Nd isotopic characteristics of Eocene to Miocene NW Anatolian granitoids: Implications for magma e

13 Pages·2014·2.98 MB·English

by  DaÄŸhan Çelebi

JournalofAsianEarthSciences93(2014)275–287
ContentslistsavailableatScienceDirect
Journal of Asian Earth Sciences
journal homepage: www.elsevier.com/locate/jseaes
The geochemical and Sr–Nd isotopic characteristics of Eocene
to Miocene NW Anatolian granitoids: Implications for magma
evolution in a post-collisional setting
⇑
Dag˘han Çelebi, Nezihi Köprüba(cid:2)sı
DepartmentofGeologicalEngineering,KocaeliUniversity,41380I_zmit,Turkey
a r t i c l e i n f o a b s t r a c t
Articlehistory: EarlyEocenetoEarlyMiocenemagmaticactivityinnorthwesternAnatolialedtotheemplacementofa
Received16December2013 numberofgranitoidplutonswithconvergentmargingeochemicalsignatures.Granitoidplutonsinthe
Receivedinrevisedform23July2014 areaaremainlydistributedwithinandnorthofthesuturezoneformedafterthecollisionoftheAnato-
Accepted25July2014
lide-TaurideplatformwiththePontidebelt.Wepresentgeochemicalcharacteristicsofthreeintrusive
Availableonline4August2014
bodiesintheregioninordertoidentifytheirsourcecharacteristicsandgeodynamicsignificance.Among
these,theÇataldag˘andIlıca-S(cid:2)amlıplutonsarelocatedtothenorthandtheOrhaneliplutonislocatedto
Keywords:
thesouthoftheIAESZ(Izmir-Ankara-ErzincanSutureZone).Theplutonsarecalc-alkaline,metaluminous,
Magmamixing
andI-typewithcompositionsfromgranitetomonzonite.TheydisplayclearenrichmentsinLILEandLREE
Granitoidicmagmatism
anddepletionsinHFSErelativetoN-MORBcompositionsandhavehigh87Sr/86Srandlow143Nd/144Nd
Fractionalcrystallization
Assimilationandfractionalcrystallization ratios.
NorthwestAnatolia TheresultsoftheoreticalFractionalCrystallization(FC)modelshowthatthesamplesareaffectedby
fractionationofK-feldspar,plagioclase,biotiteandamphibole.AssimilationandFractionalCrystallization
(AFC)modelingindicatesthatthervalue,theproportionofvariablecontaminationtofraction,ishigh,
indicatingsignificantcrustalcontaminationinthegenesisofgranitoidmagmas.Combined evaluation
ofisotopicandtraceelementdataindicatesthatthegranitoidsaretheproductsofmantle-derivedmafic
magmasvariablydifferentiatedbysimultaneouscrustalcontaminationandfractionalcrystallizationin
lowertomiddlecrustalmagmachambersinapost-collisionalsetting.
(cid:2)2014ElsevierLtd.Allrightsreserved.
1.Introduction the Armutlu, Kapıdag˘ and Lapseki peninsulas are of mostly calc-
alkaline,metaluminousandI-typeincharacterwithcompositions
The northwestern Anatolian region, lying on one of the most fromhornblendemonzogranitetogranodioriteandrepresentedby
important collision belts in the world, contains a number of anenrichmentinLILEandLREEandadepletioninHFSErelativeto
deep-seated granitoid bodies formed in association with tectonic MORBcomposition(negativeNbandTaanomalies),similartosub-
activityprevailedinthePost-LateCretaceous(Fig.1).Theseoccur- duction-related or active continental margin granites. They also
renceshavebeenthesubjectofseveralrecentinvestigations. suggest that the heat which caused partial melting within the
Harrisetal.(1994)statedthattheOrhaneligranitoidisrepre- metasomatizedpartoflithosphericmantlefollowingthecessation
sented by a metaluminous melt composition and calc-alkaline ofsubductionwasprobablyeitherduetothelateorogenicdelam-
affinity which are typical of subduction-related magmas. inationofthesubductingslaborthelowermostpartoflithospheric
DelaloyeandBingöl(2000)analyzedradiometricagesofgranitoids mantle (delamination of thermal boundary layer) and associated
inthewesternandnorthwesternAnatoliaandfoundK–Aragesof rise of hot asthenosphere. According to Boztug˘ et al. (2006), the
20.8±0.4Ma for theÇataldag˘ granitoidand 57.9±1.2, 53.0±1.1, Ilıca (Balıkesir) and Kozak (Bergama) granitoids in the west and
31.4±0.6and51.7±1.0MafortheOrhaneligranitoid.Theyinter- northwesternAnatoliaarecomposedsolelyofhighandintermedi-
pretedthesegranitoidstobeofsubductionorigin.Köprüba(cid:2)sıand ate-K, calc-alkaline, metaluminous and I-type granitoids, whilst
Aldanmaz (2004) suggested that the Eocene plutonic bodies in the Çataldag˘ (Balıkesir) granitoid consists of two different litho-
logic units. Altunkaynak (2007) examined two E–W extending
⇑ linearbeltsoftheEoceneplutonsalongtheI_zmir-Ankara-Erzincan
Correspondingauthor.Tel.:[phone].
