Geochemistry of I-type granitoids in the Karaburun Peninsula, West Turkey: Evidence for Triassic...

Research ArticleGeochemistry of I-type granitoids in the Karaburun Peninsula, WestTurkey: Evidence for Triassic continental arc magmatism following

closure of the Palaeotethys

SIBELTATAR ERKÜL,1* HASAN SÖZBILIR,2 FUAT ERKÜL,3 CAHIT HELVACI,2 YALÇIN ERSOY2

AND ÖKMEN SÜMER2

1Department of Geological Engineering, Faculty of Engineering, Akdeniz University, TR-07058 Antalya, Turkey(email: [email protected]), 2Department of Geological Engineering, Faculty of Engineering, Dokuz Eylül

University, TR-35160 Izmir, Turkey, and 3Akdeniz University, Faculty of Education, TR-07058 Antalya, Turkey

Abstract Triassic granitoids related to Palaeo- and Neo-Tethyan events occur widely in themetamorphic terranes largely affected by the Alpine orogeny. A first recorded unmeta-morphosed plutonic body intruded into the Palaeotethyan mélange in western Turkey,called the Karaburun granodiorite, is composed of two small intrusive stocks that wereemplaced between 240 and 220 Ma. It is compositionally diverse, ranging from granodioriteand tonalite to diorite. These rocks show heterogeneous compositions with 54 to 65 wt %SiO2 and are calc-alkaline in character. They are also subalkaline with molar ratios ofAl2O3/(Na2O + K2O) from 0.74 to 1.00 and are metaluminous. Most samples are diopside-normative (0.36–8.64), with Na2O > K2O. Chondrite normalized rare earth element (REE)patterns show various degrees of light REE (LREE) enrichment, with LaN = 57.79 to 99.59and (La/Yb)N = 5.98–7.85 and Eu negative anomalies (Eu/Eu* = 0.62–0.86). These rockshave coherent patterns in ocean ridge granite (ORG) normalized trace-element plots,marked by variable enrichment in K, Rb, Ba, Th, Ce and depletion in Ta and Nb, similar toI-type granites from subduction zones. In primitive mantle-normalized multi elementvariation diagrams, the granodiorites show pronounced depletions in the high-field-strengthelements (HFSE; Nb, Ta, Zr), Sr, P, and Ti. Trace-element modeling of the Karaburungranodiorite suggests an origin through partial melting of the subduction-modified mantlewedge with minor contribution of crustal components through a process of strong fractionalcrystallization (FC) combined with slight assimilation-fractional crystallization (AFC).Exposures of typical continental-arc granodiorites in the Karaburun Mélange support thevalidity of the subduction-accretion model that implies the presence of an active continentalmargin following closure of the Palaeotethyan Ocean during the Triassic.

Key words: active continental margin, mantle wedge, Neotethys, Palaeotethys, Triassic,volcanic arc granitoids.

INTRODUCTION

Western Anatolia, which is located in the tectoni-cally active Alpine–Himalayan orogenic belt,exposes granitic rocks of Precambrian to MiddleJurassic, Triassic and Late Cretaceous to Miocene

ages (Ustaömer 1999; Delaloye & Bingöl 2000;Okay & Satır 2000; Koralay et al. 2001, 2004;Bozkurt 2004; Ustaömer et al. 2005; Altunkaynak2007; Glodny & Hetzel 2007). These rocks, whichform an east–west-trending zone across westernTurkey, have diverse tectono-magmatic historiesand intrude various lithologies of the Palaeozoic–Early Mesozoic units (Okay & Tüysüz 1999;Delaloye & Bingöl 2000). Although previous

*Correspondance

Received 3 July 2007; accepted for publication 9 April 2008.

Island Arc (2008) 17, 394–418

© 2008 The AuthorsJournal compilation © 2008 Blackwell Publishing Asia Pty Ltd

doi:10.1111/j.1440-1738.2008.00627.x

mailto:[email protected]

geochronological studies revealed the presence ofTriassic magmatism in western Anatolia, the geo-dynamic setting of the Triassic granitic plutons ispoorly known. In this paper, we discuss the geo-dynamic significance of the unmetamorphosedTriassic granitic rocks related to Palaeo- andNeo-Tethyan events on the basis of geological,petrographic, and geochemical data.

BACKGROUND INFORMATION

Published work has mainly focused on the tectonicsetting of the Palaeo- and Neo-Tethyan units inthe Karaburun Peninsula and its surroundings,based on palaeontological and structural data(Fig. 1). Particular attention was paid to mecha-

nisms of mélange formation and their relationshipto the closure and opening of the Tethyan ocean(Erdogan 1990; Kozur 1997; Robertson & Pickett2000). However, the geochemical and petrologicalfeatures of the Triassic granitic rocks and theimportant Karaburun granodiorite have not yetbeen documented in detail. Magmatism of Triassicage has been established in the Menderes Massif(Koralay et al. 2001), the Cycladic Massif (Reis-chmann 1997; Ring et al. 1999), and the KaraburunBelt (Türkecan et al. 1998; Çakmakoglu & Bilgin2006). Triassic leucocratic granites occur in theMenderes Massif and intrude metapelitic rocks.Associated orthogneisses are fine-grained andenriched in felsic minerals. The crustally derivedleucocratic orthogneisses were shown to havea chemical composition typical of calc-alkaline,

Fig. 1 Generalized tectonic map of theAegean region (modified after Ring et al.1999, 2001). Inset shows tectonic units ofTurkey (after Okay et al. 1996; Okay & Tüysüz1999).

Geochemistry of the Karaburun granodiorite 395


S-type, peraluminous granite (Koralay et al. 2001).These Triassic leucocratic granites are consideredto have been emplaced immediately after theclosure of the Palaeotethys (Koralay et al. 2001).During the Alpine Orogeny, they underwentgreenschist-facies metamorphism, which occurredduring the juxtaposition of the Menderes Massifwith the structurally overlying units of Cycladicblueschist, the Izmir–Ankara–Erzincan Sutureand the Lycian nappes (Gessner et al. 2001).Similar exposures of magmatic rocks have beendocumented in the island of Samos, where theAmpelos nappe of the Cycladic Massif consistsof quartzite, phyllite, and chloritoid-kyaniteschist with marble, glaucophane-epidote schist,and greenschist units, and is intruded by Triassicgranite (Pb-Pb zircon ages of 230–240 Ma,Reischmann 1997). The Ampelos nappe, post-Carboniferous in age underwent Cretaceous blue-schist metamorphism overprinted by Tertiarygreenschist-facies metamorphism (Ring et al.1999).

The intrusive rocks of the Karaburun Peninsulawere mapped by Erdogan (1990) and Çakmakogluand Bilgin (2006). Erdogan (1990) considered theKaraburun granodiorite as several intrusivestocks of Neogene age that intruded into theScythian–Anisian Karareis Formation. The sameintrusive stocks were described by Türkecan et al.(1998) as the Karaburun intrusion, which yielded a239.9 � 2.4 Ma Rb–Sr biotite age. Recent classicU–Pb dating studies on the Karaburun granodior-ite yielded ages of 222.7 � 2.5 and 228.6 � 2.7 Maon a zircon concentrate (Akal et al. 2007).

