Geochemical constraints on petrogenesis of Late Cretaceous alkaline magmatism in east-central Anatolia (Hasancelebi–Basören, Malatya), Turkey

ORIGINAL PAPER

Geochemical constraints on petrogenesis of Late Cretaceousalkaline magmatism in east-central Anatolia(Hasancelebi–Basören, Malatya), Turkey

I. Ozgenc & N. Ilbeyli

Received: 4 December 2007 /Accepted: 1 October 2008 / Published online: 18 October 2008# Springer-Verlag 2008

Abstract Late Cretaceous alkali magmatic rocks occurwidely in the Hasancelebi and Basören regions (Malatya).The Hasancelebi and Basören intrusive rocks are mainlyperalkaline and alkaline-oversaturated. The Hasancelebiintrusive rocks are made up of syenite to quartz monzonite.On the other hand the Basören intrusive rocks mainlycontain feldspathoidal syenites that are cut by feldspathoid-bearing dykes. The Hasancelebi intrusive rocks show com-parable field, petrographic and geochemical characteristicswith A-type rocks. All intrusive rocks show enrichment inLILE and LREE relative to HFSE. The Th/Yb versus Ta/Ybdiagram indicates that all magmatic rocks formed from anenriched mantle source region(s). The parental magma forthe Basören rocks has a higher intraplate component thanthat from the Hasancelebi rocks which could be attributedto mantle source heterogeneity before collision in east-centralAnatolia. Either delamination of the thermal boundary layeror slab-breakoff are likely mechanisms for the initiation ofpost-collisional magmatism in the Hasancelebi–Basörenareas.

Introduction

A-type granites are derived from fractional crystallizationof mantle-derived melts or from partial to complete meltingof continental crust that has been metasomatized by alkali-rich fluids (Martin 2006). In many cases, both crust andmantle are involved (Bonin 2004; Martin 2006), and someexamples are associated with coeval silica-undersaturatedmagmatic suites and carbonatites (Martin 2006).

Alkaline rocks commonly occur in post-orogenic, exten-sional environments (Eby 1992; Turner et al. 1992; Blackand Liégeois 1993; Whalen et al. 1994; Martin 2006). Theserocks provide significant information on post-collisionalmagmatic processes within the continental lithosphere(Turner et al. 1992). Several investigators have argued forthe formation of A-type granites by partial melting of pre-existing crustal rocks (e.g., Collins et al. 1982; Whalen et al.1987; Landenberger and Collins 1996), whereas others haveproposed that these granites are highly fractionated prod-ucts from differentiation of mantle-derived parental maficmagmas (e.g., Stern and Gottfried 1986; Turner et al. 1992;Kessel et al. 1998; Volkert et al. 2000).

The post-collisional intrusive rocks in east-centralAnatolia, Turkey (Hasancelebi, Basören–Malatya), are thetopic of this study. Although these rocks are situated in theEastern Tauride platform, some authors (Boztug 1998,2000) argued that they are located in the Central AnatolianCrystalline Complex (Göncüoglu et al. 1991; Boztug et al.2007) (Fig. 1). Although various geological studies havebeen conducted on the plutonic rocks of east-centralAnatolia (e.g., Yilmaz et al. 1992, 1993; Gürer 1996;Boztug et al. 2007), some problems related to theirevolution remain unsolved. There are not enough current

Miner Petrol (2009) 95:71–85DOI 10.1007/s00710-008-0027-0

Editorial handling: L.G. Gwalani

I. Ozgenc (*)Department of Geology, Faculty of Engineering,Dokuz Eylül University,Tinaztepe Campus,Izmir 35160, Turkeye-mail: [email protected]

N. IlbeyliFaculty of Engineering, Mustafa Kemal University,Hatay 31040, Turkey

data to correlate the characteristics between the intrusiverocks in east-central Anatolia. In this study, the petrogenesisand geological significance of post-collisional A-type rocksfrom the eastern part of central Anatolia are examined. Thisregion probably contains one of the best examples ofalkaline magmatism formed in a post-collisional tectonicsetting (Ilbeyli et al. 2004). Here, new major- and trace-element data are presented for well-characterized samplesfrom the alkaline plutons emplaced at the eastern edge ofcentral Anatolia. These geochemical data are then used tospeculate on the genesis of alkaline intrusive bodies in apost-collisional tectonic setting.

Regional geological setting

Turkey is made up of a number of continental blocksseparated by ophiolitic suture zones (Fig. 1). The Neo-Tethyan ocean within Anatolia was divided into twobranches separated by microcontinents (Sengör and Yilmaz1981). The northern strand of Neo-Tethys consisted of theIzmir–Ankara–Erzincan and the Inner Tauride oceans,whereas the southern branch separated the Tauride–Anatolide platform and Bitlis–Pötürge fragment from themain body of Gondwanaland. The Izmir–Ankara–Erzincanocean began opening between the Sakarya continent to thenorth and the Tauride–Anatolide platform to the southduring the Lias (Görür et al. 1984). This ocean beganclosing at the beginning of the Late Cretaceous along twonorth-dipping subduction zones beneath the Pontides(Sengör and Yilmaz 1981). Ophiolite obduction, subductionand metamorphism took place during the Late Cretaceous,while collisions between the Tauride–Anatolide platformand Pontides were initiated in many places during Paleoceneor Early Eocene times (Okay et al. 2001).

Magmatic activity in central Anatolia began during theLate Cretaceous and created both calc-alkaline and alkalineproducts (Boztug 2000; Boztug et al. 2003, 2007; Köksal etal. 2004; Ilbeyli 2004, 2005; Ilbeyli et al. 2004). The centralAnatolian plutonic rocks are comprised of S-type (Kuscuand Erler 1998), I-type (Erler et al. 1991; Akiman et al.1993; Göncüoglu et al. 1993; Yaliniz et al. 1999) and A-type granites (Lünel and Akiman 1986; Bayhan andTolluoglu 1987; Göncüoglu et al. 1993; Ozkan and Erkan1994; Boztug et al. 1994; Boztug 1998; Otlu and Boztug1998; Köksal et al. 2001).

Geological setting

The Upper Cretaceous Kuluncak ophiolitic mélange con-stitutes the basement of the study area (Fig. 2). It consistsof gabbro, wehrlite and pyroxenite (Stendal et al. 1995).This basement unit is unconformably overlain by theMaastrichtian–Paleocene–Eocene-aged Hekimhan Group.Both the mélange and the basal unit of the group have anupper contact with the Upper Cretaceous Hasancelebivolcanic rocks (Leo et al. 1973, 1974), which contain trachiteand trachyandesitic volcanic rocks. These rocks are cut bythe Paleocene-aged (Izdar and Unlü 1977) Hasancelebipluton, which has a widespread contact metasomatic zone(Boztug and Yilmaz 1992). The Hekimhan Group is overlainby Miocene volcanic rocks, which contain andesite, daciteand rhyolite (Yalcin et al. 1998). All these units are overlainby Pliocene conglomerate-sandstone and limestone.

