C

anda

n 19

88)

The southern flank of the Menderes Massif in theMu¤la region is characterised by large-scale, north-vergent overturned folds in the Mesozoic succession(Boray et al. 1973; Konak et al. 1987; Bozkurt & Park1997a, 1997b, 1999; Rimmelé et al. 2003b). Within thegranitic body, the same kind of overturned flow foldinghas been deduced from our large-scale mapping,indicating that the mica schists and gneissic granites areintercalated at map scale. Okay (2001) also notedstratigraphic and metamorphic inversions in the centralpart of the massif around Ayd›n and interpreted thedominant structure as a regional overturned recumbentfold. To the north, in the vicinity of Demiköprü Dam nearDibekda¤ (Figure 1), low-grade mica schists underlie thegneissic granites and their boundary is quite diffuse,characterised by abundant granitic seams in the countryrock. The gradational boundary zone is 4–5 km in width.The same overturned relations are observed alongBozda¤ Mountain north of Ödemifl (Figure 1); there thegneissic granites overlie the mica schists and thegradational boundary is 4–5 km wide. This last area,where gneisses are interlayered with mica schists, hasbeen interpreted as thrust packages (Candan 1995;Koralay et al. 2001), although their boundaries alwaysoccur as wide diffuse zone. In all of these areas, however,the dominant structures are overturned flow folds. Thegranitic melts syn-tectonically intruded along the cores ofantiforms (Figure 13). The emplacement of graniticmagma, which was accompanied by crustal-scalepenetrative deformation and medium- to high-graderegional metamorphism, was aided by zone-melting alongflow folds and shear zones. Syn-tectonic intrusion,crustal-scale shearing and folding produced strongassimilation of the detrital country rocks.

In regions of magma emplacement, the grade of theregional metamorphism becomes higher, passing into amagmatic stage within the granitic bodies. Within thegranitic bodies strongly assimilated mica-schist patches,engulfed diabase and spheroidal mafic bodies and scarcemarble lenses that escaped digestion are preserved. Fromthese partly resorbed mafic bodies, granulitic andeclogitic metamorphic facies have been described mostlyas relict parageneses and have been attributed toPrecambrian events (Candan et al. 2001). Anymetamorphic facies or events described from the granitic-magma emplacement zones would be ill-advised, and thehigh-grade metamorphic events defined for the Menderes

Massif inside the greissic granites would need carefulreexamination.

In only a few areas, such as Lake Bafa andKavakl›dere, the boundary between the granites and micaschists is as narrow as 300–500 m and crosscuttingrelationships are clearly observed. In other areas, thisboundary is as wide as 5 km and is characterised bygradational zones with centimeters- to tens-of-metersthick granites seams which show increasing abundancetoward nearby granitic bodies. In the Çine region,sillimanite-bearing brown rocks with pronouncedpolygonal texture (previously termed “leptites”; Dora etal. 1988) are abundant. In fact, they are migmatites thatwere nearly melted and crystallised with a polygonaltexture. Zircons from these migmatites and from granitesthat clearly cut the same rocks yield nearly the same ages(~540 Ma), as reported by Hetzel & Reischmann (1996)and Reischmann et al. (2000); this situation is due toresorption and rejuvenation of the earlier detrital rocksby granite melt. The same age discrepancies are notedalong the southern flank of the massif between thequartzites and the gneissic granites. They have yieldednearly the same ages, and Reischmann et al. (2001) havetended to interpret these discrepancies as an indication ofan unconformity, meaning that the 540 Ma granites wereeroded and the quartzites deposited unconformablyabove them. However neither in that area nor anywhereelse in the Menderes Massif are any metaclastic rocksfound overlying the gneissic granites along a stratigraphicboundary; rather, the boundaries are intrusive andgranites always cut the surrounding schists. The closezircon ages between the granites and the adjacent quartz-mica schists are most probably due to assimilation of thedetrital succession by granitic melt and rejuvenation ofthe country rocks. The strong assimilation of countryrocks is clearly noted in the results of zircon-age studies(Koralay et al. 2001). In every sample of granite collectedfrom contact zones or from far inside the granitic bodies,zircon ages always show pronounced scatter.

The oldest parts of the Menderes metamorphicsshould be studied in areas away from gneissic graniteintrusions. One of the best areas is the Mahmut Da¤›region (Erdo¤an & Güngör 1992) where Mesozoicmarbles form a huge E–W-trending anticline, in the coreof which there is a detrital succession consisting ofquartzites, mica schists, cherts, scarce grey marble lensesand mafic metavolcanics, together attaining a thickness of3–4 km.