GEOLOGICAL SETTING

The Late Palaeozoic–Early Mesozoic units in theAegean region define four distinct tectonostrati-graphic units, from north to south: (i) the SakaryaZone (e.g. the Karakaya complex) (Sengör et al.1984; Okay & Tüysüz 1999; Stampfli 2000; Okay &Altıner 2004; Okay & Göncüoglu 2004; Okay et al.2006), (ii) Izmir–Ankara–Erzincan Suture Zoneincluding the Karaburun Belt (Erdogan 1990;Okay & Tüysüz 1999; Okay et al. 2001, 2002; Çak-makoglu & Bilgin 2006) (Fig. 1), (iii) MenderesMassif-Cycladic Massif and (iv) Lycian nappes(Sengör & Yılmaz 1981; Robertson & Pickett 2000;Bozkurt & Oberhänsli 2001; Rimmelé et al. 2005)(Fig. 1). These units have distinct characteristicsin terms of stratigraphy, structure, and degreeof metamorphism. The Sakarya Zone consists of

highly deformed and slightly metamorphosedclastic and volcanic series of Permian and Triassicage. The Izmir–Ankara–Erzincan Suture Zone ischaracterised by Palaeocene and younger thrustzones that form the main boundary betweenthe Karakaya complex in the north and theAnatolide-Tauride block in the south (Erdogan1990; Erdogan et al. 1990; Okay et al. 1996, 2001;Okay & Tüysüz 1999; Okay 2000; Okay & Altıner2007). The suture is represented by voluminoussubduction-accretionary complexes attributed tothe consumption of the Neotethys oceanic litho-sphere. The rock units of the accretionarycomplexes consist of chaotically deformed lateMaastrichtian to Palaeocene greywackes with Tri-assic to Cretaceous limestone and rare peridotite,radiolarian chert, and basalt blocks in the westernpart (e.g. Bornova Flysch Zone; Fig. 1) (Okay &Siyako 1993). The central part of the Izmir–Ankara–Erzincan Suture Zone is dominated byCretaceous blueschists, accretionary complex andophiolites that are intruded by Eocene granodior-ites. The Karaburun Belt lies to the far west ofthe Izmir–Ankara–Erzincan Suture Zone witha platform-type carbonate succession, and isincluded in the continuation of the Sakarya conti-nent in the classification of the cratonic realmsof western Turkey (Sengör & Yılmaz 1981). TheKaraburun Belt, also named Karaburun Mélange,is made up of Silurian–Upper Carboniferous exoticblocks within a sheared matrix of siliciclasticturbidites (Robertson & Pickett 2000). The struc-turally underlying Cycladic Massif is composedof eclogites, blueschists, and high-pressure olisto-stromal units (Oberhänsli et al. 2001). The Cycla-dic units rest on the Menderes Massif, consistingof metasediments, metabasic rocks, and Early-Middle Triassic granitic rocks (Koralay et al. 2001),and orthogneisses (Koralay et al. 2004). Both theCycladic and Menderes massifs are structurallyoverlain by metasediments that have undergonehigh-pressure metamorphism, and ophiolites ofthe Lycian nappes (Güngör & Erdogan 2001;Oberhänsli et al. 2001; Collins & Robertson 2003;Jolivet et al. 2004; Rimmelé et al. 2005).

STRATIGRAPHY

Following the first geological mapping of theKaraburun Peninsula (Kalafatçıoglu 1961), studieshave been carried out owing to the presence thereof both Palaeotethyan and Neotethyan units (e.g.Erdogan 1990; Erdogan et al. 1990; Robertson &

396 S. T. Erkül et al.


Pickett 2000) (Fig. 2). According to Erdogan et al.(1990), the oldest unit in the Karaburun Peninsulais the Early–Middle Carboniferous Alandere For-mation, which consists of fossiliferous shallowmarine limestone. The unit is unconformably over-lain by the Early Triassic (Scythian–Anisian) Den-izgiren Group, divided into two formations, theKarareis and Gerence formations, interfinger-ing with each other. These formations are com-monly intercalated with andesitic and dacitic lavas,volcaniclastic rocks (Robertson & Pickett 2000),submarine basaltic lavas, and basic pyroclastic andvolcaniclastic rocks (Çakmakoglu & Bilgin 2006).The stratigraphic position of these extrusive rockswithin sedimentary successions is controversialowing to the poor preservation of original contactsafter late-stage deformational events. Erdoganet al. (1990) interpreted the Lower Triassiccarbonate platform with the extrusive rocks tohave been formed on the uppermost part of theKarareis Formation. In contrast, Robertson andPickett (2000) proposed that the andesitic anddacitic extrusive rocks are intercalated with thecarbonate successions and are included withinthe Gerence Formation. The Karareis andGerence formations are conformably overlainby the Ladinian-Carnian Camibogazı Formation.However, Kozur (1997) proposed that the Kara-reis Formation includes various lithological andtectonostratigraphic units and thus, cannot beregarded as a formation. It consists of Ordovicianlow-grade slates, quartzites, and greywackes,

Silurian laminated mudstones, greenish blackradiolarites, siliciclastic turbidites, and an olisto-stromal series (graded sandstones, greywackes,laminated mudstones, and black keratophyretuffs), Devonian light-grey limestones, Carbo-niferous siliciclastic turbidites, radiolarites,olistostromes and mafic volcanic rocks, Viseanpelagic, cherty limestones, Bashkirian fossilifer-ous shallow-water limestones, sandstones, mud-stones, and conglomerates, ammonoid-bearingmudstones, pelagic limestones and thin tuff, andLate Permian pink dolomites and limestones.According to Kozur (1997), the Scythian–Ladinianrocks do not interfinger with the Palaeozoic rocks,as formerly claimed by Erdogan et al. (1990),but instead represent several tectonic slices. Incontrast to these views, Robertson and Pickett(2000) claimed that all the Palaeozoic units are setin a matrix of siliciclastic turbidites, pelagiccarbonates, and channelized conglomerates ofLate Palaeozoic age. These rock units are uncon-formably overlain by the Early Triassic basinalsuccession, the Gerence Formation. According tothe authors, the Late Palaeozoic units in theKaraburun Peninsula formed the basement for acarbonate-dominated succession interruptedlycontinued from Early Triassic to Maastrichtiantime. The units of the Karaburun Peninsula wereregarded as a complex unit interpreted as anUpper Palaeozoic–Lower Permian subduction-accretion complex, developed near the southernmargin of a Palaeotethyan oceanic basin.

Fig. 2 Generalized stratigraphic section of the Karaburun units in the study area and its correlation with previous studies.