In the Karakuz and Hasancelebi areas (Fig. 2), the ironores are hosted in the metasomatized and scapolite-richvolcanic/subvolcanic rocks (Ucurum et al. 1996). Kuscu etal. (2005) suggested that the ore mineralization is related tothe surrounding scapolite ± pyroxene ± amphibole ± biotitealteration. Yilmaz et al. (1993) noted that this mineraliza-tion also affected the Hasancelebi pluton. 40Ar/39Ar agedeterminations from biotite veins cutting the ores gaveresults of 73.43±0.41, 74.92±0.39 and 73.12±0.75 Ma(Marschik et al. 2008). They suggested that these agesindicate the minimum age of the ore-hosted volcanic rock,syenite, and scapolitisation of these rocks.

The basement unit for the Basören area is the UpperCretaceous–Lower Paleocene Karapinar limestone andKizilkaya ophiolitic rocks (Fig. 3). These rocks were thrustonto the Karapinar limestone (Yazgan 1984), which wasalso intruded by the Basören pluton. No contact meta-morphism has been observed. A sedimentary sequence ofMiddle to Upper Eocene (Leo et al. 1978) is represented byclastic sedimentary rocks. The Middle–Upper MioceneKepez volcanic sequence contains mainly andesitic lavas,pyroclastic units, and olivine-phyric basalts. K-Ar agedeterminations on two samples of trachite in the Basörenarea gave results of 74.3±1.7 and 71.1±1.6 Ma; one syenite

Fig. 1 Location map and position of Neo-Tethyan sutures in Turkey(taken from Okay 2000). IPS Intra-Pontide Suture, IAES Izmir–Ankara–Erzincan Suture, CACC Central Anatolian Crystalline Com-plex, ITS Intra-Tauride Suture, AS Antalya Suture, BS Bitlis Suture

72 I. Ozgenc, N. Ilbeyli

sample yielded 65.2±1.6 Ma (Leo et al. 1973). The agesfrom the Hasancelebi–Basören areas are broadly similar tothe published ages of the intrusions from the CentralAnatolian Crystalline Complex (e.g., Ilbeyli et al. 2004;Boztug et al. 2007).

Several models have been proposed concerning theorigin of the A-type granites from east-central Anatolia.Leo et al. (1974) suggested that there is an age difference

between the trachite and the syenite in the Basören area.These rocks could not be derived from the same magma.According to Yilmaz et al. (1993), an upper-mantle sourcecould be involved in the genesis of the Hasancelebi pluton.Gürer (1996) argued that the Hasancelebi plutonic andvolcanic rocks are likely related to the same episode ofmagmatism in a similar tectonic setting on the basis of theirgeological and geochemical features.

Fig. 3 Simplified geological map of the Basören region (taken from Ozgenc 1999)

Fig. 2 Simplified geological map of the Hasancelebi region (taken from Yilmaz et al. 1993)

Geochemical constraints on petrogenesis of Late Cretaceous alkaline magmatism 73

Field relations and petrography of the plutons

The field and petrographic characteristics of the represen-tative intrusive rocks from the Hasancelebi and Basörenplutons are summarized in Table 1. The Hasancelebi pluton,defined by Yilmaz et al. (1992), is also known as theYücesafak syenite (Gürer 1996). The plutonic rockscommonly occur as small stocks (Fig. 2). The pluton ismainly syenite, quartz syenite and rarely monzonite-quartzmonzonite (Table 1). The rocks are pinkish, medium-grained to porphyritic. They are cut by aplitic, pegmatiticand mafic dykes. Enclaves are common in the pluton(Table 1).

The Basören plutonic rocks are mainly found assmall stocks (Fig. 3) (Table 1). The pluton consists offeldspathoidal (nepheline ± sodalite) syenite. The rocks arepinkish to grey, medium-grained to porphyritic. They arecut by grey, dark grey-colored feldspathoid-bearing andmafic dykes. The feldspathoid-bearing dykes are fined-grained, locally porphyritic, with leucite phenocrysts andare mainly phonolitic in composition. Their widths varyfrom 5 to 10 cm.

In the Basören region, carbonatite-hosted fluorite depositshave been identified by Ozgenc and Kibici (1994) andOzgenc (1999). According to Ozgenc (1999), carbonatiterepresents the last stage of intrusions that were responsiblefor the fenitization of the syenites and deposition of smallquantities of fluorite and britholite (Fig. 3). Carbonatiteoccurs in several locations throughout Basören (Fig. 3). It

occurs as ring dykes in syenites, where the bulk of the ringstructure is composed of calcium-rich carbonatite. Acces-sory minerals include fluorite, apatite and phlogopite. Theintrusion history of the ring dykes started with theemplacement of the syenites. In addition, no dykes areobserved in the Karapinar limestone and cover units.Fenites are up to 200 m wide. Here aegirine is replacedby hastingsite and alkali feldspar is replaced by albite(Ozgenc 1999).

Analytical methods

The bulk compositions of eighteen samples were analyzedat the Activation Laboratories Ltd. (Canada) by X-rayfluorescence (XRF) using a Phillips 1400 wavelength-dispersive spectrometer with excitation by an Rh X-raytube. These samples also were analyzed by INAA tech-niques at the Activation Laboratories Ltd. (Canada). Majoroxides and minor elements in the samples were determinedusing a lasar ablation inductively coupled mass spectrom-eter (ICP-MS) following LiBO2 fusion and dilute nitric aciddigestion. Loss on ignition (L.O.I) is by weight differenceafter ignition at 1,000°C. REE contents of the samples weremeasured by ICP-MS at the Acme Analytical Laboratories,Canada. In the following sections, new major and traceelement data (Tables 2 and 3) coupled with previouslyreported major and trace element data (without REE) data(Yilmaz et al. 1993) have been combined.