Suture Zone (IAESZ) and suggested that the geochemical
E-mailaddress:[email protected](N.Köprüba(cid:2)sı).
http://dx.doi.org/10.1016/j.jseaes.2014.07.037
1367-9120/(cid:2)2014ElsevierLtd.Allrightsreserved.
276 D.Çelebi,N.Köprüba(cid:2)sı/JournalofAsianEarthSciences93(2014)275–287
Fig.1. MapofnorthwesternAnatoliashowingthedistributionoftheEocene–Miocenepostcollisiongranitoidplutonsalongwiththemainrockunitsexposedacrossthe
collisionzone.
characteristicsandagerelationsoftheseplutonsareinsupportofa sion of Tauride-Anatolide platform withthe Sakarya continent at
slab break-off. Karacık et al. (2008) studied the plutons in the north resulted in formation of compression deformations in the
southernMarmara,includingtheIlıcagranitoid,whicharegener- Paleocene and extension in the Oligo-Miocene (Seyitog˘lu and
ally represented by granodiorite bodies, stocks and sills within Scott, 1992, 1997; Is(cid:2)ık et al., 2004; Purvis and Robertson, 2004;
the Triassic basement rocks. They proposed that, although the Kaya et al., 2007). The Çataldag˘, Ilıca-S(cid:2)amlı and Orhaneli plutons
granitoidsareofLateCretaceoustoMioceneage,theycanbepre- are situated approximately in the east–west direction in the NW
dominantlydividedintotwogroups:TheEocenegranitoidsinthe Anatolia(Fig.1).TheÇataldag˘ granitoidcuttheMesozoicunitsof
northandtheMiocenegranitoidsinthesouth. the Sakarya Zone and was covered by the Neogene deposits and
Thisstudyreportsthegeochemicalandisotopic(Sr–Nd)datafor volcanic lavas. The Ilıca-S(cid:2)amlı granitoid intruded into the Kiraz
theOrhaneli,Çataldag˘andIlıca-S(cid:2)amlıgranitoidbodiesandparticu- MetamorfitsandÇataltepemarbleoftheSakaryaZone.TheOrha-
larly focuses on the major-trace element and isotopic data from neligranitoidintrudedintothebaserocksoftheTav(cid:2)sanlıZoneand
threeplutonicbodiesforinterpretingtheevolutionoftheEocene wascoveredbytheEarlyMiocenevolcanics(Altunkaynak,2007).
toMiocenemagmatism.TheEocene–Miocenegranitoidbodiesout-
cropped in the NW of Turkey provide important data for under- 3.Fieldandpetrographiccharacteristics
standingtheageandstagesoftheextensionregimethathasnot
beenfullyexplainedinwesternAnatolia.Thisstudycouldalsocon- The geographical distributions of the plutons are shown in
tributetotheinvestigationofsimilarpost-collisiongranitoidrocks. Fig. 1. The Çataldag˘ granitoid locally presents contact with the
metamorphicrocksofthearea.Itgenerallyintrudedintothebed-
2.Geologicalbackground dinganddiscontinuityplanesoftheolderrocksconcordantly.The
sills intruded into the foliation planes and dikes cut or intruded
Most part oftectonic – geologic history ofnorthwestAnatolia vertically into the foliation planes. The Ilıca-S(cid:2)amlı granitoid pre-
reflectstheevolutionofTethysOceanandisrepresentedbyaccre- sents sharp contacts with the neighboring rocks, forming an
tionoflithosphericblocksduetoaseriesofcollisionaleventspre- approximately2kmwidecontactmetamorphiczone.TheOrhaneli
vailed during the upper Mesozoic-Eocene (Köprüba(cid:2)sı and plutonisincontactwiththeMioceneandesitesanddacitesalong
Aldanmaz, 2004). In northwest Anatolia, in the period between thewesternborderofthepluton.Besides,theplutonhasbordered
theendoflateCretaceousandTertiary,asaresultofnortherlysub- byapproximatelyNE–SWnormalfaultsinitssoutheastpartwhere
ductionofnorthernbranchofNeotethysOceanundertheSakarya itcontactswithblueschists.
continent,theTauride-AnatolideplatformatsouthandtheSakarya Petrographically, the Çataldag˘ Granitoid is composed of holo-
continent at north were collided and, as a consequence, IAESZ crystalline granitic and granodioritic rocks. These rocks contain
crossing the wholenorthernAnatolia was formed. Granitoidplu- 30–35% quartz, 15–20% K-feldspar (orthoclase-microcline) and
tons are exposed in a large area at north and south of the 35–45% plagioclase (albite-oligoclase) and rare biotite together
Izmir-Ankarasuturezone(Köprüba(cid:2)sıandAldanmaz,2004).Colli- with accessory minerals of sphene, zircon and apatite (Table 1).
D.Çelebi,N.Köprüba(cid:2)sı/JournalofAsianEarthSciences93(2014)275–287 277
Table1
PetrographicfeaturessamplesofIlıca-S(cid:2)amlı,Çataldag˘,Orhaneliplutons.