Subduction-accretion was followed by riftingand passive margin evolution of a Neotethyanoceanic basin that was sutured in Early Tertiarytime (Robertson & Pickett 2000). A recent studycarried out by Çakmakoglu and Bilgin (2006)re-established the Palaeozoic–Mesozoic stratigra-phy of the Karaburun Peninsula (Fig. 2). They sub-divided the pre-Mesozoic stratigraphy into threeconformable units; these are from bottom to top,Cambrian(?)–Ordovician Küçükbahçe Formation,Silurian–Carboniferous Dikendagı Formation, andVisean–Bashkirian Alandere Formation. Theserock units are intruded by the Triassic Karaburungranodiorite. The unconformably overlying unitis the Skithian–Anisian Gerence Formation.However, our field study indicates that theKaraburun granodiorite only intruded into theDikendagı Formation (Fig. 2). There, the forma-tion consists of an alternation of greenish grey,yellowish brown sandstone, mudstone, and blackchert. In the turbiditic part of the unit, severalolistostromal levels containing blocks of recrystal-lized limestone are present. The fossil content ofthe formation yielded Silurian–Carboniferous age

(Kozur 1997). These rock units are overthrust bythe late Cretaceous–Palaeocene Bornova Mélange,including mega-blocks of the Ladinian–CarnianCamibogazı Formation. The Ladinian–CarnianIdecik Formation consist of spilitic lava andpyroclastic-volcaniclastic rocks intercalated withcherty limestones and reddish radiolarites (Çak-makoglu & Bilgin 2006); Fig. 2). All the rock unitsare unconformably overlain by the Early Miocenevolcano-sedimentary sequence.

FIELD RELATIONS, ROCK TYPE AND PETROGRAPHYOF THE KARABURUN GRANODIORITE

The Karaburun granodiorite covers an area ofabout 4 km2 in the northern part of the KaraburunPeninsula and crops out as two stocks lying N–S indirection (Fig. 3). The eastern margin of thesestocks is cut by N–S-trending strike-slip faults.The Karaburun granodiorite intruded the Dik-endagı Formation of the Karaburun Mélange(Fig. 4a,b). It consists of a suit of granodioritic,tonalitic, dioritic rocks, and minor aplitic dykes.

Fig. 3 Geological map of the study area (Erdogan et al. 1990; Çakmakoglu & Bilgin 2006) and compiled with our own observations.



Granodioritic and tonalitic-dioritic compositionscan be easily distinguished in the field by theircolour index. The Karaburun granodioriteintrudes shales and sandstone, which are trans-formed into hornfelsic rocks that can be followedin a zone a few metres wide along the contact(Fig. 5).

Rock samples from the Karaburun granodio-rite are usually altered and are characterizedby a medium-grained holocrystalline texture(Table 1; Fig. 6a,b). They consist mainly of quartz,K-feldspar, plagioclase, tremolite-actinolite, andminor hornblende, augite, and biotite (Fig. 6a–f).Common minor phases are apatite, zircon, titanite,and magnetite (Fig. 6g,h). Quartz is usually anhe-dral and interstitial. The K-feldspar generally dis-plays carlsbad twinning and occurs as tabularprismatic crystals that commonly display incipientalteration to white mica and clay minerals. Sub-hedral prismatic plagioclase crystals are usuallyaltered to white mica and kaolinite (Fig. 6c,d). Sec-ondary chlorite after biotite and hornblende ispresent in many samples. Euhedral and subhedralcrystals of hornblende and augite are scarce.Pyroxene appears as a relic in the core oftremolite-actinolite grains (Fig. 6e,f). These types

of alteration indicate somewhat high degree ofpost-magmatic and fluid-dominated adjustmentsof the mineralogy. Minerals are lacking defor-mation; all rocks have a magmatic fabric. Theoverall mineralogical composition of the Karabu-run granodiorite samples defines it as an I-typegranite (Chappell & White 1974, 2001) (Fig. 6a–h;Table 1).

Fig. 4 (a) Geological cross-section show-ing contact relationships of the Palaeotethyanand Neotethyan units, (b) Field photographshowing the contact relationship between theKaraburun Mélange and the intruding Karabu-run granodiorite. Field of view is about500 metres across.

Fig. 5 Close-up view of the hornfelsic contact zone between theKaraburun Mélange and the Karaburun granodiorite.



GEOCHEMISTRY

ANALYTICAL PROCEDURES

Whole-rock powders were prepared from 12 freshsamples in a tungsten carbide shatter box formajor- and trace- element analysis. Element abun-dances were determined by inductively coupled–plasma-atomic-emission spectrometry (ICP–AES)(major elements) and inductively coupled–plasma-mass spectroscopy (ICP–MS) (trace elements) inACME Laboratory, Canada. Total abundancesof the major oxides and several minor elementsare reported for a 0.1 g sample analysed byICP-emission spectrometry following a lithiummetaborate-tetraborate fusion and dilute nitricacid digestion. Loss on ignition (LOI) is deter-mined as the weight difference after ignition at1000°C. Rare earth and refractory elements aredetermined by the ICP–MS technique following alithium metaborate-tetraborate fusion and nitricacid digestion of a 0.1 g sample.

WHOLE-ROCK COMPOSITION AND CLASSIFICATION

The chemical compositions of rock samples fromthe Karaburun granodiorite are summarised inTable 2 and are plotted in the Q–P diagram ofDebon and Le Fort (1983). Most rock samples plotin the tonalite and granodiorite fields (Fig. 7). TheKaraburun granodiorite is medium to high-K (LeMaitre et al. 1989), calc-alkaline (Irvine & Baragar1971), and I-type in character according to majorand trace element data (Fig. 8a–f, Tables 2,3). It ismainly intermediate in composition with SiO2

ranging from 54.01 to 65.07%. The samples have

medium to high K2O (0.98–3.29%), Na2O, Rb, Ba,Zr, and total REE, whereas tFe2O3 (4.67–8.87%),MnO (0.08–0.14%), MgO (1.68–6.36%), CaO (4.11–7.76%), TiO2 (0.46–0.86%), and P2O5 (0.10–0.21%)contents are relatively high. The Al2O3 contentis between 13.47 and 16.63% (Fig. 9a–v; Table 2).The Aluminum Saturation Index (A/CNK = Al2O3/[CaO + K2O + Na2O]molar unit) indicates that thesamples are metaluminous (Fig. 8d) and containnormative diopside (Fig. 8f). They also have lowMg numbers [Mg# = molar 100*Mg/(Mg + Fe+2)](Table 2). According to these chemical signatures,together with the occurrence of biotite and horn-blende in the samples, the samples from theKaraburun granodiorite belong to the I-type cat-egory (cf. Chappell & White 1974, 2001) (Fig. 8d–f,Table 3). Harker variation diagrams show thatthree samples are distinctly clustered than theother samples depending on their high silicacontent (>64.46%) (Fig. 9a–v). All samples remainon the same line, suggesting that there is a com-positional gap between two distinctly clusteredsamples. The TiO2, Al2O3, Na2O, K2O, and P2O5

values display strong positive correlation alongwith increasing silica content, whereas tFe2O3,MgO, CaO, and MnO show negative trends(Fig. 9a–i). The trace elements exhibit consider-ably similar trends to those of the major elements:Ni, V, and Zn decrease generally with increasingSiO2, whereas K and Rb (Fig. 9e,k) contentsincrease with increasing silica (Fig. 9r,t,u). Theelement Sr (Fig. 9l), is mainly contained in plagio-clase and accompanied by Ca, and shows a nega-tive trend with respect to silica content. Aslarge-ion lithophile elements (LILE) are easilyremobilised from the crystal lattice during alter-

