Origin and Tectonic Significance of the Metamorphic Sole and

Origin and Tectonic Significance of the Metamorphic Soleand Isolated Dykes of the Divri¤i Ophiolite (Sivas, Turkey):

Evidence for Slab Break-off prior to OphioliteEmplacement

OSMAN PARLAK1, HÜSEY‹N YILMAZ2 & DURMUfi BOZTU⁄3

1 Çukurova University, Department of Geological Engineering, TR–01330 Adana, Turkey(E-mail: [email protected])

2 Cumhuriyet University, Department of Geophysical Engineering, TR–58140 Sivas, Turkey3 Cumhuriyet University, Department of Geological Engineering, TR–58140 Sivas, Turkey

Abstract: The Late Cretaceous Divri¤i ophiolite of east-central Anatolia comprises, from bottom to top, anophiolitic mélange, metamorphic sole and remnants of oceanic lithosphere. The ophiolitic mélange has been thrustonto the Lower Carboniferous–Campanian Munzur Limestone (Tauride platform), and is in turn tectonicallyoverlain by the metamorphic sole. The metamorphic-sole rocks are represented by amphibolite, plagioclaseamphibolite, plagioclase-amphibole schist, plagioclase-epidote-amphibole schist and calc-schist. The oceanic-lithosphere remnant exhibits a complete section, excluding volcanic rocks, comprising mantle tectonites, ultramaficto mafic cumulates, isotropic gabbros and sheeted dykes. Isolated dykes intrude the metamorphic sole and mantletectonites at different structural levels. The metamorphic-sole rocks beneath the Divri¤i ophiolite can be dividedinto two groups with distinct geochemical features. The first group is tholeiitic (Nb/Y=0.07–0.18), whereas thesecond group is alkaline (Nb/Y=1.77–3.48) in chemistry. Chondrite-normalized REE patterns, N-MORB-normalized spider diagrams and tectonic discrimination diagrams suggest that the protolith of the first group wassimilar to island-arc tholeiitic basalts, whereas the protolith of the second group was more akin to within-platealkali basalts. The isolated dykes cutting the metamorphic sole and the mantle tectonites exhibit alkaline(Nb/Y=0.68–2.11) character and are geochemically similar to within-plate alkaline basalts. The geochemicalevidence suggests that the Late Cretaceous Divri¤i ophiolite formed in a suprasubduction zone tectonic setting tothe north of the Tauride platform. During intraoceanic subduction/thrusting, the IAT type and seamount-typealkaline basalts were metamorphosed and accreted to the base of the Divri¤i ophiolite. The alkaline isolated dykeswere probably the result of late-stage magmatism fed by melts that originated within an asthenospheric windowdue to slab break-off, shortly before the emplacement of the Divri¤i ophiolite onto the Tauride platform to thesouth.

Key Words: isolated dyke, amphibolite, alkaline magma, tholeiitic magma, slab break-off, Divri¤i, Turkey

Divri¤i Ofiyolitindeki (Sivas, Türkiye) Metamorfik Dilim ve ‹zole Dayklar›nKökeni ve Tektonik Önemi: Ofiyolit Yerleflmesinden Önce Dalan Levhan›n

Kopmas›na ‹liflkin Veriler

Özet: Orta Anadolunun do¤usunda yer alan Geç Kretase yafll› Divri¤i ofiyoliti tabandan tavana do¤ru ofiyolitikmelanj, metamorfik dilim ve okyanusal litosfer kal›nt›lar›n› içermektedir. Ofiyolitik melanj tabanda ErkenKarbonifer–Kampaniyen yafll› Munzur Kireçtafllar›n› (Toros platformu) bindirmeli bir dokanakla üzerler ve tavandaise metamorfik dilim taraf›ndan tektonik dokanakla örtülür. Metamorfik dilim amfibolit, plajiyoklasl› amfibolit,plajiyoklas-amfibol flist, plajiyoklas-epidot-amfibol flist ve kalk-flist kayaçlar› ile temsil edilmektedir. Okyanusallitosfer kal›nt›lar› volkanikler hariç tam bir kesit sunarlar ve manto tektonitleri, ultramafik-mafik kümülatlar,izotropik gabrolar ve levha dayklar› ile temsil edilirler. ‹zole dayklar metamorfik dilim ve manto tektonitlerinide¤iflik yap›sal seviyelerde keserler. Divri¤i ofiyolitinin taban›nda yer alan metamorfik dilime ait kayaçlar farkl›jeokimyasal özelliklerine göre iki farkl› gruba ayr›labilirler. Birinci grup toleyitik (Nb/Y=0.07–0.18) ikinci grup isealkalen (Nb/Y=1.77–3.48) kimyadad›r. Kondrite göre normalize edilmifl nadir toprak element diyagram›, N-MORB’a göre normalize edilmifl örümcek diyagram› ve tektonik ortam belirleme diyagramlar› birinci gruba aitmetamorfik kayaçlar›n ada yay› toleyitik bazaltlar›ndan, ikinci gruba ait metamorfik kayaçlar›n ise k›ta içi alkalibazaltlar›ndan türediklerini iflaret etmektedir. Metamorfik dilim ve manto tektonitlerini kesen izole dayklar alkalen(Nb/Y=0.68–2.11) karakterde olup jeokimyasal aç›dan k›ta içi bazaltlar›na benzemektedir. Jeokimyasal verilerDivri¤i ofiyolitinin Geç Kretase’de Toros platformunun kuzeyinde okyanus içi dalma-batma zonu üzerinde

Turkish Journal of Earth Sciences (Turkish J. Earth Sci.), Vol. 15, 2006, pp. 25-45. Copyright ©TÜB‹TAK

25

Introduction

The Late Cretaceous ophiolites of Turkey define theNeotethyan sutures that resulted from the closure ofoceanic basins between the Eurasian and Afro-Arabianplates during the Late Triassic to Late Cretaceous period.From north to south, these suture zones are named: (a)the ‹zmir-Ankara-Erzincan, (b) the Inner Tauride, and (c)the SE Anatolian suture zones (fiengör & Y›lmaz 1981;Görür et al. 1984; Robertson & Dixon 1984; Dilek &Moores 1990; Y›lmaz 1993; Robertson 2004). Availablepetrographic and geochemical data on ophioliticextrusives and intrusives suggest that the Neotethyanophiolites of Turkey formed in a suprasubduction zoneenvironment (SSZ) (e.g., Pearce et al. 1984; Parlak1996; Parlak et al. 1996, 2000, 2002, 2004; Yal›n›z etal. 1996, 2000; Beyarslan & Bingöl 2000; Floyd et al.2000; Robertson 2002, 2004; Çelik & Delaloye 2003).

The ophiolites of southern Turkey are located alongtwo lineaments, namely the Bitlis-Zagros suture zone andthe Tauride belt (Figure 1). The Bitlis-Zagros suture zoneincludes complete and undeformed oceanic lithosphericremnants of the southern branch of Neotethys, such asTroodos in Cyprus, K›z›lda¤ in Turkey and Baer-Bassit inSyria (Figure 1). The Tauride ophiolite belt ischaracterized by dismembered ophiolitic units rooted tothe north of the Tauride platform (fiengör & Y›lmaz1981; Andrew & Robertson 2002; Robertson 2002,2004; Parlak & Robertson 2004). These are, from westto east, the Lycian, Tekirova, Beyflehir-Hoyran, Alihoca,Mersin, Pozant›-Karsant›, P›narbafl› and Divri¤i ophiolites(Figure 1). The ophiolite-related units in this latter beltare characterized, from bottom to top, by ophioliticmélanges that tectonically overlie the Tauride carbonateplatform, metamorphic soles and ophiolitic rocks. Well-developed thin metamorphic soles, ranging in thicknessfrom 100 to 400 m, crop out beneath the serpentinizedmantle tectonites. Protoliths of the metamorphic solessuggest the presence of both tholeiitic and alkalinemagma types from various tectonic settings, such as OIB,MORB and IAB (Parlak et al. 1995; Parlak 1996; Çelik

2002; Çelik & Delaloye 2003; Vergili & Parlak 2005).Isolated microgabbro and diabase dykes intrude themetamorphic soles, mantle tectonites and cumulates ofthe Tauride ophiolites. The geochemistry of the dykesshows that they formed in a subduction-relatedenvironment and indicates their derivation from anisland-arc tholeiite (IAT) (Parlak et al. 1995; Parlak &Delaloye 1996; Dilek et al. 1999; Elitok 2001; Çelik &Delaloye 2003; Vergili & Parlak 2005).