Location Sample Name Texture Grainsize Majorminerals Accessories
Ilica-S(cid:2)amliGranitoid YK-1 Granodiorite Holocrystalline Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
YK-4 Granodiorite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
YK-5 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
YK-6 Tonalite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
YK-7 Granodiorite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
YK-8 Granodiorite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
YK-9 Granodiorite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
YK-10 Granodiorite Holocrystalline Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
KD-1 Tonalite Holocrystalline Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
KD-2 Tonalite Holocrystalline Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
KD-3 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
IL-1 Granodiorite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
IL-2 Granodiorite Porphyritic Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
IL-3 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
IL-4 Granodiorite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Çataldag˘Granitoid Bo-1 Granodiorite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Bo-2 Granodiorite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Bo-3 Granite Graphic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Bo-4 Granite Graphic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Bo-5 Granodiorite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Bo-6 Granodiorite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Bo-7 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Bo-8 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.+Ms
Bo-9 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Bo-10 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Bo-11 Granite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
SU-1 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
SU-2 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
SU-3 Granodiorite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
SU-7 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
SU-9 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
SU-10 Granodiorite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
OrhaneliGranitoid O-1 Granite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-2 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-3 Granite Porphyritic Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-4 Granite Holocrystalline Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-5 Granite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-6 Granite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-7 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-11 Granite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-13 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-14 Granite Porphyritic Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-15 Granite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-16 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-17 Granite Holocrystalline Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-18 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-19 Granite Graphic Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-20 Granite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-21 Granodiorite Holocrystalline Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-22 Granodiorite Porphyritic Mediumtocoarsegrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-23 Granodiorite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-24 Tonalite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-25 Granodiorite Holocrystalline Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