Table 1 Petrographic features of the Karaburun granodiorite

Sample Location Texture Grain Size Mineralogical composition Rock type†

SK-1

Karaburun Holocrystallinegranular

Fine-medium

Qtz, Or, Pl, Tre/Act, Ap, Aug, Arg, Ser, Op TonaliteSK-2 Qtz, Or, Pl, Hb, Tre/Act, Ap, Zir, Chl, Arg, Car, Ep, Op TonaliteSK-3 Qtz, Or, Pl, Arg, Ser, Chl, Epi GranodioriteSK-4 Qtz, Or, Pl, Tre/Act, Aug, Ap, Zir, Chl, Arg, Ser TonaliteSK-5 Qtz, Or, Pl, Tre/Act, Aug, Ap, Zir, Bio (Chl), Tour, Op GranodioriteSK-6 Qtz, Or, Pl, Hb, Tre/Act, Ap, Zir, Chl, Arg, Epi, Op GranodioriteSK-7 Qtz, Or, Pl, Bio, Aug, Ap, Arg, Ser, Op GranodioriteKB-1 Qtz, Or, Pl, Tre/Act, Aug, Ap, Zir, Bio (Chl), Tour, Op GranodioriteKB-2 Qtz, Or, Pl, Tre/Act, Aug, Ap, Zir, Chl, Arg, Ser TonaliteKB-3 Qtz, Or, Pl, Hb, Tre/Act, Ap, Zir, Chl, Arg, Epi, Op GranodioriteKB-4 Qtz, Or, Pl, Tre/Act, Aug, Ap, Zir, Chl, Arg, Ser TonaliteKB-5 Qtz, Or, Pl, Hb, Tre/Act, Ap, Zir, Chl, Arg, Epi, Op Granodiorite

†Rock type is taken from Debon and Le Fort (1983).Ap, Apatite; Arg, argillisation; Aug, augite; Bio, biotite; Car, carbonatisation; Chl, chloritisation; Ep, epidote; Hb, hornblende; Op, opaque

mineral; Or, Orthoclase; Pl, plagioclase; Qtz, quartz; Ser, sericitisation; Tour, tourmaline; Tre/Act, tremolite/actinolite; Zir, zircon.



ation, Ba and Cs contents are quite low (Table 2).Plots of the high-field-strength elements (HFSE)elements Zr, Th, and Y (Fig. 9m–o) vs silicacontent show a positive correlation. The oceanridge granite (ORG)-normalized multi-elementdiagram of the Karaburun granodiorite samplesdisplays enrichment in LILE and depletion inHFSE (Fig. 10a). The patterns of the granodior-ites are similar to those of volcanic arc granites(Fig. 10a). The REE patterns of all analyzedsamples from the Karaburun granodiorite rocksare characterized by light REE-enriched patterns

[(La/Yb)N = 5.98–7.50], with relatively flat heavyREE and small negative Eu anomalies (Eu/Eu* = 0.62–0.77) (Fig. 10b; Table 2).

GEOCHEMICAL EVIDENCE FOR ARC MAGMATISM

Geochemical characteristics of subduction-relatedtectonic settings (e.g. island arc or continentalarc) are generally enrichment in the abundancesof some of the incompatible trace elements suchas LILE (Rb, K, Ba, Sr) and light rare-earth ele-ments (La, Ce, Nd), but a strong depletion in

Fig. 6 Microscopic views from the Karabu-run granodiorite. Qtz, quartz; Pl, plagioclase;Or, orthoclase; Hb, hornblende; Tre/Act,tremolite/actinolite; Ap, apatite.



Tabl

e2

Maj

oran

dtr

ace

elem

ent

com

posi

tion

sof

the

Kar

abur

ungr

anod

iori

tean

dex

trus

ive

rock

sam

ples

Sam

ple

SK-1

SK-2

SK-3

SK-4

SK-5

SK-6

SK-7

KB

-1K

B-2

KB

-3K

B-4

KB

-5S

O-1

8C

SC2a

†2d

†2e

†

Maj

orel

emen

ts(w

t%)

SiO

258

.02

59.1

959

.53

55.8

156

.13

64.4

656

.84

56.7

464

.67

59.4

554

.01

65.0

758

.17

61.1

473

.46

62.9

3A

l 2O3

13.4

714

.57

16.6

313

.72

15.0

314

.48

15.1

614

.14

14.2

214

.79

15.0

614

.39

14.1

314

.62

13.4

413

.82

Fe 2

O3

7.65

6.96

6.76

8.87

8.41

5.57

8.29

8.24

6.28

7.33

8.68

4.67

7.62

6.10

2.72

7.67

MgO

5.60

3.25

1.96

6.33

4.93

2.42

4.97

5.92

1.68

3.51

6.36

2.15

3.34

0.98

0.64

0.85

CaO

7.24

7.25

5.47

7.16

6.55

4.53

6.93

6.72

4.87

5.82

7.76

4.11

6.37

5.27

2.19

4.58

Na 2

O2.

102.

032.

402.

351.

822.

502.

021.

842.

602.

212.

002.

593.

682.

592.

971.

42K

2O1.

561.

382.

480.

981.

942.

481.

781.

901.

392.

451.

503.

292.

162.

752.

182.

83T

iO2

0.53

0.69

0.84

0.59

0.63

0.55

0.64

0.54

0.86

0.67

0.55

0.46

0.69

0.79

0.71

0.74

P2O

50.

110.

120.

190.

130.

130.

140.

120.

100.

210.

130.

110.

110.

830.

170.

150.

14M

nO0.

120.

110.

120.

140.

140.

090.

140.

140.

100.

130.

140.

080.

390.

090.

020.

11L

OI

3.50

4.30

3.50

3.80

4.20

2.20

3.00

3.60

3.00

3.40

3.70

3.00

1.9

5.68

2.07

4.86

Tota

l99

.94

99.8

799

.89

99.9

299

.93

99.7

999

.92

99.9

299

.89

99.9

199

.91

99.9

499

.84

100.

1510

0.55

99.9

4A

SI0.

740.

811.

000.

760.

880.

960.

850.

820.

970.

880.

790.

94–

––

–Tr

ace

elem

ents

(ppm

)S

O-1

8B

a27

6.9

276.

752

5.2

228.

831

9.4

442.

940

1.0

326.

545

9.7

458.

828

6.4

414.

653

9.4

400.

941

3.5

538.

7C

o66

.055

.455

.058

.352

.952

.854

.054

.491

.953

.451

.659

.327

.6–

––

Cs

1.4

1.1

2.7

0.1

1.8

3.2

1.9

2.9

1.1

1.8

1.0

1.9

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–G

a14

.317

.421

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.316

.016

.814

.915

.217

.216

.215

.614

.618

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––

Hf

3.2

3.8

4.5

3.2

3.1

4.7

3.5

2.3

6.1

3.6

2.9

4.5

10.8

––

–N

b5.

98.

710

.66.

16.

08.

66.

15.

511

.67.

25.

38.

021

.710

.59.

49.

3R

b52

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Sr20

9.9

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828

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823

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626

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227

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540

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330

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0.6

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2.9

1.4

1.4

1.9

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1.7

1.9

1.4

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––

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206.

021

8.0

204.

025

6.0

239.

013

3.0

244.

022

6.0

161.

020

6.0

244.

011

7.0

202

207.

319

6.4

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341

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328

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953

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1038

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254.

761

6.5

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r10

0.4

112.