The latest stage of magmatic activity in asuprasubduction zone setting is dominated by theeruption of MORB-like or OIB lavas on top of earlier arc-related tholeiitic lavas. Alternatively, these magmas mayintrude as dykes (Shervais 2001). This has beeninterpreted as off-axis alkaline magmatism representingmelts that possibly originated from an asthenosphericwindow beneath the displaced oceanic lithosphere in theupper plate (Shervais 2001; Dilek & Flower 2003).Examples of this type of magmatism are found in theCoast Range ophiolite of California (Shervais & Beaman1991), the Oman ophiolite (Alabaster et al. 1982;Ernewein et al. 1988; Dilek & Flower 2003), and theTauride ophiolites of Turkey (Lytwyn & Casey 1995;Dilek et al. 1999). The late-stage magmas, representedby isolated dykes in the Tauride ophiolites, range incomposition from basalts to andesites characteristic ofevolved island-arc tholeiites, and have been interpreted ashaving been derived from an asthenospheric windowcreated by the subduction of a ridge system in the InnerTauride ocean (Lytwyn & Casey 1995; Dilek et al. 1999).Çelik (2002) documented exclusively alkaline pyroxenitedykes cutting the metamorphic sole of the Pozant›-Karsant› ophiolite in southern Turkey. The isolatedalkaline microgabbro to diabase dykes of our study area,which intrude metamorphic soles and oceanic lithosphericremnants, have not previously been recorded in Turkishophiolites. Thus, the Divri¤i ophiolite is an interestingexample of alkaline-type melt generation in the earlyobduction stages of oceanic lithosphere onto thecontinental margin.

ORIGIN OF METAMORPHIC SOLE AND ISOLATED DYKES

26

olufltu¤unu göstermektedir. Okyanus içi dalma-batma/bindirme s›ras›nda ada yay› toleyitik bazaltlar› ve okyanusadas› alkali bazaltlar›n›n metamorfizmaya maruz kal›p Divri¤i ofiyolitinin taban›na yerleflmifltir. Alkalen izole dayklarise dalan levhan›n kopmas› ile aç›lan astenosferik pencereden nüfuz eden zenginleflmifl eriyiklerin besledi¤i geç-evremagmatizmas› sonucu Divri¤i ofiyolitinin Toros platformu üzerine yerleflmesinden hemen önce geliflmifltir.

Anahtar Sözcükler: izole dayk, amfibolit, alkali magma, toleyitik magma, levha kopmas›, Divri¤i, Türkiye

O. PARLAK ET AL.

27

This paper (1) presents the major- and trace-elementchemistry of the metamorphic sole and isolated dykerocks intruding both the metamorphic sole and themantle tectonites, (2) investigates possible protoliths ofthe material accreted to the base of mantle tectonitesduring intraoceanic subduction, and (3) presents theevidence for late-stage dyke intrusions fed by melts thatoriginated within an asthenospheric window due to slabbreak-off, shortly before the emplacement of the Divri¤iophiolite onto the Tauride platform in the LateCretaceous.

Geological Setting

The Divri¤i region in east-central Anatolia comprises theTauride platform unit, ophiolitic mélange, ophiolite-related metamorphic rocks, ophiolitic rocks, a volcano-sedimentary unit, granitoid rocks and Tertiary coversediments (Figure 2). Detailed (1:25000-scale) geologicalmapping of the internal stratigraphy of the ophioliticunits of the Divri¤i region was first carried out by Y›lmaz

et al. (2001). The structurally lowest unit in the studyarea is the Munzur Limestone. The Munzur Limestone ispresent in the Mesozoic carbonate sequence of most ofthe autochthonous and allochthonous units of the Tauridebelt (Özgül & Turflucu 1984). The base of the Munzurlimestone is not exposed in the study area, and this unitis tectonically overlain by the Yefliltaflyayla ophioliticmélange and above that, the metamorphic sole andDivri¤i ophiolite (Figures 2 & 3). The Munzur Limestonecomprises, from bottom to top, algal limestone, ooliticlimestone, algal and foraminiferal limestone, chertylimestone, neritic limestone, rudistic limestone andpelagic limestone (Özgül & Turflucu 1984). The typelocality of the Munzur Limestone has yielded an EarlyTriassic–Campanian age (Özgül & Turflucu 1984);however, the fossil content of this unit in the study areaindicates an Early Carboniferous–Campanian age (Öztürk& Öztunal› 1993; Y›lmaz et al. 2001).

The Yefliltaflyayla mélange tectonically overlies theMunzur Limestone east of Ekinbafl› and Maltepe villages,and is tectonically overlain by either metamorphic-sole

İstanbul

İzmir

LycianNap

pes

IPO

IAESZ

BHN

MO

AO

DOANATOLIA

İspendere-Kömürhan ophiolite

Baskil arc

Km

1000

Gulemanophiolite

Munzur

Küre ophiolite

Çangaldağarc

RhodopeMassif

MoesianPlatform

EURASIA

MirditaOphiolite

POHellenides

Dinarides

AdriaticSea

VO

Vardar Zone ophiolites

East AnatolianFault

North Anatolian Fault

ARABIA

Troodos ophiolite

DeadSeaFault

Cyprus TrenchAegean Trench

Crete

Mediterranean Sea

Black Sea

Aegean

SeaRhodes

AC

T au r id ePlatf o r m

Pontides

Ankara

Melang

e

Kızıldağophiolite

20°E 24°E 28°E 32°E 36°E 40°E44°N

42°N

40°N

36°N

34°N

Bitlis-Zagros

Suture Zone

Figure 1. Distribution of the Neotethyan ophiolites and major tectonic features of the eastern Mediterranean region (from Dilek & Flower2003). AC– Antalya Complex; IPO– Intra-Pontide Ophiolites; BHN– Beyflehir-Hoyran Nappes; IAESZ– ‹zmir-Ankara-ErzincanSuture Zone; MO– Mersin Ophiolite; PO– Pindos Ophiolite; VO– Vourinos Ophiolite; AO– Alada¤ Ophiolite; DO– Divri¤i Ophiolite.

rocks or serpentinized mantle rocks. This unit is alsounconformably overlain by Tertiary cover sediments nearDivri¤i (Figures 2 & 3). The mélange unit containslimestone blocks and metamorphic-rock fragments set ina serpentinized matrix. The limestone blocks typicallyrange from tens of metres to several hundred metres insize. The metamorphic-rock fragments are representedby gneiss, amphibolite, metavolcanic rocks,metaquartzite, calc-schist, and mica schist.

The metamorphic sole lies consistently between themantle tectonites and the Yefliltaflyayla mélange to theeast of Ekinbafl›, and shares sheared contacts with theunits above and below (Figure 2). A pronounced regionalfoliation, mineral lineations and intrafolial folds wereproduced during intraoceanic deformation. The mainlithology of the metamorphic sole is amphibolite, withsubordinate greenschist, marble and metachert. Themetamorphic sole exhibits a classic inverted metamorphicgradient, from amphibolite-facies metamorphic rocksdownward into greenschist-facies rocks. The

metamorphic sole is cut by unmetamorphosed diabase/microgabbro dykes.