O-26 Granodiorite Porphyritic Mediumgrain Q,Pl.,KFel.,Am.,Bi. Zr,Ap.,S.,Op.
Plutons Ilıca-S(cid:2)amlıGranitoids Çataldag˘Granitoids OrhaneliGranitoids
Phenocrystalgrainsize Mediumtocoarsegrain Mediumgrain Mediumtocoarsegrain
Phenocrystalmodalabundance(%) 94 95 96
Phenocrystalshape Regulartoirregular Regulartoirregular/irregular Regulartoirregular
Holocrystalline texture is common in granitoids. The samples of crystalsandsomequartzgrainsshowundulatoryextinctionunder
IlıcaS(cid:2)amlıplutonaregranitic,granodioriticandtonaliticincompo- cross polarized light. Hornblende are seen in pale green color as
sition, and the majority of the samples display a holocrystalline euhedraland subhedralcrystals and in some samples, chloritiza-
porphyritic texture. The samples contain 22–33% quartz, 15–33% tion is seen due to alteration. Biotite minerals are dark brown in
alkalifeldspar,36–48%plagioclase.TheOrhaneliGranitoidisgra- color and some of them present chloritization along their
niticandgranodioriticincompositionwithholocrystallineporfhy- cleavages.
ritictexturesimilartotheÇataldag˘ pluton.TherocksofOrhaneli
plutoncontain26–34%quartz,21–32%alkalifeldspar,36–48%pla-
gioclase.Plagioclasecrystalsinspectedinalloftheplutonsarein 4.Analyticalmethods
formofeuhedralandsubhedralcrystalsanddisplaycompositional
zoning.Alkalifeldsparsdisplaysimpletwinningalongwithgraph- Majorandselectedtraceelementconcentrationswereanalyzed
icaltextures.Quartzmineralsareseenasanhedralamongfeldspar withatotalof54samplescollectedfromÇataldag˘,Ilıca-S(cid:2)amlıand
278 D.Çelebi,N.Köprüba(cid:2)sı/JournalofAsianEarthSciences93(2014)275–287
Table2
RepresentativechemicalanalyzesofthegranitoidsfromNWAnatolia.
O-1 O-2 O-3 O-4 O-5 O-6 O-7 O-11 O-13 O-14 O-15 O-16 O-17 O-18 O-19 O-20 O-21 O-22 O-23 O-24 0-25 O-26
Orhanelipluton
SiO2 60.23 61.16 60.57 58.33 60.85 63.85 59.16 58.78 61.88 62.9 60 63.21 59.01 61.61 60.64 62.54 62.7 60.64 63.84 62.55 64.81 62.04
TiO2 0.53 0.49 0.51 0.57 0.47 0.48 0.58 0.57 0.5 0.45 0.53 0.43 0.6 0.5 0.5 0.43 0.51 0.51 0.47 0.48 0.47 0.48
Al2O3 16.42 16.58 16.27 16.72 16.52 16.82 16.58 16.7 17.19 16.67 16.44 16.56 16.63 16.95 15.63 16.59 17.15 16.43 16.65 16.89 16.76 17.03
Fe2O3 5.95 5.56 5.76 6.38 6.03 3.82 6.37 6.23 5.47 4.62 5.69 4.26 6.25 4.83 5.88 4.69 4.57 5.24 4.87 4.91 4.26 4.94
MnO 0.1 0.12 0.11 0.11 0.1 0.05 0.12 0.11 0.1 0.09 0.11 0.07 0.13 0.1 0.09 0.08 0.09 0.09 0.08 0.09 0.08 0.08
MgO 2.31 1.99 2 2.3 1.93 1.78 2.28 2.45 2.12 1.94 2.21 1.59 2.41 2.09 2.1 1.64 2.16 2.36 1.97 2.08 1.89 2.23
CaO 6.08 5.78 6.06 6.85 6.01 4.94 6.14 6.74 5.8 5.83 6.04 5.4 6.4 6.01 5.99 5.57 5.56 6.58 5.06 5.43 4.73 5.92
Na2O 4.69 4.78 5.15 5.49 4.57 4.03 5.22 5.08 4.16 4.17 5.05 4.76 5.17 4.73 5.24 4.99 4.19 4.55 4.15 4.25 3.79 4.22
K2O 2.89 2.83 3.04 2.8 2.85 2.74 2.69 2.64 2.09 2.62 3.17 2.94 2.66 2.55 3.2 2.64 2.2 2.72 2.06 2.46 2.07 2.26
P2O5 0.02 0 0 0.01 0 0.05 0.03 0.01 0.01 0.04 0.03 0 0.06 0.04 0.03 0.01 0.05 0.02 0.03 0.03 0.04 0.03
LOI 0.65 0.59 0.43 0.33 0.55 1.36 0.61 0.58 0.58 0.57 0.59 0.68 0.58 0.49 0.57 0.67 0.72 0.76 0.73 0.72 1.02 0.7