113

7.6

84.1

92.6

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296

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2.9

121.

483

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3.6

281.

913

1.8

115.

711

9.7

Y17

.322

.226

.318

.018

.519

.318

.816

.025

.320

.718

.120

.433

.224

.321

.222

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DS-

7M

o0.

30.

30.

70.

50.

20.

50.

50.

50.

20.

60.

70.

120

.6–

––

Cu

39.7

19.6

7.6

34.2

35.2

17.6

29.3

35.5

15.0

10.9

49.3

5.4

106.

214

.95.

216

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610

.411

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010

.021

.014

.111

.911

.59.

88.

110

.969

.810

.88.

910

.2Z

n39

.056

.071

.053

.057

.049

.044

.055

.066

.051

.053

.041

.040

582

.285

.088

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.113

.77.

020

.912

.58.

110

.222

.77.

414

.521

.97.

155

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43.

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8T

l0.

10.

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1<0

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10.

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O-1

8L

a15

.520

.824

.314

.915

.721

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.214

.121

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.415

.821

.612

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Ce

35.2

48.6

55.2

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36.1

51.9

35.0

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50.5

42.8

34.7

46.6

28.2

22.9

22.6

22.4

Pr

4.1

5.7

6.6

4.1

4.3

5.9

4.1

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5.6

3.42

61.4

55.9

50.4

Nd

17.

22.9

26.2

16.0

17.3

22.5

17.4

15.5

24.1

20.6

18.2

21.1

14.1

29.6

23.4

22.6

Sm3.

44.

35.

13.

43.

34.

13.

52.

94.

93.

53.

43.

73

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–E

u0.

70.

91.

10.

80.

70.

80.

80.

81.

40.

80.

80.

70.

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Gd

3.1

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–T

b0.

50.

70.

80.

50.

60.

60.

60.

50.

80.

60.

60.

60.

53–

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2.8

3.7

4.5

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2.8

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3.0

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3.0

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o0.

60.

70.

90.

60.

60.

70.

70.

60.

80.

70.

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70.

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Er

1.8

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1.9

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m0.

30.

30.

40.

30.

30.

30.

30.

30.

40.

30.

30.

30.

28–

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Yb

1.5

2.1

2.2

1.6

1.6

1.9

1.7

1.5

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1.8

1.5

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30.

30.

40.

20.

20.

30.

30.

20.

40.

30.

30.

30.

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Mg�

59.2

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36.4

958

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53.7

446

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54.3

058

.75

36.6

448

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59.2

247

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––

La N

63.5

285

.25

99.5

961

.07

64.3

488

.93

62.3

057

.79

89.7

579

.51

64.7

588

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––

Eu/

Eu*

0.68

0.62

0.66

0.77

0.68

0.64

0.72

0.80

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0.67

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(La/

Yb)

N7.

186.

737.

506.

146.

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855.

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RE

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† Ext

rusi

vero

cks

(Rob

erts

on&

Pic

kett

,200

0);t

Fe 2

O3

and

Di(

%),

repr

esen

tto

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ron

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eas

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icir

onan

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rmat

ive

diop

side

;LO

I,lo

sson

igni

tion

;ASI

,mol

arA

l 2O3/(

K2O

+N

a 2O

+C

aO);

Mg�

,[M

g#=

mol

ar10

0*M

g/(M

g+

Fe+2

)];R

EE

,rar

eea

rth

elm

ents

;SO

-18

CSC

,SO

-18

and

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7ar

eth

est

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rdre

fere

nce

sam

ple

anal

ysed

atth

eA

CM

EL

abor

ator

ies

inC

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ndit

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cks.



HFSE (Nb, Ta, Zr, Ti, Hf) (Gill 1981; Hawkesworthet al. 1991; Woodhead et al. 1993; Pearce et al. 1999;Castillo et al. 2007). Samples of the Karaburun gra-nodiorite have coherent patterns in ocean ridgegranite (ORG)-normalized multi-element diagramand display selective enrichment in LILE such asRb, Ba, Th and depletion in HFSE Ta, Nb, Zr, Hf,Sm, Y and Yb (Fig. 10a). They also show variableenrichments in K, Rb, Th, and Ce and depletions inTa and Nb, which are similar to those of I-typegranites from subduction zones (cf. Saunders et al.1991). The Karaburun granodiorite appears to betypical of magmas derived from a subduction-modified mantle (cf. Wilson 1989) (Fig. 11a). On thePearce et al. (1984) Rb/Y + Nb (Fig. 11b,c), Harriset al. (1986) Rb–Hf–Ta (Fig. 11d) and Condie (1989)La/Yb vs Th/Yb (Fig. 11e) tectonic discriminationdiagrams, all the samples fall within the volcanic arcgranite field labeled ‘active continental margin’(Pearce et al. 1984). The abundance of incompatibleelements in the granitic magmas is probably asso-ciated with the degree of arc maturity (Brown et al.1984). Samples of the Karaburun granodioriteplot on the primitive island arc/continental arcmargin field in the Rb/Zr vs Nb diagram (Fig. 11f).Chrondrite-normalized REE abundance patternsfor the Karaburun granodiorite are comparableto patterns determined from the PeninsularRanges Batholith (Gromet & Silver 1987) andCoastal Batholith, Peru (Pitcher et al. 1985). TheI-type and calc-alkaline Karaburun granodioritedisplays typical geochemical characteristicsas those seen in arc-related granitic rocks [e.g.

SiO2: 48–75 wt%, (A/CNK = Al2O3/[CaO + K2O +Na2O]molar unit) = 0.74–1.00, Na2O > K2O, negativeEu anomaly] (cf. Pitcher et al. 1985; Gromet &Silver 1987; Wilson 1989).

The mineralogical and geochemical characteris-tics of the Karaburun granodiorite are similar tothose of intrusive rocks exposed along the subduc-tion zones of the Tethyan Belt. A number of grani-toids around the Tethyan Belt are thought to haveformed in an active continental margin [e.g.Göksun-Afsin granitoid (Parlak 2006), Boroujerdgranitoid complex (Khalaji et al. 2007), and Siah-Kuh granitoid stock (Arvin et al. 2007)] (Table 4).

Triassic extrusive rocks, which are andesite anddacite in composition, are enriched in LILE anddepleted in HFSE (Robertson & Pickett 2000),similar to the Karaburun granodiorite (Figs 9a–v,10a–c). Plots of samples from the extrusive rocksappear to overlap with samples of the Karaburungranodiorite in major, trace, spider, and tectonicdiscrimination diagrams, suggesting a commonorigin (Figs 9–11b,c; Table 2). Extrusive rocks inthe Karaburun Peninsula have been suggestedas being associated with a back-arc setting(Robertson & Pickett 2000). However, coevalextrusive and intrusive rocks within the samegeological setting, as outlined above, lead us tosuggest that they developed in the same geody-namic setting, and that the andesitic/daciticrocks might be extrusive equivalents of theKaraburun granodiorite. The andesitic/daciticrocks in the Karaburun Peninsula have presum-ably been extruded over the Palaeozoic mélange(e.g. the Karareis Formation) and then might havebeen overlain by the Triassic back-arc rift succes-sions (e.g. the Gerence Formation).