Table 1 Field and petrographic characteristics of the intrusive rocks from the eastern central Anatolia

Pluton Hasancelebi Basören

Rock type Syenite, quartz syenite, monzonite quartz monzonite Feldspathoidal (nepheline, ± sodalite) syeniteFound as Stocks StocksColor Grey to pinkish Grey to pinkishMineral composition Ksp (perthitic) + Pl (albite–oligoclase) + Cpx + Qtz ± Bt Ksp (perthitic) + Pl (albite) + Cpx ± Qtz ± Bt ± NeGrain size Medium-grained to porphyritic with alkali feldspar Medium-grained to porphyritic with alkali feldsparTexture Hypidiomorphic to porphyritic Hypidiomorphic to porphyriticEnclave Igneous enclaves/xenolithsTexture/grain size hypidiomorphic HypidiomorphicMafic phase Cpx ± Bi Cpx ± BiAccessory phases Titanite Titanite

Opaque phases Opaque phasesApatite ApatiteZircon ZirconXenotime FluoriteMonazite

Alteration Muscovite (i.e. sericite), chlorite, carbonate Muscovite (i.e. sericite), Chlorite, cancriniteReferences Yilmaz et al. (1993) Yilmaz et al. (1993)

Gürer (1996) Gürer (1996)This study This study

Ksp alkali feldspar, Pl pagioclase, Cpx clinopyroxene, Qtz quartz, Bt biotite, Ne nepheline


Geochemistry

Despite selection of fresh samples for the XRF/ICP-MSanalyses, variable degrees of carbonate replacement haveaffected the Hasancelebi rocks, as indicated by the highLOI values obtained (up to 2.7 wt.%; Tables 2 and 3). Inaddition both subsolidus alteration (e.g. fenitization) and

fluorite accumulation have affected the Basören rock units(LOI: up to ~5.4 wt.%; Tables 2 and 3).

Based on whole-rock analyses, the Hasancelebi andBasören samples (excluding mafic dykes) cluster in twogroups in a (Na2O + K2O) vs. SiO2 diagram (Le Bas et al.1986; Middlemost 1994) (Fig. 4a). All samples fall withinthe alkaline field on the TAS diagram (Fig. 4a). In addition

Table 2 XRF-major element(wt %), trace element (ppm)and ICP-MS-rare earth ele-ments and also HF, Ta, Pb, Th,U (ppm) analyses of the repre-sentative samples from theHasancelebi–Basören intrusiverocks

sy syenite, mz monzonite, qmzquartz monzonite

Pluton Hasancelebi DAV-33 DAV-18 DAV-35 DAV-31 DAV-29 DAV-41

Sample no. DAV-52

Rock unit Mafic dyke sy sy mz qmz qmz aplite

SiO2 49.99 60.75 61.11 61.85 67.89 70.45 72.13TiO2 1.00 0.34 0.32 0.21 0.48 0.40 0.15Al2O3 17.24 15.78 17.33 15.89 15.29 15.62 12.85Fe2O3 14.07 6.73 4.14 3.44 1.78 1.54 1.25MnO 0.02 0.04 0.02 0.04 0.01 0.02 0.02MgO 3.05 1.08 0.04 0.10 0.06 0.03 0.21CaO 1.37 4.02 0.10 6.32 1.77 0.26 1.79Na2O 1.96 6.88 0.51 7.10 3.71 3.73 1.97K2O 8.38 1.92 12.92 2.30 7.29 7.18 7.10P2O5 0.54 0.02 0.14 0.02 0.11 0.08 0.04L.O.I 1.90 2.00 2.70 2.50 1.40 0.50 2.30Total 99.52 99.56 99.33 99.77 99.79 99.81 99.81Sc 13 2 1 1 3 2 4V 157 47 15 33 25 12 7Ni 43 34 5 9 9 7 10Co 35 51 32 42 48 69 46Cu 22 2 5 26 6 11 5Zn 18 21 3 1 1 1 5Ga 21 26 15 37 26 26 17Rb 329 10 280 1 96 104 106Sr 378 158 188 158 102 88 70Y 26 42 23 51 56 51 32Zr 183 718 343 775 767 750 188Nb 17 83 43 132 102 116 39Ba 3,651 181 4,046 61 999 912 653La 31.90 20.90 33.20 12.90 29.90 31.70 17.40Ce 70.80 61.80 58.40 41.60 82.50 95.10 49.60Pr 9.21 8.32 6.19 6.00 11.22 11.50 7.09Nd 38.10 33.40 20.20 25.40 43.80 44.90 29.30Sm 7.60 6.70 3.50 6.70 8.70 8.70 5.90Eu 1.42 0.68 0.59 0.59 1.07 0.91 0.57Gd 6.03 5.63 2.69 6.49 7.55 7.62 5.13Tb 0.92 1.13 0.57 1.48 1.53 1.44 0.94Dy 4.96 6.78 3.47 9.13 9.18 9.24 5.40Ho 0.81 1.33 0.69 1.80 1.80 1.74 0.97Er 2.46 4.53 2.53 5.63 6.26 6.16 3.23Tm 0.35 0.79 0.41 0.97 0.98 0.98 0.48Yb 2.09 5.45 2.73 6.34 6.32 6.23 2.82Lu 0.30 0.93 0.40 1.01 0.89 1.03 0.41Hf 5.30 19.00 8.80 26.10 19.30 21.10 6.40Ta 1.20 6.70 2.70 12.60 6.10 7.10 3.10Pb 1.30 2.10 0.70 5.80 0.80 0.80 0.70Th 21.70 60.90 37.60 120.40 55.40 66.90 27.10U 7.10 9.80 18.40 19.90 11.80 13.00 5.50


the Basören rocks are more strongly alkaline and less silica-saturated than the Hasancelebi rocks (Fig. 4a). Thus theBasören samples plot in the undersaturated field (Miyashiro1978) (Fig. 4a). The Hasancelebi and Basören samples fall

in the shoshonitic field on a K2O vs. SiO2 diagram (LeMaitre et al. 1989) (not shown). Most of the Hasancelebisamples have higher K2O than Na2O contents, whereasmost of the Basören samples have higher Na2O than K2O

Table 3 XRF-major element (wt %), trace element (ppm) and ICP-MS-rare earth elements and also HF, Ta, Pb, Th, U (ppm) analyses of therepresentative samples from the Hasancelebi–Basören intrusive rocks