The Divri¤i ophiolite is located between Çetinkaya andMaltepe in the study area (Figure 2). It displays an almostcomplete oceanic lithospheric section, represented byserpentinized mantle tectonites, cumulates, isotropicgabbros and sheeted dykes (Figures 2 & 3). Ophioliticvolcanic rocks and associated sediments are absent. Thetransitions from cumulate to isotropic gabbros and fromisotropic gabbros to sheeted dykes are gradual, and areexposed along the Tatl›çay river between Günefl andÇetinkaya (Figure 2). The contacts between the otherunits of the ophiolite are tectonic (Figure 2). Theexposures of the mantle tectonite are located betweenPengürt and Maltepe, and are dominated by serpentinizedharzburgite that contains dunitic lenses and subordinatelherzolite. A number of chromite deposits within thedunitic lenses were mined at Pengürt, north of Bizevi andsouth of Gal›n (Figure 2). The tectonites are intruded bypyroxenite and gabbroic to diabasic dykes at different


28

Çetinkaya

Divriği

Ekinbaşı

Maltepe

Sincan

sheeted dyke complex

massive gabbros

layered gabbros

cumulate peridodites

tectonites

metamorphic solethrust faultYeşiltaşyayla m langeé

Munzur LimestoneE. Carboniferous-Campanian

Divriği granitoid

Saya formationvolcano-clastic rocks

MaastrichtianCampanian

PalaeoceneMaastrichtian alluvium and talus

Örenlice formationcontinental detriticsYamadağı Volcanics

unnamed unitsdetritics, carbonates andevaporites

Eocene-Miocene

Plio-Quaternary

Quaternary

0 2Km

DivriğiOphiolite

Pengürt

Yellice

Güneş

38 06o’37 37o

’

39 23o’

39 11o’

LateCretaceous

Cürek

Akmeşe

Karatepe

Kızılyüce tepe

Galın

Bizevi

Tekke

Soğucak

Keçikaya

İnallı

Eskiköy

Tatlıçay river

N

Figure 2. Geological map of the area between Divri¤i and Çetinkaya (Sivas) (modified from Y›lmaz et al. 2001; Y›lmaz & Y›lmaz 2004).

structural levels. The ultramafic cumulate rocks crop outmainly to the south of Pengürt and to the northeast ofYellice (Figure 2). The ultramafic cumulates comprisedunite, wehrlite, olivine websterite and scarce lherzolite.The gabbroic cumulates are observed along the Tatl›çay

river to the northeast of Çetinkaya (Figure 2) and arerepresented by normal gabbro and olivine gabbro. Thecumulate gabbro passes transitionally into isotropicgabbroic rocks along the Tatl›çay river near Keçikaya andto the northeast of ‹nalli (Figure 2). It is represented by

O. PARLAK ET AL.

29

Örenlice formation

Yamadağıvolcanics

Divriğigranitoids

Yeşiltaşyaylam langeé

MunzurLimestone

AGE UNIT LITHOLOGY

QuaternaryPliocene

Miocene

Eocene

L. CarboniferousCampanian

EXPLANATION

recrystalized limestone

mélange containing limestoneand metamorphics within serpentinizedmatrix

isolated dykes

tectonites containing orthopyroxenitelayers and dunite pods

cumulate peridotites containingdunite, wherlite and clinopyroxenites

massive gabbros

basal conglomerate, gravelstone-sandstone alternation, pillow lavaswith milstone interlayers and reefallimestone

continental clastic rocks

Quaternary

PalaeoceneMaastrichtian

CampanianMaastrichtian

Sayaformation

Late

Cretaceous

DivriğiOphiolite

tectonic contact

tectonic contact

tectonic contact

layered gabbros

sheeted dyke complex

granitic rocks

alluvium and talus

andesitic and basaltic lavasand pyroclastites

detritics, carbonates and evaporites

unconformity

unconformity

unconformity

unconformity

unconformity

tectonic contact

metamorphicsole

unnamedunits

Figure 3. Columnar section of units in the study area (modified from Y›lmaz et al. 2001; Y›lmaz & Y›lmaz2004).

gabbro and diorite. The sheeted dykes are sparselyrepresented in the upper parts of the isotropic gabbrosand increase in frequency upwards. The dyke thicknessesrange from 20 to 50 cm. The sheeted dykes arecharacterized by diabase and microdiorite.

The volcano-sedimentary unit, named the Sayaformation, is well exposed around Yellice and southwestof Günefl village (Figure 2). The Saya formationunconformably overlies the Divri¤i ophiolite, andcomprises conglomerates at the base in which ophiolite-derived pebbles are dominant. The basal conglomeratepasses into alternations of sandstone-mudstone-marl,limestone lenses, agglomerate, tuff and spilitic volcanics.This volcano-sedimentary unit is intruded by basic dykes.The fossil content of the limestone lenses yielded aCampanian-Maastrichtian age (Y›lmaz et al. 2001).

The granitoid rocks, intruding all of the pre-existingunits, are observed at Yellice, Pengürt and Ekinbafl›(Figure 2). They are A-type granitoid bodies, consisting offelsic monzonitic/syenitic and mafic monzogabbroic/monzodioritic rocks and monzodiorite, and arethemselves intruded by numerous aplite and diabasedykes (Y›lmaz et al. 2001; Boztu¤ et al. 2005). Thegranitoid body cuts the volcano-sedimentary unit ofCampanian–Maastrichtian age and is unconformablyoverlain by Eocene basal conglomerates (Do¤an et al.1989; Y›lmaz et al. 2001). Thus, the intrusion age of thegranitoid body is thought to be between Maastrichtianand Eocene (Figures 2 & 3).

The Tertiary cover sediments, cropping out betweenDivri¤i and Çetinkaya, range in age from Eocene toQuaternary and are represented by detrital material,carbonate rocks, evaporites, volcanic rocks and alluvium(Figure 2). The base of the cover sedimentsunconformably overlies the former units and begins withan Eocene basal conglomerate in which pebbles ofgranitoid rock, ophiolitic rocks and iron ore are dominant(Gürsoy 1986; Do¤an et al. 1989; Y›lmaz et al. 2001).

Petrography

The isolated dyke intrusions in the mantle tectonites ofthe Divri¤i ophiolite are widespread and are representedby microgabbro-diabase and pyroxenite whereas themetamorphic sole is only intruded by microgabbro-diabase dykes. The dykes have sharp contacts with theirhost rocks but chilled margins are not observed. The

pyroxenite dykes have thicknesses ranging from 10 to 25cm and show granular texture. They are made upexclusively of orthopyroxenes, which are recognised inthin section by their first-order colours and lamellarstructure. In some cases, they contain clinopyroxeneexsolution lamellae (Figure 4a). The microgabbro-diabasedykes have 30 cm to 1 m thickness and exhibitintergranular to microgranular-ophitic textures (Figure4b–d). They are composed mainly of plagioclase,amphibole and clinopyroxene. The plagioclase showsextensive saussuritization. The clinopyroxene occurs asrelict grains surrounded by reaction rims of green togreen-brown hornblende. In some dykes, biotite isobserved together with amphibole (Figure 4c). Thesecondary phases include epidote and chlorite, andaccessory minerals are titanite and ilmenite. Calcite andquartz are also found in veins.

The metamorphic-sole rocks of the Divri¤i ophiolitecomprise four mineralogical associations. These are (1)amphibolite, (2) plagioclase amphibolite, (3) plagioclase-amphibole schist and (4) plagioclase-epidote-amphiboleschist. The amphibolites have no pronounced foliation,are characterized by granoblastic texture, and arecomposed exclusively of green hornblende (Figure 4e).The plagioclase-amphibolite rocks have granoblastictexture and are made up of brown hornblende (65–75%), plagioclase (25–35 %), epidote (< 5 %) and opaqueminerals (Figure 4f). The plagioclase is intensely alteredto saussurite and sericite. Quartz, epidote and calcite areobserved in veins. The plagioclase-amphibole schist hasnematoblastic texture and exhibits pronounced foliationdue to the preferred orientation of hornblende (70–75%) and plagioclase (25–30 %) (Figure 4g). Theplagioclase-epidote-amphibole schist has nematoblastictexture and comprises plagioclase (5–10 %), epidote(10–15 %) and green to brown hornblende (70–75 %)(Figure 4h).

Analytical Techniques

A total of 29 samples from the metamorphic-sole rocks(17) and isolated mafic dykes (12) were analysed fortheir major- and trace-element contents. The major- andtrace-element analyses were carried out in the MineralogyDepartment of the University of Geneva (Switzerland).The major elements were determined by XRFspectrometry on glass beads fused from ignited powders


30

– to which Li2B4O7 had been added (1:5) – in a gold-platinum crucible at 1150 ºC. The trace elements wereanalyzed on pressed powder pellets by the sameinstrument. A subset of 11 samples was analysed fortrace elements (including REE) by ICP-MS at Acme

Analytical Laboratories in Canada. A subset of 3 sampleswas also analysed for rare-earth elements (REE) by thesame method in the Minerology Department of theUniversity of Geneva.

O. PARLAK ET AL.

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a

c

e

g

b

h

f

d

Figure 4. Microscopic views from the isolated dyke (a-d) and metamorphic-sole rocks (e-h) of the Divri¤iophiolite.