PETROGENESIS

FRACTIONAL CRYSTALLIZATION ANDASSIMILATION-FRACTIONAL CRYSTALLIZATIONPROCESSES

Major and trace element variation trends indicatethat fractional crystallization and assimilation-fractional crystallization could have occurredduring formation of the Karaburun granodioriticrocks. Samples of the Karaburun granodioritedisplay a typical fractional crystallization trend inplots of La/Yb vs La and Ni vs Th (Fig. 12a,b),suggesting that the effects of fractional crystalli-zation were more important than partial meltingin controlling the compositional variations. TheLa/Yb ratios for the Karaburun granodiorite

Fig. 7 Chemical nomenclature diagram (Debon & Le Fort 1983) forthe Karaburun granodiorite. 1. granite; 2. adamellite; 3. granodiorite; 4.tonalite; 5. quartz syenite; 6. quartz monzonite; 7. quartz monzodiorite; 8.quartz diorite/gabbro; 9. syenite; 10. monzonite; 11. monzodiorite/monzogabbro; 12. diorite/gabbro.



Fig. 8 Geochemical discrimination diagrams for the Karaburun granodiorite. (a) Total alkali-silica diagram, (b) AFM diagram (after Irvine & Baragar1971), (c) Plots of rock samples from the Karaburun granodiorite in the K2O vs SiO2 diagram (Le Maitre et al. 1989), (d) Al2O3/(Na2O + K2O) vsAl2O3/(CaO + Na2O + K2O) diagram (Maniar & Piccoli 1989) for the Karaburun granodiorite samples. (e) Na2O vs K2O discrimination plot for I-S-typegranites. It shows that Karaburun granodiorite have K2O/Na2O ratio around 0.4–1.3 and plot in the field of I-type granites, (f) Frequency distribution of ASI(Aluminium Saturation Index; White & Chappell 1988) values of rock samples from the Karaburun granodiorite. Same symbol as in Fig. 6.



samples, which are almost constant against decrea-sing Mg# values used as a differentiation index,may also be explained by a process of fractionalcrystallization (Fig. 12c; e.g. Panter et al. 1997). Interms of Nb/Zr ratios vs Nb, concentrations aremodeled on the basis of the equation of De Paolo(1981) (Fig. 12d). Samples of the Karaburungranodiorite mainly plot on the fractional crystal-lization (FC) trend, and less on the assimilation-fractional crystallization (AFC) trend with r (ratiobetween assimilation and fractional crystallizationand fractionated material) = 0.2. Lower r valuesimply that the chemical trends observed are moreinfluenced by fractional crystallization processesthan crustal contamination effects.

An increase in Na2O and K2O (Fig. 9d,e), anddecrease in Fe2O3, CaO, MgO, and MnO contentsare compatible with their evolution through frac-tional crystallization processes (Fig. 9c,f–h). Adecrease in Al2O3, CaO, MgO, Fe2O3 (Fig. 9c,f–h),and Sr (Fig. 9l) with increasing silica contents aredirectly associated with plagioclase, amphiboleand pyroxene fractionation during crystallizationof magma. Increases in K2O and Rb (Fig. 9e,k)commonly associated with biotite and K-feldsparpoint to the fact these minerals have undergonelate-stage fractionation processes. The elementsSr and Eu display negative trends with increasing

silica contents. Negative trends in Sr and Eu indi-cate an evolution by fractionation of K-feldsparand plagioclase, either in magma chambers orduring magma ascent (Parlak 2006; Khalaji et al.2007; Kaygusuz et al. in press). This is also sup-ported by a negative correlation between CaO andSiO2 (Fig. 9f).

Major- and trace-element data show that themajor fractionating phases are feldspars (bothK-feldspar and plagioclase), amphibole, biotite,and pyroxene. In order to confirm the presence offractional crystallization processes during evolu-tion of the Karaburun granodiorite, we havemodeled fractionation trends of some trace ele-ments, such as Ba, Rb, Sr and Y using the frac-tional crystallization equation suggested by DePaolo (1981). Partition coefficients are from Elliott(2003). On the Ba/Sr vs Sr diagram, plots ofthe samples show a negative trend (Fig. 12e).K-feldspar and plagioclase fractionations have dis-tinct influences on Ba and Sr contents, and hence,these elements can be used to determine whichphase was more effective during magmatic evolu-tion. Plagioclase fractionation would cause anincrease in Ba and a decrease in Sr in the melt,whereas K-feldspar fractionation leads to adecrease in both elements (Fig. 12e). The regres-sion line for the samples of the Karaburun grano-

Table 3 Comparison of the Karaburun granodiorite with typical I-type granitoids

I-type granitoids (Chappell & White 1974, 2001) Karaburun granodiorite

Field characteristics They occur as a number of large batholites, isolatedplutonic complexes or dykes

Small stocks

Broad spectrum of compositions from felsic to mafic.Tonalites and granodiorites are common, althoughthey show wide ranges of SiO2 content

Tonalite, granodiorite and diorite

They are usually associated with genetically-relatedvolcanic suites

Coeval andesitic rocks

Mineralogic Hornblende is common in the mafic types while biotiteusually occur in felsic types

Tremolite/actinolite � biotite

Magnetite is a major opaque phase. Allanite, sphene,acicular apatite are accessory minerals

Abundant apatite

Relatively high Na2O Na2O is between 1.82 and 2.60Chemical Na2O > 3.2 in felsic rocks while

Na2O > 2.2 in mafic rocks

Mol. Al2O3/(Na2O + K2O + CaO) < 1.1 Mol. Al2O3/(Na2O + K2O + CaO) = 0.74–1.00

CIPW- normative diopside or <% 1 normativecorundum

Normative diopside-<% 1 normativecorundum

Broad spectrum of compositions from felsic to mafic.Regular inter-element variations within plutons

Granodiorite, diorite

Irregular linear or near-linearvariation diagrams

Displays near-linear variations



diorite has a similar trend to that observed inplagioclase fractionation. Alternatively, as shownby major element data, other phases (such asK-feldspar, clinopyroxene, biotite, and amphibole)must also be taken into account, so the best fitfractionation trend on this diagram is equivalentto vector A, represented by the 0.65plg + 0.15K-fld + 0.1cpx + 0.05bio + 0.05amp mineral assem-blage (Fig. 12e). The validity of this calculated

fractionating mineral assemblage is also supportedby a plot of Y/Rb vs Ba/Rb (Fig. 12f). Overall, thesedata clearly show that the Karaburun granodioriteunderwent plagioclase-dominated fractionation.