Pluton Basören BA-31 BA-16 BA-26 BA-2 BA-17 BA-10 BA-21

Sample no. BA-4

Rock unit Mafic dyke sy feldspathoid-bearingdyke

feldspathoid-bearingdyke

sy sy Sy sy

SiO2 52.95 54.40 55.56 55.57 55.66 55.88 55.89 55.94TiO2 0.12 0.05 0.07 0.35 0.09 0.09 0.08 0.07Al2O3 20.70 21.12 20.69 8.96 21.06 20.91 20.95 18.88Fe2O3 4.00 3.86 4.42 19.57 3.80 3.58 4.02 8.20MnO 0.18 0.04 0.03 0.15 0.15 0.12 0.13 0.07MgO 0.79 0.07 0.02 0.04 0.31 0.01 0.15 0.12CaO 4.33 2.22 1.87 1.5 2.03 1.53 1.55 1.03Na2O 7.00 6.87 10.44 9.69 7.41 9.52 8.33 10.12K2O 5.57 5.97 5.24 3.39 6.13 6.16 6.17 4.36P2O5 0.01 0.01 0.01 0.02 0.01 0.02 0.01 0.01L.O.I 4.20 5.40 1.50 0.7 3.30 2.00 2.70 1.20TOTAL 99.85 100.01 99.85 99.94 99.95 99.82 99.98 100.00Sc <1 <1 <1 <1 <1 <1 <1 <1V <5 <5 <5 <5 <5 <5 <5 <5Ni <0.1 <0.1 0 0.3 0 0 0 1Co 32 25 50 12.8 26 29 34 38Cu 1 1 1 0.6 1 1 1 1Zn 119 28 20 15 91 104 88 31Ga 38 43 37 31.1 34 34 31 46Rb 228 432 352 242.1 274 255 285 249Sr 335 165 157 32 197 96 174 53Y 50 3 4 3.2 29 42 7 8Zr 595 117 87 587 369 276 179 165Nb 169 13 3 11 87 86 38 24Ba 21 37 313 28.3 32 23 33 37La 100.40 7.20 5.20 5.5 57.70 94.50 27.70 13.80Ce 185.10 11.20 8.60 11.9 96.30 187.20 46.20 21.80Pr 17.35 0.98 1.04 1.07 8.61 17.78 4.18 2.04Nd 50.50 2.90 3.50 3.6 25.20 52.10 12.20 5.70Sm 7.70 0.40 0.50 0.6 3.90 7.60 1.60 0.80Eu 1.22 0.08 0.08 0.1 0.70 1.32 0.33 0.13Gd 5.96 0.36 0.40 0.41 2.99 5.99 1.06 0.65Tb 1.22 0.05 0.05 0.06 0.61 1.18 0.18 0.14Dy 7.41 0.45 0.24 0.54 4.03 6.62 1.09 0.98Ho 1.50 0.07 0.07 0.1 0.84 1.24 0.20 0.17Er 5.31 0.24 0.16 0.49 3.06 3.80 0.77 0.65Tm 0.76 <0.05 <0.05 0.12 0.55 0.54 0.15 0.11Yb 4.51 0.36 0.20 1.2 3.47 2.55 1.09 0.77Lu 0.53 0.06 0.03 0.22 0.45 0.29 0.17 0.12Hf 7.40 2.00 1.40 11 5.10 3.60 2.60 2.90Ta 8.30 0.60 0.20 0.6 4.20 4.70 1.70 1.30Pb 17.50 7.70 1.60 6.9 29.60 38.20 17.50 6.90Th 76.80 4.50 0.90 7 36.70 39.80 14.70 7.10U 23.00 2.40 0.50 1.9 11.80 16.10 7.90 4.50


contents (Tables 2 and 3). The Hasancelebi plutonic rockscover the compositional range from monzonite throughquartz monzonite to granite (Fig. 4a). On the other hand,the Basören intrusive rocks fall within the feldspathoidalmonzosyenite and feldspathoidal syenite fields (Middlemost1994) (Fig. 4a). The Hasancelebi and Basören intrusiverocks have a predominantly peralkaline (A<NK) character(Fig. 4b).

The distinction between the Hasancelebi and Basörenintrusive rocks is also evident in most of the variationdiagrams (Figs. 5 and 6). The Hasancelebi plutonic rocksshow a range in SiO2 values from 61 to 72 wt.%, whereasthe Basören samples display a narrow range in SiO2 values,from 54 to 56 wt% (Tables 2 and 3). In the Hasancelebi andBasören plutons Al2O3, Fe2O3, CaO, Na2O (Fig. 5), andP2O5 (not shown) decrease with increasing SiO2. On theother hand, TiO2 and MgO do not show any clear trends

with increasing silica. The Basören rocks tend to have thehighest contents of Al2O3 and Na2O and the lowestcontents of TiO2 and P2O5 (not shown) for a given silicavalue. The concentrations of selected trace elements areplotted against silica in Fig. 6. Rubidium decreases for theHasancelebi samples up to ~62 wt.% SiO2 and then slightlyincreases (Fig. 6). In addition Nb has a positive correlationwith increasing silica in the Hasancelebi samples. However,Sr and Ba have a negative correlation with silica in theHasancelebi rocks. The Basören samples generally have thehighest contents of Rb for a given silica value; but theyhave the lowest Ba value (Fig. 6). The low Ba content maybe due to the fractionation of alkali feldspar.

Chondrite-normalized REE patterns for selected samplesfrom the Hasancelebi and Basören intrusive rocks areshown in Fig. 7. The Hasancelebi rocks are all very similar.They are all LREE-enriched (LaN/YbN=1.37–8.20), with

Fig. 4 a Classification ofplutonic rocks (Middlemost1994) using the total alkali-silicadiagram. Line (I) separates thealkaline and subalkaline fieldof Miyashiro (1978) andline (II) separates thealkaline oversaturated andundersaturated series from theKerguelen Archipelago (Giretand Lameyre 1980). b Aluminasaturation diagram of intrusiverocks taken from Shand (1951)


small to moderate negative Eu (Eu/Eu*=0.27–0.59)anomalies (Fig. 7a). The Basören intrusive rocks areLREE-enriched (LaN/YbN=3.09–24.98) with moderatenegative Eu (Eu/Eu*=0.55–0.78) anomalies (Fig. 7b). TheBasören pluton samples have less negative Eu anomaliesthan those from the Hasancelebi pluton. The presence ofnegative Eu anomalies indicates that feldspar and/orplagioclase were fractionating phases.

In the primitive mantle-normalized trace element dia-grams, the Hasancelebi intrusive suite (Fig. 8a) is charac-terized by enrichment in LILE (i.e. Rb, Ba, Th, U and K)relative to LREE (i.e. La, Ce, Nd and Sm) and HFSE (i.e.

Ta, Nb, and Ti). The Basören intrusive suite is also enrichedin LREE compared to the HFSE (Fig. 8b). Although theHasancelebi and Basören samples show similar patterns(Fig. 8), the former samples are less depleted in Ba, Sr, Pand Ti compared to the latter samples. The troughs at Sr, P,and Ti could be related to residual plagioclase, apatite, andFe–Ti oxides or the earlier removal of Fe–Ti phases.

Samples from the Hasancelebi pluton (samples >5%modal quartz) are plotted on the tectonic discriminationdiagrams of Pearce et al. (1984) (Fig. 9). The Basörensamples are not plotted in the diagrams (Fig. 9) since theyhave <5% modal quartz. In the Nb vs. Y and Rb vs. (Y+Nb)

Fig. 5 Selected major-elementvariation diagrams (a–f) for theHasancelebi–Basören magmaticrocks


diagrams (Fig. 9), all the Hasancelebi samples fall in theWPG (Within-Plate Granite) field, which is consistent withthe alkaline character of the intrusion. The most silicicsamples from the Hasancelebi pluton conform to thedefinition of A-type granites (e.g., high Na2O + K2O, Nb,Zr, low CaO, and peralkaline; A<NK) (Whalen et al. 1987;Eby 1990).