Geochemistry

The major-, trace- and rare-earth-element contents of themetamorphic-sole and isolated dyke rocks from theDivri¤i ophiolite are given in Tables 1 to 3. Themetamorphic-sole rocks and the isolated dykes of theDivri¤i ophiolite have a wide range of loss-on-ignition(LOI) values, ranging from 0.8 to 11.03 (Tables 1 & 2).The wide variation in LOI is a crude measure of thedegree of rock alteration and reflects the contribution bysecondary hydrated and carbonate phases. Humphris &Thompson (1978) and Thompson (1991) stated thatunder medium grades of metamorphism involvinghydrous fluids, some degree of selective element mobilityis to be expected, especially for the large-ion-lithophile(LIL) elements. Characterization and discrimination ofmetamorphic (e.g., amphibolites) and magmatic suiteshas been done on the basis of trace elements generallyconsidered relatively stable (immobile) during alteration,such as the high-field-strength (HFS) elements and rare-earth elements (Pearce & Cann 1973; Smith & Smith1976; Floyd & Winchester 1978, 1983). Good linearcoherence between pairs of stable incompatible elements,and smooth normalized patterns for REE or a sequenceof incompatible elements mirror pre-metamorphic/alteration magmatic compositional variations (Floyd et al.1996; Winchester et al. 1998; Vergili & Parlak 2005).

The amphibolitic rocks from the metamorphic soleexhibit two geochemically distinguishable magma typeson the basis of the Zr/Ti versus Nb/Y diagram of Pearce(1996). The first group plots in the alkali-basalt field andis characterized by high concentrations of TiO2 (1.81 to5.04 wt %), P2O5 (0.2 to 1.55 wt %), Zr (150 to 339ppm), Nb (30 to 115 ppm) and Nb/Y (1.77 to 3.48)whereas the second group plots in the tholeiitic-basaltfield and is represented by low concentrations of TiO2

(0.61 to 0.99 wt %), P2O5 (0.05 to 0.21 wt %), Zr (38to 72 ppm), Nb (2 to 4 ppm) and Nb/Y (0.07 to 0.18)(Figure 5).

The isolated dykes cutting the metamorphic sole andthe mantle tectonites are nepheline normative (Table 2).They plot in the alkali-basalt to trachy-andesite field andcontain high values of TiO2 (0.5 to 1.76 wt %), P2O5

(0.11 to 0.49 wt %), Zr (128 to 217 ppm), Nb (17 to89 ppm) and Nb/Y (0.68 to 2.11) (Figure 5). While theDivri¤i subophiolitic amphibolitic rocks exhibitgeochemical features similar to metamorphic-sole rocksoccurring elsewhere in the Tauride belt, the Divri¤i

isolated dykes differ from other isolated dykes in the beltin terms of their alkaline nature. The isolated dykes atMersin, P›narbafl›, Pozant›-Karsant›, Antalya and Köyce¤izin southern Turkey have tholeiitic chemistry.

The plots in Figure 6a, b illustrate the broad range ofvariable Zr/Y and Zr/Ti ratios for the amphibolites. Thealkaline amphibolites are characterized by high Zr/Y(11.66 to 7.77) and Zr/Ti (0.008 to 0.025) ratioswhereas the tholeiitic amphibolites have low Zr/Y ratios(2.11 to 3) and Zr/Ti (0.01 to 0.013). The isolated dykesdisplay similar geochemical behaviour to the alkalineamphibolites in terms of Zr/Y (4.16 to 10.08) and Zr/Ti(0.015 to 0.065) ratios (Figure 6a, b). Both amphibolitesand dykes display coherent trends in Ti, Y and FeO*/MgOwith increasing Zr (Figure 6a–c). The FeO*/MgO variationdiagram in Figure 6c shows that the internal chemicalvariation is governed largely by mafic fractionation thatproduced a typical Fe-enrichment trend for the alkaline totholeiitic amphibolites and alkaline isolated dykes. Thetholeiitic amphibolites appear to define a differentfractionation trend, however, they exhibit geochemicalfeatures similar to the other data at lower values of Zr.Figure 6d presents two ratios (Ce/Yb vs Zr/Nb) of pairsof elements of different degrees of incompatibility. Onthis plot, the degree of partial melting increases fromupper left to lower right. Thus, the protolith of thealkaline amphibolites is thought to have formed as aresult of smaller degrees of partial melting than theprotolith of the tholeiitic amphibolites. The data from theisolated dykes plot between those of the alkaline andtholeiitic amphibolites, suggesting that they formed as aresult of smaller degrees of partial melting compared tothe tholeiitic amphibolites and higher degrees of partialmelting compared to the alkaline amphibolites (Figure5d). These geochemical aspects will be discussed later inmore detail.

The chondrite-normalized REE patterns of themetamorphic sole rocks and isolated dykes are presentedin Figure 7. The metamorphic-sole rocks display twodistinct REE patterns. The alkaline amphibolites exhibitLREE-enriched patterns (LaN/YbN=8.80 to 21.95)whereas the tholeiitic ones exhibit flat REE patterns(LaN/YbN=0.59 to 1.25). The alkaline amphibolites displaygeochemical trends similar to LREE-enriched patterns ofocean-island basalts (Sun & McDonough 1989) whereasthe tholeiitic amphibolites are more akin to the flat-lyingREE patterns of basaltic rocks formed in subduction-


32

O. PARLAK ET AL.

33

Tabl

e 1.

Maj

or-

and

trac

e-el

emen

t co

nten

ts o

f th

e m

etam

orph

ic s

ole

rock

s.

Met

amor

phic

-Sol

e R

ocks

Thol

eiiti

c Am

phib

olite

sAl

kalin

e Am

phib

olite

s

Sam

ple

PD-1

PD-2

PD-4

PD-5

PD-1

9PD

-20

PD-2

3PD

-24

PD-2

7PD

-28

PD-2

9PD

-30

PD-3

1PD

-32

PD-3

3PD

-71

PD-7

2

SiO

241

.14

44.1

140

.31

46.5

941

.15

41.6

841

.67

46.3

249

.73

49.8

443

.15

46.6

841

.23

42.6

536

.58

44.9

844

.53

TiO

20.

990.

990.

840.

614.

725.

042.

573.

312.

152.

293.

322.

834.

084.

061.

813.

914.

03Al

2O3

17.2

716

.58

12.5

916

.30

12.1

212

.23

10.5

316

.24

17.0

916

.99

13.0

311

.75

13.6

814

.68

9.09

14.3

214

.88

FeO

*11

.47

12.0

89.

579.

3015

.82

16.0

113

.05

14.2

511

.27

11.5

115

.81

12.8

115

.13

14.6

39.

4013

.81

13.0

3M

nO0.

380.

310.

300.

160.

290.

280.

170.

200.

270.

240.

240.

220.

210.

220.

420.

120.

09M

gO5.

024.

305.

577.

507.

746.

878.

632.

773.

263.

268.

038.

807.

315.

175.

985.

755.

50Ca

O14

.38

10.8

515

.39

14.6

510

.90

11.0

519

.92

7.10

7.29

6.91

10.5

711

.08

13.1

411

.60

22.3

910

.70

11.4

3N

a 2O

2.79

4.39

2.93

2.05

2.03

2.36

0.76

4.53

4.83

4.85

2.29

2.54

2.06

3.02

2.05

2.88

2.37

K2O

1.38

1.52

0.91

0.46

1.41

1.41

0.59

2.04

2.38

2.11

1.07

0.96

1.17

1.30

0.88

1.92

2.40

P 2O

50.

200.

210.

120.

050.

840.

870.

421.

550.

780.

840.

200.

360.

590.

600.

240.

700.

65Cr

2O3

0.11

0.10

0.06

0.07

0.03

0.03

0.10

0.00

0.00

0.00

0.09

0.08

0.01

0.01

0.12

0.02

0.01

NiO

0.03

0.03

0.02

0.01

0.02

0.01

0.05

0.00

0.00

0.00

0.05

0.03

0.01

0.01

0.03

0.01

0.01

LOI

4.95

4.55

11.0

32.

411.

971.

601.

821.

300.

920.

801.

301.

490.

911.

2810

.37

0.83

0.99

Tota

l10

0.11

100.

0499

.65

100.