SOURCE ROCK CONSTRAINTS

Granitic rocks previously described arc settingsare typically granite, granodiorite, monzonite, and

Fig. 9 (a–i) Major elements vs SiO2 plotsand (j–v) Trace elements vs SiO2 plots for theKaraburun granodiorite.



diorite in composition. Whereas felsic membersof the association have high SiO2 (>66 wt%) andlow MgO (1–3 wt%), diorites have low SiO2 (aslow as 54 wt%) and high MgO (5–6 wt%). Althoughsamples of the Karaburun granitoids are grano-dioritic, tonalitic, and dioritic in composition, theirrelatively high MgO contents (1.94–6.33 wt%) arecomparable to granodioritic-dioritic rocks. Experi-

mental studies involving melting of basalts andamphibolites below 10 kbar indicate that garnetis not stable in the residue, and the resultingmelts are tonalitic in composition (Rushmer 1991).On the other hand, dehydration melting ofbasaltic amphibolites and eclogites at pressures of10–32 kbar may produce adakitic melts leavingbehind garnet granulite to eclogite residues (e.g.Rapp & Watson 1995). On a plot of MgO vs SiO2,samples of the Karaburun granodiorite are com-parable with the liquids obtained by experimentalmelting of basaltic protoliths. At a given SiO2

content, samples have MgO concentrations clearlyhigher than the experimental melts (Fig. 13a). TheMgO concentrations of these granitoids are com-parable to those of modern adakites produced bymelting of subducted oceanic crust through inter-actions with the mantle (cf. Defant & Drummond1990; Smithies 2000). However, samples of theKaraburun granodiorite are significantly lowerin Sr (mostly between 142 and 404 ppm), Sr/Y(mostly between 9 and 15) and higher in heavyrare-earth elements than adakites (cf. Defant &Drummond 1993; Martin 1999) (Fig. 13b). Hence,important aspects of their petrology and geochem-istry are clearly different from adakites.

Two models are accepted as capable of explain-ing the petrogenesis of the arc-related magmas(granitoids and volcanic equivalents) based onstudies of typical examples of subduction zones:(i) They are generated from basaltic parentalmagmas that undergo assimilation, fractional crys-tallization, assimilation-fractional crystallizationand storage processes (Grove & Donnelly-Nolan1986; Bacon & Druitt 1988; Hildreth & Moorbath1988; Khalaji et al. 2007). (ii) Mafic magmasprovide heat for the partial melting of continentalcrust (Roberts & Clemens 1993; Tepper et al. 1993;Guffanti et al. 1996). The role of the mantle inessential crustal processes is important for provid-ing stress and heat, as well as for granite genera-tion (Vigneresse 2004). The second model is notlikely to be valid in this instance due to the factthat Karaburun rocks have relatively high MgO(1.94–6.33 wt%), higher Mg# and low-mediumsilica contents (54.01–65.07 wt%). MgO and Mg#values of the Karaburun granodiorite samples aresignificantly higher than typical crustal melts, andhence high-Mg granodiorites/diorites are too basicto be derived from pure crustal melts which tendto show very low MgO and high SiO2 contents.Hence, the Karaburun granodiorite is unlikely tohave been generated by partial melting of conti-nental crust.

Fig. 10 (a) ORG-normalised spider diagrams for the Karaburun gra-nodiorite (Pearce et al. 1984), (b) Chondrite-normalised rare-earthelement spider diagram for the Karaburun granodiorite. The normalizationvalues are from Sun (1982). (c) ORG-normalised spider diagrams for theextrusive rocks (Pearce et al. 1984). Symbols as in Fig. 9.



High-MgO rocks are generally considered tobe a relatively rare component of arc-type magmasuites. Recent studies suggest two contrastinghypotheses for the formation of the high-Mgintrusions and their equivalent extrusive rocks(Bourdon et al. 2002, 2003): (i) High-Mg rocks havebeen genetically linked with the mantle wedgeby partial melting of a peridotitic/basaltic sourcemetasomatized by slab melts and/or hydrous fluids;(ii) high-Mg rocks result from the interaction ofslab melts produced in the downgoing oceanic crustwith the peridotitic/basaltic mantle wedge duringtheir journey to the surface.

The Karaburun granodioritic rocks are charac-terized by relatively high 87Sr/86Sri (0.70919–0.709538) and low 143Nd/144Nd (0.512020–0.512044)(Akal et al. 2007). These data require contamina-tion of mantle-derived magmas by the continentalcrust (Hawkesworth et al. 1982; James 1982;Harmon et al. 1984; Thorpe et al. 1984; Wilson1989) and they could have been generated througha fractional crystallization (FC) and assimilation-fractional crystallization (AFC) process from con-temporaneous mafic magmas. The geological andgeochemical data suggest that the I-type Karabu-run granodiorite originated from partial melting of

the subduction-modified mantle wedge (enrichedmantle) with minor contribution of crustal compo-nents through a process of FC and slight AFC.

DISCUSSION

Two models were proposed for the formation ofthe Palaeozoic and Early Mesozoic units includingthe Karakaya complex and the Karaburun Belt. (i)Rift model: This model assumes that the Karakayacomplex was deposited within a rift basin ofLate Permian age (Sengör & Yılmaz 1981; Sengör1984, 1987; Sengör et al. 1984; Genç & Yılmaz 1995;Göncüoglu et al. 2000). The rift basin closed in theLate Triassic by southward subduction that wasfollowed by the consumption of the PalaeotethysOcean (Genç & Yılmaz 1995). The rift model alsosuggests that a back-arc rifting event in the LateTriassic was responsible for the formation of theKarakaya complex on the northern margin ofthe Tauride-Anatolide Platform (Göncüoglu et al.2000; Sayıt & Göncüoglu in press). In this model,the Karaburun Belt is assumed to represent theTriassic rift succession that is mainly character-ised by Upper Palaeozoic limestone and chert

Fig. 11 Tectonomagmatic discrimination diagrams based on (a) La/Yb vs Th/Yb plot to show between subduction related magmas, (b) Nb vs Y and (c)Rb vs Y + Nb for the granitoid rocks. (b) and (c) are after Pearce et al. (1984). VAG, volcanic arc granite; Syn-COLG, syn-collisional granite; WPG,within-plate granite; ORG, ocean ridge granite, (d) Rb-Hf-Ta triangular diagram (after Harris et al. 1986), (e) La/Yb vs Th/Yb diagram (after Condie 1989),(f) Rb/Zr vs Nb diagram (after Brown et al. 1984) for the granitoid rocks for the Karaburun granodiorite samples. Symbols as in Fig. 9.



Tabl

e4

Com

pari

son

ofso

me

gran

itoi

dsar

ound

the

Teth

yan

belt

Uni

tna

me

Kar

abur

ungr

anod

iori

teB

orou

jerd

,San

anda

j-Si

rjan

Zon

e,W

este

rnIr

an(K

hala

jiet

al.2

007)

Siah

-Kuh

gran

itoi

d,K

erm

anIr

an(A

rvin

etal

.200

7)G

öksu

n-A

fsin

(Kah

ram

anm

aras

,Tur

key)

(Par

lak

2006

)

Geo

logi

cal

sett

ing

Intr

uded

rock

accr

etio

nary

pris

mL

ow-g

rade

met

amor

phic

rock

sA

mph

ibol

ites

and

gree

nsch

ists

ofth

em

etam

orph

icco

mpl

exM

etam

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blocks that slid from the marginal to axial zonesof a rift (Erdogan et al. 1990). (ii) Subduction-accretion model: This model assumes that the Kar-akaya complex was formed by the accretion ofoceanic crust by northward subduction duringthe Late Palaeozoic–Triassic (Pickett & Robertson

1996, 2004; Okay 2000). The subduction-accretionmodel also emphasizes that the units of theKarakaya complex were formed by oceanic crust,oceanic seamounts and narrow continental frag-ments. The Karaburun Belt is the preserved rem-nants of the accretionary complex, developed in