32

During the main Menderes metamorphism, tectonictransport along the southern flank of the massif wasnorthward as the geometry of large-scale folds andkinematic studies of the sole of the Lycian Nappes indicate(Boray et al. 1973; Konak et al. 1987; Bozkurt & Park1997a, 1999; Arslan 2001; Rimmelé et al. 2003b).During this folding, granitic melts intruded the cores ofantiforms at deeper crustal levels where remobilisation ofcrustal rocks was taking place (Figure 13). Emplacementof granitic melts produced additional thermal fronts inthe core zones of antiforms in addition to the overallregional metamorphism. Tectonic transport accompaniedby magma injection produced intensive penetrativedeformation and stretching lineations throughout themassif.

The gneissic granites underlie a vast area of theMenderes Massif, and we believe that production of sucha large volume of granitic melt requires, besidesrejuvenation, some kind of subduction below theMenderes platform. In the northern part of the MenderesMassif near Demirci and Akhisar, non-metamorphicophiolitic mélanges lie directly on regionallymetamorphosed rocks as klippen (Baflar›r & Konuk 1981;Kaya 1981; Candan 1988; Erdo¤an & Güngör 1992).There probably was a south-dipping subduction zonealong the northern border of the Menderes platformwithin Neotethys. As the Sakarya and Menderesplatforms (lying on either side of this ocean) collided bysubduction (probably both northward below the SakaryaContinent and southward below the Menderes platform),mélange prisms formed along the subduction zone andwere thrust southward atop the relatively early-formedMenderes metamorphic rocks. Subduction along thenorthern border, accompanied by northward thrusting ofthe Lycian Nappes along the southern border, generated

granite emplacement, regional Barrovian metamorphismand intense ductile deformation of the Menderesplatform.

In the proposed subduction model of the metamorphicand deformational evolution of the Menderes Massif,there is no need for deep burial of the platform by theload of nappe packages. Thus, the exhumation of theMassif would be accomplished solely by erosion withoutextensive tectonic denudation envisaged in the earliermodels (Hetzel et al. 1995a).

During subduction, strong erosion was taking placealong the axis of the developing Menderes Mountainswhich striped off the uppermost structural successions(Figure 13). When the Sakarya Continent finally collidedwith the Menderes Platform, it was internally imbricated(Figure 13b) and parts of the Lycian Nappes were thrustfarther to the north and came to overlie directly highergrade metamorphic successions, as observed on the DilekPeninsula (Güngör 1998).

In this study, we have endeavored to document thegeology of the southern part of the Menderes Massif intwo critical areas and introduce a model which may firenew discussions on the tectonic evolution of this complexregion.

Acknowledgements

This study was supported financially by the Scientific andTechnical Research Council of Turkey (project no:YDAÇBAG-3). We are grateful to Dr. Steven K. Mittwedefor constructive comments on the manuscript. We thankProf. Dr. Demir Alt›ner (Middle East Technical University)for descriptions of fossils.


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ARSLAN, A. 2001. Mezoscopic and Microscopic Structures Along theContact Between Menderes Massif and Lycian Nappes in the MilasRegion. MSc Thesis, Dokuz Eylül University, Graduate School ofNatural and Applied Sciences, 92 p [unpublished].

BAflAR›R, E. 1970. Bafa Gölü Do¤usunda Kalan Menderes Masifi GüneyKanad›n›n Jeolojisi ve Petrografisi [Geology and Petrography ofthe Southern Margin of the Menderes Massif to the East of LakeBafa]. Faculty of Science Publications, Ege University, 102 p [inTurkish with English abstract].

BAflAR›R, E. & KONUK, Y.T. 1981. Crystalline basement and allochthonunits of Gümüldür region. Geological Bulletin of Turkey 24, 1–6.

BATCHELOR, R.A. & BOWDEN, P. 1985. Petrogenetic interpretation ofgranitoid rock series using multicationic parameters. ChemicalGeology 48, 43–55.

BORAY, A., AKAT, U., AKDEN‹Z, N., AKÇAÖREN, Z., ÇA⁄LAYAN, A., GÜNAY, E.,KORKMAZER, B., ÖZTÜRK, E.M. & SAV, H. 1973. Menderes Masifiningüney kenar› boyunca baz› önemli sorunlar ve bunlar›n muhtemelçözümleri. Cumhuriyetin 50. Y›l› Yerbilimleri Kongresi Kitapç›¤›,General Directorate of Mineral Exploration and Rearch Institute ofTurkey (MTA) Publications, 11–20.

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Received 20 October 2003; revised typescript accepted 16 January 2004

The Problem of the Core—Cover Boundary of the Menderes ...journals.tubitak.gov.tr/earth/issues/yer-04-13-1/yer-13-1-2-0310-5.pdf · with a regionally metamorphosed rock succession

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