1499

.06

99.4

210

0.27

99.6

099

.96

99.6

599

.13

99.6

299

.54

99.2

399

.36

99.9

699

.92

Nb

23

42

6767

5311

211

511

047

3966

6430

5059

Zr72

7066

3823

825

218

133

933

132

020

717

127

628

015

024

227

0Y

2727

2218

2727

1941

3334

2622

2424

1327

32Sr

698

476

123

107

497

553

252

1235

1435

1864

354

244

671

583

254

1215

613

U2

22

32

213

23

22

22

22

22

Rb

2932

2312

1616

741

4041

1920

1718

2066

79Th

22

23

22

22

83

22

22

22

2Pb

1518

1313

22

102

96

33

22

32

2G

a18

1512

1517

1915

2316

1519

1722

2012

1922

Zn12

311

382

6713

414

511

717

310

085

132

104

137

152

7385

58Cu

8219

4367

2524

854

75

4629

6339

164

2415

Ni

208

202

108

9511

911

332

710

44

340

175

8947

147

6940

Co64

6143

4155

5475

2311

969

5651

4250

4832

Cr85

776

144

053

121

926

072

310

512

692

589

7748

974

109

87V

221

231

214

234

333

367

280

9925

3227

728

637

736

824

532

832

8Ce

1416

1514

114

108

3917

112

613

647

4591

7616

8997

Nd

119

1010

4339

3068

6061

2320

4838

2239

42Ba

112

182

5410

464

546

114

683

1776

1230

339

162

290

397

254

398

837

La8

104

421

2151

4567

7416

2537

2833

3027

S10

38

233

33

352

922

927

357

818

8252

812

1977

9H

f1

16

15

53

612

112

28

114

59

Sc26

2618

4735

3327

1011

1139

4132

262

2720

As6

75

53

75

85

55

88

56

117

Ti/Y

219.

522

0.4

230.

220

1.5

1048

.911

18.5

811.

748

3.4

390.

640

4.0

764.

677

0.4

1019

.710

13.4

834.

386

7.6

754.

9N

b/Y

0.07

0.11

0.18

0.11

2.48

2.48

2.79

2.73

3.48

3.24

1.81

1.77

2.75

2.67

2.31

1.85

1.84

Zr/T

i0.

010.

010.

010.

010.

010.

010.

010.

020.

030.

020.

010.

010.

010.

010.

010.

010.

01


34

Tabl

e 2.

Maj

or-

and

trac

e-el

emen

t co

nten

ts a

nd C

IPW

nor

ms

of t

he is

olat

ed d

ykes

. Isol

ated

Dik

es

Sam

ple

PD-3

PD-6

PD-7

PD-8

PD-1

0PD

-11

PD-1

2PD

-13

PD-1

4PD

-16

PD-1

7PD

-18

SiO

251

.15

46.3

946

.12

49.0

046

.60

46.8

749

.37

49.3

950

.22

51.5

755

.39

46.2

0Ti

O2

1.41

1.33

1.31

1.76

1.14

1.17

1.31

1.35

1.22

0.50

0.50

1.15

Al2O

319

.62

15.6

315

.88

17.5

616

.89

15.9

817

.87

17.7

117

.11

23.7

424

.62

15.1

0

FeO

*7.

589.

339.

4810

.27

9.06

8.22

8.53

8.90

8.05

0.70

0.86

8.67

MnO

0.13

0.16

0.17

0.15

0.12

0.12

0.12

0.12

0.11

0.02

0.01

0.23

MgO

6.94

7.08

7.07

3.85

7.23

7.94

5.88

6.19

6.26

1.59

0.53

6.82

CaO

0.85

12.9

012

.27

5.61

12.1

713

.68

8.60

8.19

7.92

7.70

8.28

10.0

3N

a 2O

7.25

2.78

2.81

5.01

3.22

2.70

4.39

4.46

3.93

5.19

7.53

2.71

K2O

0.34

1.00

1.15

2.64

1.42

1.41

2.33

2.27

3.32

4.39

0.61

3.26

P 2O

50.

350.

360.

350.

420.

330.

240.

470.

490.

420.

140.

110.

37

Cr2O

30.

010.

020.

020.

000.

010.

030.

030.

030.

030.

000.

000.

01

NiO

0.02

0.01

0.01

0.00

0.01

0.01

0.01

0.01

0.01

0.00

0.00

0.01

LOI

3.76

3.24

3.32

3.21

2.17

2.15

1.26

1.04

1.34

4.75

1.50

5.04

Tota

l99

.41

100.

2299

.97

99.4

910

0.37

100.

5210

0.18

100.

1599

.95

100.

2999

.94

99.5

8N

b19

1717

2717

1725

2424

8089

17Zr

131

129

128

217

130

140

159

163

164

193

179

136

Y13

2424

3225

2328

2829

3843

24Sr

8828

129

024

438

169

776

362

368

240

269

751

9U

53

24

32

33

36

94

Rb

1218

2133

6757

7876

104

217

2559

Th13

1010

1610

58

1010

3836

11Pb

316

205

108

335

63

314

Ga

2316

1521

1613

1618

1718

2015

Zn57

7083

7239

4028

853

4734

2773

Cu2

3056

5218

2559

345

58

98N

i14

981

813

6167

8288

9721

1674

Co21

4242

2741

3630

3427

33

38Cr

145

154

168

2172

204

234

239

268

833

61V

390

238

242

262

234

231

188

189

186

1610

229

Ce23

3147

8646

4262

6762

117

113

56N

d4

1727

3625

2530

3028

4550

28Ba

6532

238

967

461

844

410

7681

913

1844

322

816

27La

532

2940

4329

3145

4679

102

43S

385

115

487

2910

330

920

559

4914

781

7H

f1

31

61

83

93

47

5Sc

4935

3723

3733

1922

228

934

As5

47

43

34

43

33

4Ti

/Y65

2.3

331.

232

8.4

330.

027

4.5

306.

128

1.2

288.

225

2.9

78.2

70.0

287.

0N

b/Y

1.46

0.71

0.71

0.84

0.68

0.74

0.89

0.86

0.83

2.11

2.07

0.71

Zr/T

i0.

020.

020.

020.

020.

020.

020.

020.

020.

020.

060.

060.

02

CIPW

Nor

ms

Plag

iocl

ase

72.4

547

.07

47.3

052

.90

43.1

439

.32

47.9

948

.69

42.6

148

.59

81.3

730

.97

Ort

hocl

ase

2.38

7.15

8.24

18.2

49.

949.

9115

.77

15.3

522

.43

28.5

43.

8623

.48

Nep

helin

e0.

436.

276.

418.

1210

.27

9.64

9.49

9.11

8.28

15.3

69.

1810

.13

Coru

ndum

5.05

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

0.00

Dio

psid

e0.

0026

.12

23.7

55.

5022

.84

29.0

012

.51

11.3

612

.39

5.98

3.03

21.3

3W

olla

ston

ite0.

000.

000.

000.

000.

000.

000.

000.

000.

000.

001.

700.

00O

livin

e16

.14

9.58

10.5

210

.80

10.4

49.

0110

.55

11.6

510

.88

0.59

0.00

10.5

6Ilm

enite

1.71

1.65

1.63

2.11

1.38

1.42

1.54

1.58

1.43

0.56

0.55

1.43

Mag

netit

e1.

071.

351.

371.

431.

281.

161.

161.

211.

090.

090.

111.

25Ap

atite

0.77

0.81

0.79

0.91

0.72

0.53

1.00

1.04

0.89

0.29

0.22

0.84

Tota

l10

0.00

100.

0010

0.01

100.

0110

0.01

99.9

910

0.01

99.9

910

0.00

100.

0010

0.02

99.9

9

O. PARLAK ET AL.

35

Tabl

e 3.

Trac

e-el

emen

t an

d R

EE c

ompo

sitio

ns o

f th

e su

bset

of

sam

ples

ana

lyse

d by

ICP

-MS.

Met

amor

phic

-Sol

e R

ocks

Isol

ated

Dik

es

Sam

ple

PD-2

PD-5

PD-2

0PD

-23

PD-2

4PD

-27

PD-2

9PD

-30

PD-3

PD-7

PD-1

0PD

-14

PD-1

6PD

-18

Rb

31.1

08.

1020

.80

nd50

.80

46.0

0nd

23.9

06.

8018

.00

71.1

010

9.90

174.

50nd

Ba15

0.50

15.7

051

6.50

nd69

5.00

1545

.30

nd14

7.80

25.1

034

5.50

490.

9012

20.4

048

1.30

nd

Th0.