Discussion

The Hasancelebi and Basören intrusive rocks from east-central Anatolia show LILE enrichment and HFSE deple-tion in the normalized diagrams (Figs. 7 and 8). Thesegeochemical features could indicate (1) interaction betweencrust and mafic magmas through fractional crystallizationcoupled with crustal contamination (AFC) (e.g. Hildrethand Moorbath 1988) and (2) enrichment of the mantle-derived magmas by recycling of crustal material (sourceenrichment) (e.g., Sun and McDonough 1989; Pearce et al.1990; Platt and England 1993; Turner et al. 1996).

Some authors (Pearce 1983; Pearce et al. 1984; Harriset al. 1986) have used trace elements to identify sourceregions and determine the tectonic setting of igneous rocks.In order to assess source regions and magmatic processes

(e.g., source enrichment, AFC) in the derivation of theHasancelebi–Basören magmatic rocks, the Th/Yb ratio isplotted against the Ta/Yb ratio (Fig. 10). The latter ratio canbe used to differentiate between mantle sources. The formerratio can be used to monitor the transfer of slab-derivedfluids via subducted sediments to the mantle wedge (Pearce1983). In Fig. 10, a greywacke sample from the centralAnatolian crust is also plotted as the crustal contaminant(Ilbeyli et al. 2004).

As can be seen in Fig. 10, the Ta/Yb and Th/Yb ratiosfor the Hasancelebi–Basören rocks are higher than the crustcomposition from central Anatolia. In Fig. 10, most of theHasancelebi–Basören rocks form trends that run almostparallel to the mantle metasomatism array, but the Basörensamples are displaced mainly towards higher Ta/Yb ratios.The high Ta/Yb values of these rocks could be explained byderivation from a more enriched-mantle source than that ofthe Hasancelebi alkaline rocks. As can be seen in Fig. 10,the intrusive rocks do not form trends from the mantle arrayto the crust. Therefore AFC is not the only process for thegeneration of plutonic rocks. The variations shown by theHasancelebi rocks might indicate that the parental magmafor these rocks have experienced assimilation and fractionalcrystallization during ascent through continental crust. Incontrast, the parental magma for the Basören alkaline rocks

Fig. 6 Selected trace-elementvariation diagrams (a-d) for theHasancelebi–Basören magmaticrocks


might be derived from a more enriched-mantle source withless coupled crustal assimilation-fractionation compared tothat for the Hasancelebi alkaline rocks.

Immobile elements (e.g., Nb, Ta, Zr, Hf) in igneousrocks also are used as powerful tools for understandingpetrogenetic processes (e.g., Pearce 1983; Green 1995). Inorder to further consider those processes in the derivation ofthe Hasancelebi–Basören intrusive rocks, the Nb/Ta ratio isplotted against the Zr/Hf ratio (Fig. 11). Typical mantleratios (Nb/Ta=17.5 and Zr/Hf=44; Green 1995) are alsoshown in Fig. 11. As can be seen from Fig. 11, allHasancelebi samples have sub-chondritic (or mantle) ratioscompared to the Basören samples. Most Basören samplesplot near the chondritic (or mantle) ratios with scatter

towards higher ratios indicating more enriched-mantlesource for the Hasancelebi samples (Fig. 11).

Green (1995) suggested that in alkaline rocks Nb/Taratios generally fall into two groups: (1) consistent Nb/Taratios close to chondritic or mantle values; and (2) variableNb/Ta ratios that notably exceed mantle values. In Fig. 11,the Basören samples belong to the former group. Note thatin Fig. 11, the Hasancelebi–Basören samples plot indifferent locations suggesting different sources and mag-matic histories for these rock types. In general, the Basörensamples are more depleted in Ta and Nb than theHasancelebi rocks (Fig. 8). Alkaline rocks generated fromenriched lithospheric mantle can be depleted in HFSE (e.g.,Litvinovsky et al. 2002; Zhang et al. 2005). This depletion

Fig. 7 Chondrite-normalizedREE patterns (a, b) for theHasancelebi–Basören magmaticrocks. Normalization factors aretaken from Boynton (1984)


in HFSE characterizes all rock types from east-centralAnatolia (Fig. 8). The greater depletion in Ta and Nb seenin the Basören rocks is most likely inherited from theirsource region.

The overall trends seen for major and trace elements(Figs. 4, 5 and 6), REE (Fig. 7), primitive mantle-normalized multi-element plots (Fig. 8) and ratio-ratiodiagrams (Figs. 10 and 11) suggest that the Hasancelebi–Basören suites could not be derived from the same parentalmagma. This could be related to mantle source heteroge-neity before collision in east-central Anatolia. A similarmechanism was also suggested for the origin of the west-central Anatolian plutonic rocks (Ilbeyli et al. 2004; Ilbeyli

2005). Further investigation involving the determination ofisotopic ratios will be done to justify the proposed origin ofthe alkaline suites in east-central Anatolia.

Tectonic implications

In the Hasancelebi and Basören plutons felsic rocks makeup the dominant lithologies (Tables 1, 2 and 3). The onlyexposed mafic rocks are occasional mafic dykes cross-cutting these plutons. Moreover, all rock types have highK2O and Rb contents and low contents of MgO and Ni(Tables 2 and 3), indicating that no samples representprimitive mantle liquid compositions. This may also indi-

Fig. 8 Primitive-mantle-normalized diagrams(a, b) illustrating thegeochemical characteristics ofthe Hasancelebi–Basörenmagmatic rocks. Normalizationfactors are taken from Sun andMcDonough (1989)


cate that the parental melts for all rock types have under-gone significant crystal fractionation prior to emplacementinto the central Anatolian crust.

Field relationships, petrological, and geochemical dataindicate that the intrusive rocks from the Hasancelebi–Basören plutons were derived from the partial melting of ametasomatized lithospheric mantle source. All samples alsohave low Ti (Tables 2 and 3), suggesting that extension didnot approach the within-plate rifting stage in east-centralAnatolia. However high concentrations of Nb, Zr, and Y inthe alkaline rocks and the presence of carbonatites areconsistent with magmatism caused by extension. Therefore,we propose that the Hasancelebi–Basören plutons weregenerated in a post-collisional extension environment.

Many collisional events are closely followed by anextensional episode, caused either by the collapse oflithosphere overthickened during compression, or the ‘pull-ing apart’ of the lithosphere during subsequent plate re-organisation and roll-back (e.g., Houseman et al. 1981;England and Thompson 1986). In the case of the

Hasancelebi–Basören rocks, the likely mechanisms formagma generation are either lithospheric extension anduplift or the melting of the mantle lithosphere due to theperturbation of the geotherm from the delamination of thethermal boundary layer or slab detachment. Perturbation ofmetasomatized lithosphere by either delamination of thethermal boundary layer or slab breakoff may have gener-ated the primary magmas for these rock types. Bothprocesses would lead to conductive heating of enrichedmantle. This may have assisted or initiated the orogeniccollapse that followed collision and uplift. A similar mecha-nism was also suggested for the origin of the west-centralAnatolian intrusive rocks (e.g., Ilbeyli et al. 2004; Ilbeyli2005).