Total 99.89 99.88 99.89 99.89 99.89 99.9 99.78 99.9 99.89 99.9 99.86 99.9 99.89 99.89 99.87 99.86 99.9 99.9 99.9 99.9 99.92 99.93
Mg# 0.25 0.24 0.23 0.24 0.22 0.29 0.23 0.25 0.25 0.27 0.25 0.24 0.25 0.27 0.24 0.23 0.29 0.28 0.26 0.27 0.28 0.28
ADI 0.85 0.87 0.81 0.78 0.87 1.01 0.84 0.82 1.02 0.93 0.81 0.89 0.83 0.9 0.76 0.89 1.02 0.84 1.05 0.99 1.12 0.98
Sc 5 3.2 3.4 3.5 3.3 4.1 5.9 3.3 3.6 3.6 3.7 3.5 3.6 3.8 4.5 3.3 4.1 3.9 4.2 3.4 3.7 4.2
V 88 73 68 78 73 50 72 77 72 57 56 46 66 63 63 47 67 69 80 61 61 70
Ni 4.6 3.6 4.5 2.9 7 2.6 4.4 3.3 2.1 4.5 3.3 5.6 2.9 4.9 6.8 4.7 3.2 4 4.1 4 3.3 5.3
Cu 93.8 5.34 8.43 14.9 16.4 2.75 3.65 6.67 3.55 6.88 4.85 9.82 7.18 7.97 7.19 6.61 4.35 11.3 7.01 6.23 6.17 7.42
Zn 41.5 87.8 31.5 36.8 30.9 38.4 44.8 36.8 30.5 37.6 40.4 35.1 45.6 34.2 39.1 27.1 38.1 31.4 34.4 34.6 36.3 39
Ga 7.18 5.3 4.74 6.49 4.84 6.65 5.54 5.91 5.91 3.54 4.03 5.28 6.37 4.51 6.54 6.42 4.21 7.3 7.96 4.66 4.64 4.38
Rb 37.2 26.7 31 29.1 31.3 22.2 46 20.3 24.6 29 31.5 29.8 31.9 34 39.6 28.3 35.4 22.3 31.2 24.1 9.6 32.3
Sr 94.9 58.1 71.1 78.6 85.5 61.6 86.7 69.7 69.3 80.5 80.3 69.3 75.9 88 135 63.8 92.3 87.7 94.7 68 62.8 86.3
Y 15.2 12.2 11.5 12.8 11.4 17 12.9 11.7 11 10 13.8 12.9 9.94 10.1 12.3 10.1 11.5 12.5 11.7 10.5 11.2 11.5
Zr 4.7 3.8 4.1 3.7 4.6 2.3 2.2 4.4 3.3 2.7 2.6 3.1 2.2 3 3 2.9 2.6 3.5 3 3.4 3 3.2
Nb 0.5 0.5 0.5 0.5 0.4 0.7 0.4 0.6 0.5 0.5 0.7 0.7 0.6 0.4 0.5 0.6 0.5 0.6 0.5 0.5 0.7 0.5
Cs 1.13 1.3 1.13 1.15 1.25 0.71 1.66 0.73 1 0.95 0.96 0.73 0.94 1.11 1.01 0.61 0.99 0.57 0.76 0.94 0.35 0.81
Ba 244 145 142 133 161 152 236 194 185 273 267 226 238 263 352 193 306 232 287 229 111 297
La 11.1 13.1 15.6 16.2 13.1 14.3 17 12.3 13.2 14.1 12.4 26.2 18.6 15 20.3 17.9 10.3 16.3 20.1 19.9 14.4 12.5
Ce 26.6 26.9 30.3 32.8 26.4 31.6 35 25.5 26.3 27.8 26.2 50 36.9 30.2 40 34.5 23.4 33.8 39.2 37.6 28.6 26
Pr 3.3 3.1 3.2 3.6 2.9 3.9 4 2.9 2.9 3.2 3.1 5.2 4 3.4 4.4 3.8 2.8 3.9 4.2 4.1 3.2 3.1
Nd 12.7 11.6 11.2 12.8 10.5 16.3 14.6 10.8 10.6 11.5 12 17.8 14.2 12.5 15.4 13.5 11 14.5 14.4 14.3 11.9 11.3
Sm 2.6 2.3 2.1 2.4 2.1 3.6 2.7 2.1 2.1 2.1 2.5 2.8 2.4 2.3 2.7 2.3 2.3 2.6 2.5 2.5 2.2 2.2
Eu 0.5 0.4 0.4 0.5 0.4 0.7 0.5 0.4 0.4 0.4 0.4 0.4 0.4 0.5 0.5 0.4 0.4 0.5 0.4 0.5 0.4 0.4
Gd 2.6 2.4 2.1 2.4 2.2 3.3 2.7 2.2 2.2 2.2 2.6 2.4 2.3 2.3 2.4 2.2 2.3 2.5 2.3 2.5 2.4 2.3
Tb 0.4 0.3 0.3 0.3 0.3 0.5 0.4 0.3 0.3 0.3 0.4 0.3 0.3 0.3 0.3 0.3 0.3 0.3 0.3 0.3 0.3 0.3
Dy 2.47 2.2 2.06 2.21 2.05 3.01 2.31 2.05 2.02 1.87 2.41 2.09 1.74 1.87 2.08 1.78 2.03 2.19 1.97 2.01 2.05 2.03
Ho 0.5 0.5 0.4 0.5 0.4 0.6 0.5 0.4 0.4 0.4 0.5 0.4 0.4 0.4 0.4 0.4 0.4 0.4 0.4 0.4 0.4 0.4
Er 1.6 1.3 1.3 1.4 1.2 1.8 1.4 1.2 1.3 1.1 1.5 1.3 1.1 1.1 1.2 1.1 1.2 1.3 1.2 1.2 1.2 1.2
Tm 0.2 0.2 0.2 0.2 0.2 0.3 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2
Yb 1.6 1.4 1.2 1.4 1.2 1.7 1.2 1.3 1.3 1.1 1.5 1.3 1.1 1.1 1.2 1.1 1.1 1.4 1.1 1.2 1.2 1.2
Lu 0.2 0.2 0.2 0.2 0.2 0.3 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2
Hf 0.2 0.2 0.2 0.2 0.3 0.1 0.1 0.3 0.2 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.2 0.1 0.2 0.2 0.1
Ta 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05
Pb 2.41 2.14 2.02 2.09 2.45 3.46 2.7 1.99 2.49 2.2 2 2.06 2.22 2.34 2.44 2.01 3.15 2.19 1.92 2.17 2.13 2.01
Th 9.6 9.4 9.1 10.6 9 6.7 8 8.5 7.3 9 7.2 10.9 8.6 7.8 10.1 8.9 6.3 8.7 8.5 7.4 7.4 6.5
U 1.3 1.9 1.4 1.7 1.8 2.1 1.9 1.1 1.7 1.9 2.3 1.8 2.1 1.6 2 1.4 1.3 1.8 1.2 1.6 1.5 1.4