20<

0.1

5.50

nd10

.40

8.50

nd3.

306.

006.

005.

207.

4036

.30

nd

U0.

20<

0.1

1.80

nd1.

802.

80nd

1.20

3.30

2.20

2.90

3.10

6.60

nd

Nb

1.80

0.70

79.8

0nd

124.

7011

6.50

nd43

.30

20.0

016

.70

15.8

024

.80

75.1

0nd

Ta0.

1<

0.1

4.4

nd6.

76.

60nd

2.5

1.2

11.

001.

44.

4nd

Pb0.

900.

600.

50nd

1.80

2.70

nd0.

403.

006.

303.

400.

707.

40nd

Sr50

8.40

113.

7063

1.10

nd13

62.9

014

47.8

0nd

285.

7010

6.10

345.

8038

0.80

794.

7045

8.90

nd

Zr55

.40

28.1

024

8.50

nd33

7.50

310.

30nd

164.

7014

6.30

128.

0011

7.90

159.

5016

8.70

nd

Hf

1.60

0.90

7.00

nd8.

407.

70nd

4.60

4.00

3.00

3.30

3.70

2.20

nd

Y30

.80

17.7

033

.60

nd45

.10

40.6

0nd

21.9

08.

8025

.40

24.2

025

.30

34.3

0nd

La5.

301.

5063

.20

38.1

210

7.10

80.9

026

.61

32.6

05.

7023

.50

22.2

032

.30

48.0

023

.88

Ce7.

703.

8013

2.60

83.0

621

5.90

173.

8064

.87

66.0

010

.80

46.3

048

.00

60.8

010

0.60

49.3

4

Pr1.

800.

7715

.98

9.68

25.2

119

.06

7.94

7.98

1.28

5.58

5.49

6.93

10.7

05.

83

Nd

9.70

4.30

69.4

038

.79

106.

8078

.30

34.2

935

.50

4.90

23.6

023

.50

27.7

038

.80

23.6

3

Sm3.

301.

5012

.00

7.73

18.1

013

.50

7.84

6.50

1.10

5.00

4.80

5.50

6.30

4.90

Eu1.

180.

653.

962.

126.

164.

782.

422.

170.

201.

471.

301.

511.

261.

38

Gd

4.28

2.05

10.3

36.

2715

.04

10.6

97.

056.

301.

144.

664.

114.

934.

984.

40

Tb0.

760.

551.

660.

842.

181.

701.

001.

040.

180.

800.

820.

811.

020.

65

Dy

4.69

2.82

6.86

4.51

9.93

8.02

5.82

4.56

1.22

4.40

4.02

4.23

5.48

3.91

Ho

1.00

0.67

1.18

0.79

1.68

1.40

1.06

0.79

0.31

0.83

0.85

0.87

1.12

0.77

Er3.

031.

943.

032.

024.

123.

582.

772.

041.

012.

402.

302.

543.

412.

24

Tm0.

500.

380.

460.

260.

610.

450.

370.

280.

210.

380.

300.

400.

540.

31

Yb3.

041.

822.

551.

543.

502.

892.

171.

841.

292.

252.

062.

463.

912.

02

Lu0.

390.

330.

310.

210.

440.

410.

310.

240.

260.

320.

310.

340.

470.

31

nd =

not

det

erm

ined

; <

= b

elow

det

ectio

n lim

it.


36

0.01 0.1 1 10 100

Nb/Y

0.001

0.01

0.1

1

alkali rhyolite

rhyolite & dacite

phonolite

tephri-phon

olite

foidite

trachy-andesite

alkalibasalt

andesite &

basaltic-ande

site

basalt

Zr/

Ti

fieldofisolateddikes

inTaurideophiolites

field of tholeiitic amphibolitesbeneath Tauride ophiolites

fieldofalkalineamphibolites

beneathTaurideophiolites

isolated dikealkaline amphibolitetholeiitic amphibolite

Figure 5. Rock classification diagram for the metamorphic sole and isolateddykes from the Divri¤i ophiolite (after Pearce 1996). Field ofmetamorphic soles and mafic dykes from the Tauride ophiolitesare from Parlak et al. (1995), Lytwyn & Casey (1995), Dilek et al.(1999), Parlak (2000), Çelik & Delaloye (2003).

0 100 200 300 400Zr (ppm)

10

20

30

40

50

Y(p

pm

)

0 100 200 300 400Zr (ppm)

Zr (ppm)

Ti

(pp

m)

0

1

2

3

4

5

6

Fe

O*/

Mg

O

Zr/Nb

Ce/

Yb

(a) (b)

(c) (d)


0 5 10 15 20 25 30

0

0

0 100 200 300 400

10

20

30

40

50

60

70

5000

10000

15000

20000

25000

30000

35000

Increasing degree of partial melting

Figure 6. Characterization of metamorphic-sole rocks and isolated diabase dykes in terms of (a) Zr-Y, (b)Zr-Ti, (c) Zr-FeO*/MgO and (d) Zr/Nb-Ce/Yb.

related settings. These two REE patterns are typical ofother metamorphic soles beneath Tauride-belt ophiolitesand are interpreted to indicate that basaltic volcanicsformed in mid-ocean ridge (MORB), within- plate (WPB)and island-arc (IAT) settings were metamorphosed duringintraoceanic subduction in a Neotethyan oceanic basin(Parlak et al. 1995; Lytwyn & Casey 1995; Dilek et al.1999; Çelik & Delaloye 2003; Vergili & Parlak 2005).The isolated dykes have LREE-enriched, differentiatedpatterns (LaN/YbN=3.17 to 9.42) that are distinct fromthe REE patterns of isolated dykes elsewhere in theTauride-belt ophiolites (Parlak et al. 1995; Lytwyn &Casey 1995; Parlak & Delaloye 1996; Çelik & Delaloye2003; Vergili & Parlak 2005). The LREE-enrichmentpatterns of the isolated dykes from the Divri¤i ophiolitedisplay similarity to LREE-enrichment patterns of ocean-island basalts (Sun & McDonough 1989). One sample ofthe isolated dykes (PD-3) exhibited lower fractionation(LaN/YbN=3.17) and concentrations of REE compared tothe others (Figure 7); this may be due to differentdegrees of partial melting at different depths.

The multi-element diagrams for the isolated dykes,alkaline and tholeiitic amphibolites are presented in

Figure 8. The isolated dykes exhibit enriched multi-element patterns compared to N-MORB and the isolateddykes in other Tauride-belt ophiolites (Figure 8a). Theyexhibit similar patterns to OIB-type basalts in general(Figure 8a). But the isolated alkaline dykes seem toexhibit small relative Nb depletions with respect to theadjacent elements and LIL-element enrichments such asRb, Ba and Th. This may reflect a slight contribution froma subduction-modified source to the alkaline melts. Thealkaline amphibolites can be directly compared chemicallywith ocean-island basalt (OIB) and show multi-elementpatterns similar to the other analysed amphibolites fromthe base of the Tauride-belt ophiolites (Sun &McDonough 1989; Parlak et al. 1995; Lytwyn & Casey1995; Çelik & Delaloye 2003; Vergili & Parlak 2005)(Figure 8b). The tholeiitic amphibolites are different fromOIB-type basaltic rocks but exhibit multi-element patternssimilar to the other tholeiitic amphibolites beneath theTauride-belt ophiolites (Figure 8c). They arecharacterized by enrichment of LIL elements (i.e., Rb, Ba,Th, K), Nb depletion, and flat patterns of HFS elementsrelative to MORB (Figure 8c). All of this evidence suggeststhat the protolith of the tholeiitic amphibolites formed ina subduction-related setting.

O. PARLAK ET AL.

37

1

10

100

1000

La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

Ro

ck/C

ho

nd

rite


field of tholeiitic amphibolitesbeneath Tauride ophiolites

field of alkaline amphibolitesbeneath Tauride ophiolites

field of isolated dikesin Tauride ophiolites

Figure 7. Chondrite-normalized REE patterns of the isolated dykes and metamorphic-sole rocks of the Divri¤i ophiolite (normalizing values are from Sun &McDonough 1989). Data for the metamorphic soles and mafic dykes from theTauride ophiolites are the same as in Figure 5.