Fig. 11 Plot of Zr/Hf ratio versus Nb/Ta ratio for the Hasancelebi–Basören intrusive rocks. Crust composition from central Anatolia(Ilbeyli et al. 2004)

Fig. 10 Th/Yb versus Ta/Yb diagram (after Pearce 1983) for basicand intermediate intrusive rocks (samples <63% SiO2 are plotted)from the Hasancelebi–Basören magmatic rocks. sz subduction zoneenrichment, within-plate enrichment. Crust composition from centralAnatolia (Ilbeyli et al. 2004)

Fig. 9 a Nb versus Y; and b Rb versus (Y + Nb) discriminationdiagrams for the Hasancelebi plutonic rocks (samples >5% modalquartz are plotted; after Pearce et al. 1984)


Metallogenic implications

The presence of magmatic fluorite suggests that theintrusive rocks are highly differentiated and formed duringa late- to post-orogenic magmatic cycle (Bregar et al. 2002).De Boorder et al. (1998) also suggested that mineralizationin collision-related setting generally occurs late in thecollisional event and is related to late-orogenic extensionprocesses.

Slab breakoff may also explain the Middle-UpperPaleocene mineralization (e.g. fluorite) in the Basörenregion (Fig. 3). A similar mechanism was also suggestedfor mineralization in the western Mediterranean (DeBoorder et al. 1998; Blundell et al. 2005). The mineraliza-tion in Malatya could be related to an extensional settingfollowing collision, reflecting an increase in heat and fluidflows, in response to detachment of a lithospheric slab.

Conclusions

The Hasancelebi and Basören rocks are alkaline incharacter. All intrusive rocks show enrichment in LILEand LREE relative to HFSE. The Hasancelebi intrusiverocks show petrographic and geochemical characteristicssimilar to A-type granites. The parental magmas for theHasancelebi and Basören plutons were generated frommantle sources, which were modified by a subductioncomponent before collision. Both parental magmas alsohave experienced crustal assimilation coupled with frac-tional crystallization during ascent through the centralAnatolian crust. The parental magma for the Basören rockshas a higher intra-plate component than that from theHasancelebi rocks. In the east-central Anatolian regionpartial melting occurred in a post-collisional setting relatedto lithospheric removal and crustal extension induced byconvective instability of a thickened mantle boundary layeror slab breakoff.

Acknowledgements This work is part of a research projectsupported by TUBITAK (YDABAG 105 Y 076). We thank Prof. Dr.Ahmet SASMAZ and also Ulkü KARAKURT, Mehmet AKBULUTfor their help during the fieldwork. We specially thank to Prof. Dr.Donna L. WHITNEY for improving English in the manuscript.Constructive reviews by Drs. Andy BEARD, Prelevic DEJAN, JoseAffonso BROD and Moacir J. B. MACAMBIRA are acknowledged.We also thank Prof. Dr. L.G. Gwalani for editorial handling.

References

Akiman O, Erler A, Göncüoglu MC, Gülec N, Geven A, Türeli K,Kadioglu YK (1993) Geochemical characteristics of granitoidsalong the western margin of the Central Anatolian CrystallineComplex and their tectonic implications. Geol J 28:371–382

Bayhan H, Tolluoglu AU (1987) The mineralogical–petrographicaland geochemical characteristics of the Cayagazi syenitoid(northwest of Kirsehir province). H.U Yerbilimleri 14:109–120(in Turkish with English abstract)

Black R, Liégeois JP (1993) Cratons, mobile belts, alkaline rocks andcontinental lithospheric mantle: the Pan-African testimony. JGeol Soc London 150:89–98

Blundell D, Arndt N, Cobblod PR, Heinrich C (2005) Processes oftectonism, magmatism and mineralization: lessons from Europe.Ore Geol Rev 27:333–349

Bonin B (2004) Do coeval mafic and felsic magmas in post-collisionalto within-plate regimes necessarily imply two contrasting, mantleand crustal, sources? A review. Lithos 78:1–24

Boynton WV (1984) Geochemistry of the rare earth elements:meteorite studies. In: Henderson P (ed) Rare earth elementgeochemistry. Elsevier, Amsterdam, pp 63–114

Boztug D (1998) Post-collisional central Anatolian alkaline plutonism,Turkey. Turk J Earth Sci 7:145–165

Boztug D (2000) S-I-A- type intrusive associations: geodynamicsignificance of synchronism between metamorphism and mag-matism in central Anatolia, Turkey. In: Bozkurt E, WinchesterJA, Piper JDA (eds) Tectonics and magmatism in Turkey and thesurrounding area. Geol Soc Spec Publ 173:407–424

Boztug D, Yilmaz S (1992) Petrology of Konukdere metasomatites(Hekimhan–Hasancelebi, NW Malatya). Geol Bull Turk 7:116–129

Boztug D, Yilmaz S, Kesgin Y (1994) Petrography, petrochemistryand petrogenesis of the eastern part of Kösedag pluton from theCentral-Eastern Anatolian alkaline province, Susehri, NE Sivas.Geol Bull Turk 32/2:1–12 (in Turkish with English abstract)

Boztug D, Kuscu I, Ercin AI, Avci N (2003) Mineral depositsassociated with the pre-, syn- and post-collisional granitoids ofthe Neo-Tethyan convergence system between the Eurasian andAnatolian plates in NE and Central Turkey. In: Eliopoulos D (ed)Mineral exploration and sustainable development. Mill Press,Rotterdam, pp 1141–1144

Boztug D, Harlavan Y, Arehart GB, Satir M, Avci N (2007) K-Ar age,whole-rock and isotope geochemistry of A-type granitoids in theDivrigi-Sivas region, eastern-central Anatolia, Turkey. Lithos97:193–218

Bregar M, Bauernhofer A, Pelz K, Kloetzli U, Fritz H, Neumayer P(2002) A late Neoproterozoic magmatic core complex in theEastern Desert of Egypt; emplacement of granitoids in a wrench-tectonic setting. Precam Res 118:59–82

Collins WJ, Beams SD, White AJR, Chappell BW (1982) Nature andorigin of A-type granites with particular reference to southeasternAustralia. Contrib Mineral Petrol 80:189–200

De Boorder H, Spakman W, White SH, Wortel MJR (1998) Latecenozoic mineralization, orogenic collapse and slab detachmentin the European Alpine Belt. Earth Planet Sci Lett 164:569–575

Eby GN (1990) The A-type granitoids: a review of their occurrenceand chemical characteristics and speculations on their petrogenesis.Lithos 26:115–134

Eby GN (1992) Chemical subdivision of the A-type granitoids:petrogenetic and tectonic implications. Geology 20:641–644