Bo-1 Bo-2 Bo-3 Bo-4 Bo-5 Bo-6 Bo-7 Bo-8 Bo-9 Bo-10 Bo-11 SÜ-1 SÜ-2 SÜ-3 SÜ-7 SÜ-9 SÜ-10 YK-1 YK-4 YK-5 YK-6 YK-7
Çataldag˘pluton Ilica-S(cid:2)amlipluton
SiO2 61.34 67.48 65.87 63.09 68.58 60.95 72.28 66.77 70.42 67.53 64.13 66.72 65.66 71.41 67.39 67.37 69.54 64.27 63.67 58.92 63.03 59.44
TiO2 0.56 0.4 0.4 0.51 0.26 0.56 0.17 0.39 0.27 0.35 0.45 0.39 0.47 0.3 0.33 0.34 0.33 0.53 0.53 0.66 0.59 0.62
Al2O3 15.94 16.36 16.28 16.67 15.8 15.85 13.71 16.23 15.8 13.91 14.63 15.81 15.85 15.51 16.14 16.13 15.53 15.52 14.99 15.41 15.97 16.49
Fe2O3 4.29 2.56 2.86 4.06 1.71 4.79 1.33 2.54 1.34 2.77 3.25 2.4 3.04 1.45 1.75 2.23 2.06 4.14 4.68 6.41 4.97 5.96
MnO 0.08 0.09 0.06 0.11 0.03 0.12 0.02 0.01 0.01 0.05 0.05 0.02 0.02 0.01 0.01 0.02 0.02 0.36 0.07 0.1 0.06 0.09
MgO 1.38 0.83 1.08 1.44 0.59 1.26 0.39 0.8 0.58 0.91 1.1 0.82 0.82 0.59 0.53 0.72 0.83 2.03 1.96 2.81 2.32 2.87
CaO 4.58 2.79 3.4 4.54 2.36 4.5 0.85 1.5 1.33 3.05 3.02 2.51 3.19 1.95 1.94 1.94 2.09 3.93 4.34 5.94 4.98 5.76
Na2O 6.09 4.64 5.02 5.72 5.13 6.3 4.78 3.95 5.03 4.81 5.81 6.14 6.38 4.53 5.61 5.8 4.53 3.63 4.24 4.63 3.88 4.33
K2O 4.33 3.16 3.9 3.05 3.88 4.65 5.87 6.75 4.5 5.47 6.52 4.65 3.75 3.58 5.28 4.13 3.25 4.54 4.91 4.01 3.73 3.78
P2O5 0.18 0.04 0.07 0.13 0.03 0.14 0.01 0 0 0 0.01 0 0.02 0 0 0.01 0.02 0.07 0.03 0.1 0.09 0.11
LOI 1.12 1.57 0.98 0.6 1.55 0.78 0.5 0.98 0.66 1.02 0.92 0.43 0.67 0.6 0.94 1.24 1.35 1.22 0.47 0.88 0.29 0.46
Total 99.88 99.92 99.93 99.92 99.92 99.89 99.92 99.92 99.94 99.87 99.9 99.89 99.88 99.93 99.92 99.92 99.55 100.24 99.88 99.87 99.91 99.9
Mg# 0.22 0.22 0.25 0.23 0.23 0.18 0.2 0.21 0.27 0.22 0.22 0.23 0.19 0.26 0.21 0.22 0.26 0.3 0.26 0.27 0.29 0.29
ADI 0.74 1.07 0.92 0.88 0.96 0.71 0.8 0.89 0.99 0.72 0.65 0.82 0.83 1.06 0.86 0.94 1.09 0.89 0.77 0.74 0.89 0.83
Sc 3.6 2.2 2.2 2.8 1.6 3.1 1.8 1.2 1.7 3.6 3.5 2.3 1.6 1.7 1.4 1.8 1.9 1.8 3.8 6.1 4.4 5.9
V 43 25 27 38 12 32 5 3 6 18 23 18 15 14 8 12 15 56 61 94 67 78
Ni 3.2 5.5 3.6 5.2 2.4 4.3 2.7 3.3 2.1 5.4 3.7 2.7 3.5 2 3 3.4 4.1 7.3 5.2 9.5 7.5 9.2
Cu 5.38 8.15 9.27 11.3 6.71 13.5 7.38 6.71 3.56 16.1 7.3 6.68 6.96 9.6 10.6 2.03 6.09 105 23.6 21.2 16.7 14.4
Zn 42.8 101 58.6 69.6 32.2 55.5 14.3 46 43.5 39.9 37 57.2 61.5 44.6 23.5 57.8 45.3 31.5 30.9 46.6 37.6 45.1
Ga 5.86 4.84 5.18 7.1 3.89 4.77 3.7 5.67 6.13 4.1 4.95 7.87 6.36 5.84 6.07 6.68 6.02 4.11 3.17 6.94 2.06 5.64
Rb 35 34.5 60.6 66.7 34.6 49.8 43.2 45.9 60.5 59.6 53.3 74.8 42.8 41.6 62.3 79.9 85.6 11.1 37.8 33.4 31 36.9
Sr 62.2 93.5 65.6 86.4 76.4 66.5 4.1 8.6 11.2 15.9 15 20.1 36.9 25.7 12.9 13.9 25.8 59.2 69.5 80.7 76.8 85
D.Çelebi,N.Köprüba(cid:2)sı/JournalofAsianEarthSciences93(2014)275–287 279
Y 17.4 14.2 12.1 14.4 12.9 16.1 6.89 3.55 4.64 18.1 20.7 4.5 5.02 4.55 4.39 6.66 7.33 15.5 17.4 16.5 12.5 11.7
Zr 3.2 3 1.7 4.5 1.2 3 1.6 2.3 1.4 2 1.4 1.8 1.6 1.3 2.2 1.6 1.6 6.6 4.3 7.2 5.6 5.8
Nb 2.3 1.6 1.5 1.7 1.2 2.4 1 0.6 0.5 2.6 2.6 0.5 0.4 0.8 0.6 0.6 0.8 1.4 1.1 1 0.8 0.5
Cs 3.7 3.55 5.78 7.07 2.93 3.86 3.95 3.32 8.32 3.53 3.8 7.37 3.73 4.55 6.25 7.84 9.23 0.74 1.89 2.26 1.73 2.12
Ba 82.4 147 109 144 87.9 99.6 22.3 91.6 45.7 97.2 129 85.2 126 80.1 42.7 58.3 279 137 240 246 268 284
La 47.9 41.3 33.9 42.5 22.7 47.7 13.6 21.2 19 29.1 26.3 20.5 46.7 30.6 19.9 18.5 29.4 28.3 42.3 33.3 31.1 24.7
Ce 83 71 58.9 74.9 40.2 78.4 26.8 38.4 35.7 51.9 47 39 75 55.4 35.2 33.3 48.4 54.5 72.2 63.6 56.1 46.8
Pr 9.4 7.9 6.5 8.6 4.3 8.8 3 4.1 3.9 5.6 5.2 4.3 7.5 6 3.8 3.6 5 5.9 7.6 7.2 6.1 5.2