To characterize mantle source regions for themetamorphic-sole and isolated dyke rocks of the Divri¤iophiolite, ratio/ratio plots of incompatible elements wereused in Figure 9a, b. The Ce/Sm versus Sm/Yb ratios areplotted in Figure 9a together with OIB and MORBcompositions. The high Sm/Yb and Ce/Sm ratios of thealkaline amphibolites and isolated dykes suggest that theywere derived by melting of an OIB-like enriched mantlesource, whereas the low Sm/Yb and Ce/Sm ratios of the

tholeiitic amphibolites suggest derivation from a moredepleted MORB-like mantle source (Figure 9a). Both thetholeiitic and alkaline amphibolites show geochemicalbehaviour similar to other amphibolites beneath theTauride ophiolites in terms of Ce/Sm and Sm/Yb ratioplots, whereas the isolated dykes are chemically distinctfrom the amphibolites. Th and Ta show similar degrees ofenrichment and depletion in most mantle source regions,however, Th alone is enriched in mantle wedges abovesubduction zones (Pearce 1982; Alabaster et al. 1982).Thus, in Figure 9b, MOR basalts and intraplate basalts fallin a broad band with a slope of unity. The single sampleof tholeiitic amphibolite suggest that it was derived froma depleted mantle source region modified by the additionof a subduction component, whereas the four samples of


38

0.1

0.1

0.1

1

1

1

10

10

10

100

100

100

1000

Rock

/N-M

OR

BR

ock

/N-M

OR

BR

ock

/N-M

OR

B

Rb Th Nb La Pb Sr Nd Zr Eu Gd Y Er Yb

Ba U K Ce Pr P Sm Hf Ti Dy Ho Tm Lu

(a)

(b)

(c)

isolated dikealkaline amphibolitetholeiitic amphiboliteaverage OIB

field of isolated dikesin Tauride belt ophiolite

field of alkaline amphibolitesbeneath Tauride belt ophiolites

field of tholeiitic amphibolitesbeneath Tauride belt ophiolites

Figure 8. N-MORB-normalized spider diagram for the isolated diabasedykes (a), alkaline amphibolite (b) and tholeiitic amphibolites(c) of the Divri¤i ophiolite (normalizing values are from Sun& McDonough 1989). Data for the metamorphic-sole rocksand mafic dykes from the Tauride ophiolites are the same asin Figure 5.

0.01 0.1 1 100.01

0.1

1

10

Ta/Yb

Th

/Yb

shoshonites

calc-alkaline lavas

tholeiitic lavas

depleted m

antle source

enrichedmantle source

MORB

intra-plate basalts

(b)

(a)

0 42 8 12 1614106 18

Ce/Sm

0

1

2

3

4

5

6

OIB

MORB

fieldofalkalineamphibolites

beneath Taurideophiolites

field of tholeiitic amphibolitesbeneath Tauride ophiolitesS

m/Y

b


subduction

component

Figure 9. (a) Sm/Yb versus Ce/Sm diagram and (b) Ta/Yb versusTh/Yb diagram (after Pearce 1982), showing sourcecharacteristics for the metamorphic-sole rocks and isolateddykes of the Divri¤i ophiolite. Fields of OIB and MORB arefrom Harms et al. (1997). Data for the mafic dykes of theTauride ophiolites are the same as in Figure 5.

alkaline amphibolites appear to have been derived froman enriched mantle source region with no subductioncomponent (Figure 9b). The five samples of isolateddykes exhibit a shift towards higher Th values and wereprobably derived from an enriched mantle source,modified by the addition of a subduction component(Figure 9b).

Tectonic-environment discrimination diagrams basedon immobile trace elements are presented in Figure 10.The Zr-Nb-Y triangular plot of Meschede (1986) and theZr/Y versus Zr plot of Pearce & Norry (1979) showwithin-plate affinities for the alkaline amphibolites andisolated dykes, and island-arc affinities for the tholeiiticamphibolites of the Divri¤i ophiolite.

Discussion

Shervais (2001) reviewed the literature on subduction-related ophiolites and proposed an evolutionary scenariothat consisted of five stages, overlapping each other intime and space. In his analysis, he compared ophioliteevolution to the biological life cycle: namely, the birth,youth, maturity, death and resurrection stages. Each ofthese stages has its own geological, petrographical andgeochemical features. The eastern Mediterraneanophiolites possessed most of these characteristics during

their evolution – from birth to resurrection stages. Oneof the most important stages in this cycle appears to bethe death stage, at which time the high-grademetamorphic sole is formed and OIB-type enrichedmagmas supply lavas or dykes which invade plutonitesand the metamorphic sole prior to ophioliteemplacement. A number of ophiolite examples possessthese features, including the Coastal Range ophiolite ofCalifornia (the Stonyford Volcanic Complex) (Shervais &Hanan 1989; Shervais & Beaman 1991), the Omanophiolite (the Salahi volcanics) (Alabaster et al. 1982),and the Pozant›-Karsant› ophiolite in Turkey (thepyroxenite dykes) (Çelik 2002). Dilek & Flower (2003)proposed a tectonic model depicting the late-stage (i.e.,prior to trench-passive margin collision and subsequentophiolite emplacement) petrogenetic evolution of theSemail (Oman) ophiolite. The latter authors suggestedthat the late-stage alkali basalts and dykes of the Salahiunit were probably the result of off-axis magmatism fedby melts that originated within an asthenospheric windowas a result of delamination of subducting lithosphereshortly before the emplacement of the ophiolite onto theArabian continental margin.

The magmatic and metamorphic processes during thedeath stage of the suprasubduction-zone life cycle of theDivri¤i ophiolite are well constrained by the presence of

O. PARLAK ET AL.

39

A

B

C

D

Zr/4 Y

Nb*2

10 100 10001

10

20

A - within plate basaltsB - island arc basaltsC - mid-ocean ridge basalts

A

B

C

Zr

Zr/

Y

A: WPBB: E-MORBC: VABD: VAB-MORB


(b)(a)

Figure 10. Tectonomagmatic discrimination diagrams for the metamorphic-sole rocks and isolated diabase dykes of the Divri¤iophiolite. (a) after Pearce & Norry (1979) and (b) after Meschede (1986).

the metamorphic sole and the alkaline isolated dykes. Theprotoliths of the metamorphic-sole rocks include bothalkaline and tholeiitic magma types. The major-, trace-and rare-earth-element geochemistry of the alkalineamphibolites suggest that these rocks were derived froman enriched mantle source and do not exhibit asubduction-zone component on the basis of Th/Yb andTa/Yb ratios (Figure 9b). Therefore, these rocks aregeochemically similar to seamount-type alkaline basalts.Jurassic–Cretaceous seamount-type alkaline basalts cropout extensively along the Neotethyan sutures of Turkey(e.g., Floyd 1993; Parlak et al. 1995; Lytwyn & Casey1995; Dilek et al. 1999; Parlak 2000; Rojay et al. 2001;Çelik & Delaloye 2003; Vergili & Parlak 2005). Theserocks are considered to have accreted to the base of theNeotethyan ophiolites to form metamorphic soles duringthe Late Cretaceous. The tholeiitic amphibolites of themetamorphic sole were derived by the metamorphism ofan IAT-type basaltic protolith during intraoceanicthrusting/subduction, and show a minor subduction-zonecomponent based on the Th/Yb and Ta/Yb ratios (Figure9b). These volcanic rocks were presumably detachedfrom the front of the overriding SSZ-type crust and werethen underplated and metamorphosed. The alkalineisolated dykes cutting the metamorphic sole and mantletectonites were probably derived from an asthenosphericwindow with some modification by a subductioncomponent based on the evidence of Th/Yb and Ta/Ybratios (Figure 9b).