England PC, Thompson A (1986) Some thermal and tectonic modelsfor the crustal melting in continental collision zones. In: CowardMP, Ries AC (eds) Collision tectonics. Geol Soc Spec Publ19:83–94

Erler A, Akiman O, Unan C, Dalkilic B, Geven A, Onen P (1991) Thepetrology and geochemisty of the Kirsehir massif magmaticrocks in Kaman (Kirsehir) and Yozgat regions. Doga-Turk J EngEnviron Sci 15:76–100

Giret A, Lameyre J (1980) Mise en place et evolution magmatique descomplexes plutoniques de la caldera de Courbet, ile Kerguelen.Bull Geol Soc (France) 7-XXII-3:437–446


Göncüoglu MC, Toprak V, Kuscu I, Erler A, Olgun E (1991) Geologyof the western part of the Central Anatolian Massif. Part I:Southern Section. Türkiye Petrolleri Anonim Ortakligi (TPAO)Report No: 2909 (in Turkish)

Göncüoglu MC, Erler A, Toprak V, Olgun E, Yaliniz KM, Kuscu I,Köksal S, Dirik K (1993) Geology of the central part of theCentral Anatolian Massif. Part III: geological evolution of theTertiary Basin of the central Kızılırmak. Türkiye PetrolleriAnonim Ortakligi (TPAO) Report No: 3313 (in Turkish)

Görür N, Oktay FY, Seymen I, Sengör AMC (1984) Paleotectonicevolution of the Tuzgölü basin complex, central Anatolia(Turkey): sedimentary record of a Neo-Tethyan closure. In:Dixon JE, Robertson AHF (eds) The geological evolution of theEastern Mediterranean. Geol Soc Spec Publ 17:467–482

Green TH (1995) Significance of Nb/Ta as an indicator of geochemicalprocesses in the crust-mantle system. Chem Geol 120:347–359

Gürer OF (1996) Geological position and the genesis of Hasancelebialkaline magmatism at the Eastern Taurides (NW Malatya). TurkJ Earth Sci 5:71–88 (in Turkish with English abstract)

Harris NBW, Pearce JA, Tindle AG (1986) Geochemical charac-teristics of collision-zone magmatism. In: Coward MP, Ries AC(eds) Collision tectonics. Geol Soc London Spec Publ 19:67–81

Hildreth W, Moorbath S (1988) Crustal contribution to arc magmatismin the Andes of southern Chile. Contrib Mineral Petrol 98:455–489

Houseman GA, McKenzie DP, Molnar P (1981) Convective instabilityof a thickened boundary layer and its relevance for the thermalevolution of continental convergent belts. J Geophys Res86:6115–6132

Ilbeyli N (2004) Field, Petrographic and geochemical characteristicsof the Hamit alkaline intrusion in the Central AnatolianCrystalline Complex, Turkey. Turk J Earth Sci 12:1–27

Ilbeyli N (2005) Mineralogical-geochemical constraints on intrusivesin central Anatolia, Turkey: tectono-magmatic evolution andcharacteristics of mantle source. Geol Mag 142:187–207

Ilbeyli N, Pearce JA, Thirlwall MF, Mitchell JG (2004) Petrogenesisof collision-related plutonics in central Anatolia, Turkey. Lithos72:163–182

Izdar E, Unlü T (1977) Geology of Hekimhan–Hasancelebi–Kuluncakregion. In: Fourth Conference on the Geology of the AegeanRegion. Dokuz Eylül University, Izmir, pp 303–329

Kessel R, Stein M, Navon O (1998) Petrogenesis of late Neoproterozoicdikes in the northern Arabian-Nubian Shield; implications for theorigin of A-type granites. Precam Res 92:195–213

Köksal S, Göncüoglu MC, Floyd PA (2001) Extrusive members ofpost collisional A-type magmatism in central Anatolia: Karahidirvolcanics, Idis Dagi-Avanos area, Turkey. Int Geol Rev 43:683–694

Köksal S, Romer RL, Göncüoglu MC, Toksoy-Köksal F (2004)Timing of post-collisional H-type to A-type granitic magmatism:U-Pb titanite ages from the Alpine central Anatolian granitoids(Turkey). Int J Earth Sci 93:974–989

Kuscu I, Erler A (1998) Mineralization events in a collision-relatedsetting: the Central Anatolian Crystalline Complex, Turkey. IntGeol Rev 40:552–566

Kuscu I, Yilmazer E, Demirela G, Gökce H, Gülec N (2005)Alteration zoning of iron oxide deposits in the Hasancelebi andKarakuz (Malatya) regions. In: 58th Turkish Geological Sympo-sium, Ankara, pp 66–67 (in Turkish with English abstract)

Landenberger B, Collins WJ (1996) Derivation of A-type granitesfrom a dehydrated charnockitic lower crust: evidence from theChaelundi complex, Eastern Australia. J Petrol 37:145–170

Le Bas MJ, Le Maitre RW, Streckeisen A, Zanettin BA (1986)Chemical classification of volcanic rocks based on the totalalkali-silica diagram. J Petrol 27:745–750

Le Maitre RW, Bateman P, Dudek A, Keller J, Lameyre J, Le Bas MJ,Sabine PA, Schmid R, Sorensen H, Streckeisen A, Woolley AR,Zanettin B (1989) A classification of igneous rocks and glossaryof terms: recommendations of the International Union ofGeological Sciences Subcommission on the Systematics ofIgneous Rocks. Blackwell Scientific, Oxford, UK

Leo GW, Marvin RF, Mehnert HH (1973) Potassium-argon ages ofigneous rocks in the Kuluncak-Sofular area, Malatya province,central Turkey. Internal Miner Res Explor Inst Turk Report, p 16

Leo GW, Marvin RF, Mehnert HH (1974) Geological framework ofKuluncak–Sofular area, east-central Turkey, and K-Ar ages ofigneous rocks. Geol Soc Am Bull 85:1785–1788

Leo GW, Onder E, Kilic M, Avci M (1978) Geology and mineralresources of Kuluncak-Sofular area (Malatya K39-al, K39-a2quadrangles), Turkey. USA Geol Surv Bull No:1429

LitvinovskyBA, JahnBM, ZanvilevichAN, ShadaevMG (2002) Crystalfractionation in the petrogenesis of an alkali monzodiorite-syenite-series: the Oshurkovo plutonic sheeted complex, Transbaikalia,Russia. Lithos 64:97–130

Lünel AT, Akiman O (1986) Pseudoleucite from Hamitköy area,Kaman, Kirsehir occurrence and its use as a pressure indicator.Bull Miner Res Explor Inst Turk 103/104:117–123

Marschik R, Spikings R, Kuscu I (2008) Geochronology and stableisotope signature of alteration related to hydrothermal magnetiteores in Central Anatolia, Turkey. Mineral Depo 43:111–124

Martin RF (2006) A-type granites of crustal origin ultimately resultfrom open-system fenitization-type reactions in an extensionalenvironment. Lithos 91:125–136