Nd 33.2 28.4 22.4 30.8 14.7 31.2 10.3 14.2 13.8 19.3 18.1 14.8 25.1 20.1 13.2 13 16.5 21.3 24.7 26 21.2 19.2
Sm 5.7 4.9 3.9 5.3 2.8 5.3 2.5 2.6 2.6 3.7 3.6 2.6 3.9 3.2 2.2 2.4 2.8 3.7 4.1 4.6 3.6 3.5
Eu 1.4 1.2 1 1.3 0.6 1.3 0.1 0.1 0.2 0.2 0.3 0.1 0.4 0.2 0.1 0.2 0.3 0.7 0.7 0.8 0.6 0.7
Gd 4.6 4.3 3.3 4.6 2.7 5 2.3 2.3 2.2 3.8 3.9 1.9 3 2.4 1.8 2.1 2.5 3.7 3.9 4 3.2 3.2
Tb 0.6 0.5 0.4 0.5 0.4 0.6 0.3 0.2 0.2 0.6 0.6 0.2 0.3 0.2 0.2 0.3 0.3 0.4 0.5 0.5 0.4 0.4
Dy 3.05 2.82 2.27 2.77 2.42 3.41 1.57 1.12 1.16 3.4 3.53 1.03 1.35 1.1 0.99 1.44 1.66 2.66 3.12 2.99 2.46 2.34
Ho 0.6 0.5 0.4 0.5 0.4 0.6 0.3 0.2 0.2 0.7 0.7 0.2 0.2 0.2 0.2 0.2 0.3 0.5 0.6 0.6 0.5 0.4
Er 1.6 1.4 1.1 1.4 1.2 1.6 0.6 0.3 0.4 1.8 2 0.4 0.4 0.4 0.4 0.6 0.6 1.4 1.8 1.8 1.3 1.3
Tm 0.2 0.2 0.2 0.2 0.2 0.2 0.1 0.1 0.1 0.3 0.3 0.1 0.1 0.1 0.1 0.1 0.1 0.2 0.3 0.3 0.2 0.2
Yb 1.4 1.4 1 1.2 1 1.5 0.6 0.1 0.2 1.6 2.1 0.2 0.2 0.2 0.2 0.3 0.4 1.3 1.7 1.8 1.2 1.3
Lu 0.2 0.2 0.1 0.2 0.1 0.2 0.1 0.1 0.1 0.2 0.3 0.1 0.1 0.1 0.1 0.1 0.1 0.2 0.2 0.2 0.2 0.2
Hf 0.1 0.1 0.1 0.2 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.4 0.2 0.4 0.3 0.3
Ta 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05
Pb 7 52.3 9.24 10.2 14 6.34 10.3 4.7 8.46 7.89 6.83 6.3 5.63 11.5 5.23 3.73 9.78 17.5 6.33 7.63 6.18 7.36
Th 18.2 18.3 14.5 20.9 10.3 20.4 19.9 9.9 11.2 20.9 23.2 11.1 17.5 15.1 11.9 11.3 10.9 32.3 41.3 33.5 54.2 24.5
U 9.6 6.3 10.7 11.9 16.3 8.7 3.1 1.6 4.9 7.5 6.8 1.9 6 4.5 1.1 1.2 1.1 4.7 9.1 7.8 7.7 2.5
YK-8 YK-9 YK-10 IL-1 IL-2 IL-3 IL-4 KD-1 KD-2 KD-3
Ilica-S(cid:2)amlipluton
SiO2 62.28 61.06 58.24 59.54 60.19 60.1 59.92 59.13 58.22 59.26
TiO2 0.62 0.6 0.68 0.65 0.64 0.62 0.66 0.65 0.68 0.67
Al2O3 15.72 15.5 15.54 16.14 16.11 16.17 16.19 16.59 16.25 16.66
Fe2O3 5.37 5.48 7.3 6.07 5.85 5.77 6.06 6.13 6.53 5.83
MnO 0.08 0.1 0.11 0.09 0.09 0.08 0.1 0.11 0.1 0.09
MgO 2.66 2.66 2.61 2.87 2.96 2.71 2.92 2.88 3.11 2.4
CaO 4.99 5.16 5.72 5.83 5.71 5.61 5.71 5.7 5.86 5.67
Na2O 3.94 4.3 4.71 4.33 4.08 4.42 4.36 4.3 4.43 4.27
K2O 3.58 4.22 4.06 3.46 3.62 3.7 3.43 3.43 3.83 3.56
P2O5 0.11 0.09 0.07 0.06 0.06 0.06 0.07 0.08 0.09 0.08
LOI 0.57 0.75 0.08 0.75 0.61 0.65 0.49 0.92 0.82 1.42
Total 99.92 99.92 99.12 99.79 99.92 99.89 99.89 99.92 99.91 99.9
Mg# 0.3 0.29 0.24 0.29 0.3 0.29 0.29 0.29 0.29 0.26
ADI 0.88 0.79 0.75 0.83 0.84 0.83 0.84 0.87 0.81 0.87
Sc 4.7 4.9 5.2 5.6 5.5 4.7 4.3 4 4.7 7.1
V 80 73 74 80 80 80 75 74 81 93
Ni 8.1 9.6 12 5.5 8.1 5.2 6.5 5.1 6.6 5.9
Cu 12.9 12.3 18.4 9.74 13.9 7.34 8.95 11.9 13.6 9.32
Zn 42.7 35.9 46.6 37.2 48.5 45.7 46 119 45 45.1
Ga 5.78 2.98 3.82 2.81 6.21 5.95 4.08 4.21 4.97 6.12
Rb 40.6 42.5 39.5 43.1 39.8 32 36.5 18.2 19.9 36.7
Sr 66 75.6 127 90.8 83.1 84.7 68.6 70.2 81.4 86.8
Y 13 13.3 16.4 13.4 15 13 12.4 11.8 13.3 12.4
Zr 4.8 5.8 4.9 5 6.9 4.9 5.8 3.8 5.6 3.6
Nb 0.7 0.8 0.6 0.5 0.8 0.6 0.7 0.7 0.5 0.5
Cs 1.91 2.45 1.95 2.67 3.23 2.88 3.74 1.68 1.31 6.38
Ba 297 295 427 347 419 396 394 280 326 233
La 31.5 31.9 24.1 28.8 24.9 23.9 21.4 20.2 20.6 28.2
Ce 55.4 55.6 48.1 49.1 46.3 44.3 40.2 37.2 38.3 50.5
Pr 5.9 5.8 5.4 5 5 4.8 4.4 4.1 4.2 5.4
Nd 20.2 20.3 19.7 17.2 17.6 16.9 15.7 14.8 15.4 18.4
Sm 3.4 3.5 3.7 2.9 3.1 3.1 2.9 2.6 2.8 3.1
Eu 0.6 0.6 0.7 0.5 0.5 0.5 0.5 0.5 0.5 0.5
Gd 3 3.2 3.6 2.9 3 2.8 2.9 2.6 2.7 2.8
Tb 0.4 0.4 0.5 0.4 0.4 0.4 0.4 0.4 0.4 0.4
Dy 2.32 2.49 3.03 2.41 2.53 2.33 2.32 2.22 2.18 2.26
Ho 0.5 0.5 0.6 0.5 0.5 0.5 0.5 0.4 0.5 0.5