The Late Cretaceous Neotethyan palaeogeography ofthe eastern Mediterranean region involved three differentbranches of oceanic basins separated by continentalfragments and platform carbonates. These are northernNeotethys, southern Neotethys and the Inner Taurideocean (fiengör & Y›lmaz 1981; Robertson & Dixon 1984;Görür et al. 1984; Dilek et al. 1999). The Divri¤iophiolite is located within the Tauride belt in the easternpart of Central Anatolia. Although there have beennumerous studies on the origin of the Tauride ophiolites,their root zone is still debated. Göncüo¤lu et al. (1996-1997) and Gürer & Aldanmaz (2002) suggested that theTauride ophiolites formed in a suprasubduction-zonetectonic setting in the northern branch of Neotethys andwere thrust over the K›rflehir-Ni¤de metamorphicsmassifs, then over the Bolkarda¤/Alada¤ carbonateplatforms in the Late Cretaceous (Figure 11). Accordingto some workers (Özgül 1976, 1984; Monod 1977;fiengör & Y›lmaz 1981; Lytwyn & Casey 1995; Polat &

Casey 1995; Polat et al. 1996; Dilek & Whitney 1997;Collins & Robertson 1998; Dilek et al. 1999; Parlak &Robertson 2004), all of the Late Cretaceous Taurideophiolites are interpreted as remnants of a single vastophiolitic thrust sheet generated within Neotethys to thenorth of the Tauride carbonate platform, called the InnerTauride Ocean (Görür et al. 1984). They concluded thatthe Tauride ophiolites formed above a N-dippingintraoceanic subduction zone (SSZ-type) between theAnatolides to the north and the Tauride carbonateplatform to the south (Figure 11). There are several linesof evidence, supporting this model of ophioliteemplacement over the Tauride carbonate platform. Theseare as follows: The Central Anatolian ophiolites differlithologically and chemically from those emplaced overthe Tauride platform. There are number of isolateddismembered ophiolites lying structurally above theK›rflehir and Ni¤de metamorphic massifs (Yal›n›z &Göncüo¤lu 1998; Floyd et al. 2000). Their overallstratigraphy is as follows: the lowest part is composed ofultramafic rocks overlain by layered and isotropicgabbros. These are followed upwards by plagiogranite,then dolerite dykes, pillow basalts and acidic extrusives.Epiophiolitic sediments are of middle Turonian–earlySantonian age according to Yal›n›z (1996). Both ophioliteand overlying sediments were later intruded bypostcollisional quartz monzonite dated as 81–67 Ma(Yal›n›z et al. 1999). Geochemical data indicate that thebasalts and dolerites of the volcanic sequence are of IATtype, whereas the late dolerite dykes have compositionsmore akin to N-MORB (Yal›n›z et al. 1996). Bycomparison, the Tauride ophiolites display more intactophiolite stratigraphy. A thick slab of residual mantledominated mainly by harzburgite is tectonically underlainby dynamothermal metamorphic soles exhibiting invertedmetamorphic gradient (from amphibolite to greenschistfacies), well-preserved ultramafic and mafic cumulateswith a thickness of over 3 km, isotropic gabbros, basalticpillow lavas and associated sediments. Isolateddolerite/diabase dykes intruded the Tauride ophiolites andthe underlying metamorphic soles. Both the basaltic rocksin the volcanic sequence and the isolated diabase dykeswhich intrude the ophiolites are of IAT type (Parlak &Delaloye 1996; Parlak 2000; Elitok 2001; Çelik &Delaloye 2003). Dilek & Whitney (1997) and Okay(1989) mentioned the local presence of HP/LTmetamorphic rocks along the northern edge of theBolkarda¤ platform and in Tavflanl› (Kütahya) region,perhaps due to subduction and later exhumation of the


40

leading edge of the Tauride platform. Robertson (2002)noted that, if the K›rflehir/Ni¤de metamorphic rocksformed part of the Tauride platform, a large amount ofcontinental crust would have to be subducted. There isvery little evidence of regional HP/LT metamorphismwithin the K›rflehir/Ni¤de metamorphic units. Theophiolite geology and the geochemical features of theTauride ophiolites suggest that an oceanic basin existed inthe interval from Late Triassic to the Late Cretaceous, andwas located between the Tauride platform to the southand the Anatolides to the north (Figure 11).

The geological, geochemical and regional tectoniccontext of the Tauride belt is consistent with thefollowing evolving scenario: The Divri¤i ophiolite formedabove a north-dipping subduction zone (SSZ setting)within the Inner Tauride Ocean (Görür et al. 1984),between the K›rflehir Massif to the north and the Taurideplatform to the south, in the Late Cretaceous (Figure12a) (Parlak et al. 2005). During intraoceanicsubduction, IAT-type volcanic rocks were detached from

the forward edge of the overriding SSZ-type crust whileseamount alkaline volcanic rocks from the top of thesubducting plate were metamorphosed to amphibolitefacies as the plate was subducted (Figure 12b). Late-stagemagmatic activity prior to the emplacement of the Divri¤iophiolite was represented by the intrusion of isolateddykes that were generated in an asthenospheric windowdue to slab break-off (Figure 12c). A similar model hasbeen proposed by Dilek & Flower (2003) for the Salahivolcanics in the Oman ophiolite. Boztu¤ et al. (2005)reported that the A-type Dumluca and Murmanagranitoids intrude Late Cretaceous ophiolitic units in theDivri¤i (Sivas) area. They concluded that these granitoidsresulted from the slab break-off stage of the Neotethyanconvergence system.

Conclusions

The Divri¤i ophiolite comprises three tectonic units (inascending order): the ophiolitic mélange, the

O. PARLAK ET AL.

41

CO

R/SM BS

AES

KN

SC

IASAM

V

P

PO

AP MTauri

des

A C

ITO

?

?

?

?

?

S. NEOTETHYS

subduction zone

N. NEOTETHYS

Latest Cretaceous

30 NO

Figure 11. Simplified palaeogeographic sketch map of the eastern Mediterranean during the Late Cretaceous (fromRobertson, 2002). A– Antalya, AES– Ankara-Erzincan suture zone, AM– Ankara mélange, AP– Apulia, BS:Black Sea marginal basin, C– Cyprus, CO– Carpathian ocean, IAS– ‹mir-Ankara suture zone, ITO– InnerTauride ocean, KN– K›rflehir/Ni¤de metamorphic massif, M– Menderes Massif, P– Pelagonian, PO– Pindosocean, R/SM– Rhodope/Serbo-Macedonian, SC– Sakarya metamorphic massif, V– Vardar.

metamorphic sole and the ophiolite unit. Itstectonostratigraphy is similar to that found in other partsof the Tauride ophiolite belt. Therefore the Divri¤iophiolite is thought to have been derived from the InnerTauride ocean which was located between the K›rflehirblock and the Tauride platform in the Late Cretaceous.

The metamorphic-sole rocks comprise two distinctgeochemical groups. The first group is alkaline(Nb/Y=1.77–3.48), whereas the second group istholeiitic (Nb/Y=0.07–0.18) in nature. The REE patterns,multi-element and tectonomagmatic discriminationdiagrams suggest that the alkaline amphibolites formedas a result of metamorphism of seamount-type basalticrocks in an intraoceanic subduction-zone setting, whereas

the tholeiitic amphibolites formed as result ofintraoceanic thrusting in a suprasubduction-zone (SSZ)basin.

The isolated dykes exhibit alkaline (Nb/Y=0.68–2.11)affinity. The major-, trace- and rare-earth-elementgeochemistry of the dykes show that they formed in awithin-plate environment. The Th values of the isolateddykes are higher than normal within-plate alkalinemagmas; this situation is interpreted as indicating thatthe isolated dykes were probably derived from anenriched mantle source modified by the addition of asubduction component.

The late-stage isolated dykes may be a result of off-axis magmatism fed by melts that originated within an


42

S N

SSZ-typeDivriği ophiolite

seamountalkali basalt

Taurideblock

Kırşehirblock

Late Cretaceous (a)

Taurideblock

Late Cretaceous

alkaline & tholeiiticbasalt basalt

Kırşehirblock

(b)

Late Cretaceous

Metamorphic sole

asthenosphericwindow

OIB sourceasthenosphere

delaminatedslab sinking into mantle

Kırşehirblock

Taurideblock

(c)

Figure 12. A tectonic model for the genesis of the Divri¤i ophiolite and metamorphic-sole rocks.

asthenospheric window due to slab break-off, shortlybefore the emplacement of the Divri¤i ophiolite onto theTauride passive margin in the Late Cretaceous.

Acknowledgements

This research was partially funded by ÇukurovaUniversity, Division of Scientific Research Projects

(Project No: MMF2003BAP16), and by a TurkishAcademy of Sciences grant to Osman Parlak, in theframework of the Young Scientist Award Program(TÜBA-GEB‹P/2003-111). The authors would like tothank Abdel Rahman Fowler, Ercan Aldanmaz and ErdinBozkurt for their valuable scientific and technicalcomments that improved the quality of the presentmanuscript.

O. PARLAK ET AL.

43

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Origin and Tectonic Significance of the Metamorphic Sole and