Middlemost EAK (1994) Naming materials in the magma/igneousrock system. Earth-Sci Rev 37:215–224

Miyashiro A (1978) Nature of alkalic volcanic rock series. ContribMineral Petrol 66:91–104

Okay A (2000) Was the Late Triassic orogeny in Turkey caused by thecollision of an oceanic plateau? In: Bozkurt E, Winchester JA,Piper JDA (eds) Tectonics and magmatism in Turkey and thesurrounding area. Geol Soc Spec Publ 173:25–41

Okay AI, Tansel I, Tüysüz O (2001) Obduction, subduction andcollision as reflected in the Upper Cretaceous-Lower Eocenesedimentary record of western Turkey. Geol Mag 138:117–142

Otlu N, Boztug D (1998) The coexistence of the silica oversaturated(ALKOS) and undersaturated alkaline (ALKUS) rocks in theKortundag and Baranadag plutons from the central Anatolianalkaline plutonism, E Kaman/NW Kirsehir, Turkey. Turk J EarthSci 7:241–257 (in Turkish with English abstract)

Ozgenc I (1999) Carbonatite-hosted fluorite and britholite mineraliza-tion at Sofular area, Malatya, Turkey. In: Stanley CJ (ed) Mineraldeposits: processes to processing. Proceedings of the FifthBiennial SGA Meeting and the Tenth Quadrennial IAGODSymposium, pp 663–666

Ozgenc I, Kibici Y (1994) The geology and chemical–mineralogicalproperties of britholite veins of Basören village (Kuluncak,Malatya). Geol Bull Turk 37:77–85 (in Turkish with Englishabstract)

Ozkan HM, Erkan Y (1994) A petrological study on a foid syeniteintrusion in central Anatolia (Kayseri-Turkey). Turk J Earth Sci3:45–55 (in Turkish with English abstract)

Pearce JA (1983) Role of the sub-continental lithosphere in magmagenesis at active continental margins. In: Hawkesworth CJ, NorryMJ (eds) Continental basalts and mantle xenoliths. Shiva,Nantwich, pp 230–249

Pearce JA, Harris NBW, Tindle AG (1984) Trace element discrimi-nation diagrams for the tectonic interpretation of granitic rocks. JPetrol 25:956–983

Pearce JA, Bender JF, De Long SE, Kidd WSF, Low PJ, Güner Y,Saroglu F, Yılmaz Y, Moorbath S, Mitchell JG (1990) Genesis of


collision volcanism in eastern Anatolia, Turkey. J VolcanolGeotherm Res 44:189–229

Platt JP, England PC (1993) Convective removal of lithospherebeneath mountain belts: thermal and mechanical consequences.Am J Sci 293:307–336

Sengör AMC, Yilmaz Y (1981) Tethyan evolution of Turkey: a platetectonic approach. Tectonophysics 75:181–241

Shand SJ (1951) Eruptive rocks. John Wiley, New YorkStendal H, Unlü T, Konnerup-Madsen J (1995) Geological setting of

iron deposits of Hekimhan province, Malatya, central Anatolia,Turkey. Trans Inst Min Metall Sect B 104:B46–B54

Stern RJ, Gottfried D (1986) Petrogenesis of a Late Precambrian(575–600 Ma) bimodal suite in Northeast Africa. ContribMineral Petrol 92:492–501

Sun SS, McDonough WF (1989) Chemical and isotopic systematics ofoceanic basalts: implications for mantle composition and pro-cesses. In: Saunders AD, Norry MJ (eds) Magmatism in theocean basins. Geol Soc Spec Publ 42:313–345

Turner SP, Foden JD, Deblond A, Duchesne JC (1992) Derivation ofsome A-type magmas by fractionation of basaltic magma: anexample from the Padhaway Ridge, South Australia. Lithos28:23–55

Turner SP, Arnaud N, Liu J, Rogers N, Hawkesworth C, Harris N,Kelley S, Van Calsteren P, Deng W (1996) Post-collision,shoshonitic volcanism on the Tibetan plateau: implications forconvective thinning of the lithosphere and the source of oceanisland basalts. J Petrol 27:45–71

Ucurum A, Larson LT, Boztug D (1996) Geology, geochemistry, andpetrology of the alkaline subvolcanic trachyte-hosted iron depositin the Karakuz area, northwestern Hekimhan–Malatya, Turkey.Int Geol Rev 38:995–1005

Volkert RA, Feigenson MD, Patino LC, Delaney JS, Drake AA Jr(2000) Sr and Nd isotopic compositions, age and petrogenesis of

A-type granitoids of the Vernon Supersuite, New Jersey Highlands,USA. Lithos 50:325–347

Whalen JB, Currie KL, Chappell BW (1987) A-type granites:geochemical characteristics, discrimination and petrogenesis.Contrib Mineral Petrol 95:407–419

Whalen JB, Jenner GA, Currie KL, Barr SM, Longstaffe FJ, Hegner E(1994) Geochemical and isotopic characteristics of granitoids ofthe Avalon Zone, southern New Brunswick: possible evidencefor repeated delamination events. J Geol 102:269–282

Yalcin H, Gündogdu MN, Gourgaud A, Vidal P, Ucurum A (1998)Geochemical characteristics of Yamadagi Volcanics in centraleast Anatolia: an example from collision-zone volcanism. JVolcanol Geotherm Res 85:303–326

Yaliniz KM, Aydin NS, Göncüoglu MC, Parlak O (1999) Terlemezquartz monzonite of central Anatolia (Aksaray-Sarikaraman):age, petrogenesis and geotectonic implications for ophioliteemplacement. Geol J 34:233–242

Yazgan E (1984) Geodynamic evolution of the Eastern Taurus region.In: Tekeli O, Göncüoğlu MC (eds) Proceedings InternationalSymposium on the Geology of the Taurus Belt, Ankara, pp 199–208

Yilmaz S, Boztug D, Ozturk A (1992) The geological setting,petrographical and geochemical characteristics of the Cretaceousand Tertiary magmatites in the Hekimhan–Hasancelebi area, NWMalatya, Turkey. International Workshop: work in progress onthe geology of Turkey, Keele, p 81

Yilmaz S, Boztug D, Ozturk A (1993) Geological setting, petrographicand geochemical characteristics of the Cretaceous and Tertiaryigneous rocks in the Hekimhan–Hasancelebi area, north-westMalatya, Turkey. Geol J 28:383–398

Zhang HF, Sun M, Zhou XH, Ying JF (2005) Geochemical constraintson the origin of Mesozoic alkaline intrusive complexes fromthe North China Craton and tectonic implications. Lithos81:297–317


Geochemical constraints on petrogenesis of Late Cretaceous alkaline magmatism in east-central Anatolia (Hasancelebi–Basören, Malatya), Turkey

Documents