Fig. 12 (a) La/Yb vs La, (b) Ni vs Th (c) La/Yb vs Mg#, and (d) Nb/Zr vs Nb diagrams for the Karaburun granodiorite. AFC and FC trends are alsoindicated on the Nb/Zr vs Nb diagram. For the AFC and FC trajectories, partition coefficients values for Zr and Nb are from Ewart and Griffin (1994). Uppercrust (UC) values are from Taylor and McLennan (1985). Dashed lines on the diagrams are regression lines of the samples. Partial melting and fractionalcrystallization trends are according to Panter et al. (1997), Ding et al. (2003) & Wang et al. (2006), (e) Ba/Sr vs Sr and (f) Y/Rb vs Ba/Rb fractionationalcrystallization models using the equation of De Paolo (1981). Partition coefficients were obtained from Elliott (2003). amp, amphibole; bio, biotite; cpx,clinopyroxene; K-fld, K-feldspar; plg, plagioclase. Symbols as in Fig. 6.



response to steady-state subduction of Palaeo-tethyan oceanic crust beneath an active con-tinental margin (Robertson & Pickett 2000). TheTethys Ocean consisted of at least two litho-spheric plates of Carboniferous-Late Triassic andTriassic-Palaeocene ages respectively (Sengör1987; Stampfli 1996; Okay & Tüysüz 1999). Accord-ing to Okay et al. (1996) and Okay (2000), theIzmir–Ankara–Erzincan Suture represents boththe Palaeotethyan and Neotethyan sutures. Thelatter was opened as a separate ocean duringthe Early Triasssic. The Palaeotethyan units inthe Karaburun Peninsula are characterised bythe Karaburun Mélange, which is dominated bySilurian–Upper Carboniferous exotic blocks ofneritic and pelagic carbonate, black chert and vol-canogenic units. The blocks are set in a shearedmatrix of siliciclastic turbidites. An overlyingLower Triassic succession, which is composed ofinterbedded pelagic carbonates, turbiditic sand-stones, red ribbon radiolarites, pink AmmoniticoRosso, and basic volcanic rocks, is interpreted as arift basin-fill related to opening of the Neotethyanoceanic basin (Robertson & Pickett 2000). Accord-ing to Robertson & Pickett (2000), the mélange isseen here as the end-product of a combinationof Late Palaeozoic southward (?) subduction-accretion (culminating in trench-microcontinentcollision?), Early Triassic rifting and latestCretaceous–Early Tertiary subduction/collision.Regional comparisons suggest that initial mélangeformation took place in Late Carboniferous–EarlyPermian time. The Triassic rift was overlain by a

subsiding passive margin adjacent to a northerlyNeotethyan oceanic basin from Middle Triassic toLate Cretaceous. This ocean was closed in theLate Cretaceous–Early Tertiary, resulting in a col-lapse of the passive margin, subduction-accretionand further mélange formation. Continental colli-sion resulted in further deformation of the Palaeo-zoic mélange, thrust imbrication of the Mesozoicplatform and shearing at its base. However,detailed kinematic data as well as timing of defor-mation and thrusting, and hence direction ofthe subducting slab in the Karaburun Peninsula,remain incomplete. The Karaburun Mélange canbe now regarded as a Palaeozoic mélange, in rela-tion to the subduction of the Palaeotethyan ocean,and can be interpreted as the remnants of thePalaeotethyan fore-arc basin (Eren et al. 2004).During early Triassic times a back-arc rift openedin the Carboniferous fore-arc basin due to rollback of the Palaeotethys slab (Pickett & Robertson1996). The Gerence Formation represents theback-arc rift sequence (Robertson & Pickett 2000).Subduction events, arc magmatism and back-arcrifting began to occur more or less contemporane-ously during the Early Triassic.

A schematic cross-section showing the relation-ship between tectonic setting and production of theKaraburun granodioritic magmas in the activecontinental arc margin (volcanic arc) is illustratedin Fig. 14. Once primary mafic magmas haveformed from partial melting of the subduction-modified mantle wedge, they must subsequentlyrise through a thick section of continental crustal

Fig. 13 (a) MgO vs SiO2 plot comparing experimental melts composition and (b) Sr/Y vs Y (after Martin 1993) diagram for the Karaburun granodioritesamples. Symbols as in Fig. 6.



rocks. Mafic magma with minor crustal con-tribution formed the Karaburun stock and associ-ated extrusive rocks. Crustal contaminationseems inevitable and the subsequent geochemicalevolution of the magmas must be dominated byfractional crystallizaton and minor assimilation-fractional crystallization processes (De Paolo 1981;Wilson 1989). The magmas that erupted to formthe Idecik basalt were associated with the openingof the Neotethyan ocean as a back-arc basin. Thegeological setting of the Karaburun area indicatesthat the I-type granitoids intruded into the accre-tionary prism of an arc setting, similar to that ofthe southward-subducting northern margin ofGondwana (cf. Ustaömer 1999; Yigitbas et al. 2004;Gürsu & Göncüoglu 2005).

CONCLUSIONS

The Karaburun granodiorite has I-type character-istics and belongs to the calc-alkaline series. It wasgenerated by melting of subduction-modifiedmantle wedge source rocks with inevitable crustalinput through a process of fractional crystalliza-tion combined with minor assimilation-fractionalcrystallization. Small negative Eu/Eu* anomaliesand depletion in medium rare earth element(MREE) relative to heavy rare earth element(HREE) indicate that plagioclase was a majorfractionation phase during magma segregation.The major and trace element compositions indi-cate that the Triassic granitic rocks in the Karabu-run Peninsula are subduction-related products(low Zr, Y, Nb, La, and the Nd isotope values).Geological constraints outlined above suggest that

the Karaburun granodiorite formed in a criticaltime interval corresponding to the closure of thePalaeotethys and opening of the Neotethys Oceanduring Triassic. While the granodioritic magmawas emplaced into a deformed accretionary prism(i.e. the Karaburun Mélange), the NeotethysOcean opened as a back-arc rift basin during theTriassic. The back-arc basin-fill in the KaraburunBelt is represented by the Gerence Formation andthe Idecik basalt. The Karaburun granodioriteformed within the continental active margin andextruded andesitic/dacitic lava flows and associ-ated volcaniclastic rocks. Exposures of typicalcontinental-arc granitoids in the Karaburun Beltsupport the validity of the subduction-accretionmodel.

ACKNOWLEDGEMENTS

This paper was supported by the ScientificResearch Projects Unit of Dokuz Eylül University(project no 04.KB.087). The financial support ofthe scientific research project of Akdeniz Univer-sity is also acknowledged. Many thanks go toMartin Palmer for constructive comments thatcontributed to improvement of this paper. Edito-rial handling by Simon Wallis and Yoji Arakawaand reviews by Masaaki Owada are greatly appre-ciated. The authors also thank Robert Martin andPhilip Glover for English editing.

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Fig. 14 A schematic cross-section show-ing relationship between tectonic setting andproduction of mafic to felsic magmas in mag-matic arc and back-arc regions of the Karabu-run Peninsula during the Triassic.



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Geochemistry of I-type granitoids in the Karaburun Peninsula, West Turkey: Evidence for Triassic...

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