Er 1.3 1.4 1.8 1.4 1.6 1.3 1.4 1.3 1.3 1.3
Tm 0.2 0.2 0.3 0.2 0.2 0.2 0.2 0.2 0.2 0.2
Yb 1.3 1.3 1.6 1.4 1.5 1.3 1.3 1.1 1.1 1.2
Lu 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2
Hf 0.2 0.3 0.2 0.2 0.3 0.2 0.3 0.1 0.2 0.1
Ta 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05
Pb 5.31 5.72 19.1 6.53 9.25 17.4 14.8 58.5 14.5 33.6
Th 26.7 30 26.4 20.8 21.5 21.9 20.7 17.6 21.5 20.6
U 6.1 6.3 4.4 6.5 4.6 4.7 4.8 2 1.8 2.5
280 D.Çelebi,N.Köprüba(cid:2)sı/JournalofAsianEarthSciences93(2014)275–287
Orhaneli granitoids. Analyses of the samples were carried out at 16.66%,andNa Ocontentbetween3.94%and4.71%.Thesamples
2
Actlabs (Activation Laboratories Ltd.) in Ontario with the ICP-MS of the Çataldag˘ granitoid present a SiO content from 60.95 to
2
method.Resultsofthemajorandtraceelementanalysesaregiven 72.28,Al O %contentfrom13.91%to16.67%,andaNa Ocontent
2 3 2
inTable2. from 4.53% to 6.30%. The samples of the Orhaneli granitoid are
The Sr and Nd isotope analyses were conducted at the Radio- composedofSiO contentbetween58.30%and63.85%,Al O con-
2 2 3
genic Isotope Laboratory of the Middle East Technical University, tentbetween17.19%and15.63%,andNa Ocontentbetween5.24%
2
Ankarainasimilarmannertotheanalyticalproceduresdescribed and3.79%.
by Köksal and Göncüog˘lu (2008). Isotope ratios were measured In the major and trace element Harker diagrams, increasing
usingaTritonMulti-CollectorThermalIonizationMassSpectrom- trendsofSiO withincreasingK OandRbcontentsanddecreasing
2 2
eter (TIMS). Powdered samples (ca. 80mg) were weighed and TiO ,Al O ,Fe O ,MgO,CaOandP O contentsofstudiedsamples
2 2 3 2 3 2 5
transferredintoteflonperfluoroalkoxyvials.Sampleswereleached can be explained by a fractional crystallization. Increasing SiO
2
with 4ml of 52% HF for four days at 160(cid:3)C on the hot plate. contentswithadecreaseinTiO isattributedtosphenecrystalliza-
2
Digested samples were dried and then dissolved overnight in tion whilst the decrease in P O is due to apatite crystallization.
2 5
4ml6NHClat160(cid:3)Conthehotplate.Leachinganddryingwere DecreasingtrendsinCaO andAl O concentrationsareexplained
2 3
doneonteflonhotplateswithinlaminarflowhotboxes. byplagioclasefractionation.Additionally,fractionalcrystallization
Sr was separated in 2.5N HCl medium using 12ml Bio Rad effectsonstudiedsamplesareindicatedbyEu,GdandErnegative
poly-propylene columns with 2ml Bio Rad AG50W-X12, anomalies in chondrite normalized diagrams and P–Ti negative
100–200 mesh resin. Sr was loaded on single Re-filaments with anomalies in N-MORB normalized diagrams. The negative Eu
Ta-activatorand0.005NH PO ,anditsisotopiccompositionwas anomaly is attributed to plagioclase fractionation, and negative
3 4
determinedbyusingthestaticmulti-collectionwithTritonTIMS. Gd–Eranomaliesareduetoamphibolefractionation.Thenegative
Analytical uncertainties are given at the 2-sigma error. 87Sr/86Sr Tianomalyisassociatedwithfractionationofilmeniteandtitanite
data are normalizedwith 86Sr/88Sr=0.1194.During thecourse of (sphene)whilethenegativePanomalyisexplainedbyanapatite
the measurements, Sr standard NIST SRM 987 was measured as fractionation.
0.710240±5(n=3)whichiswithintheerroroftheacceptedvalue
forthisstandard. 6.Isotopechemistry
NdwasseparatedfromtheREEfractionina0.022NHClmed-
ium using 12ml Bio Rad poly-propylene columns with 2ml bio- IsotopevaluesofsamplescollectedfromtheOrhaneli,Çataldag˘
beads (Bio Rad) coated with HDEHP (bisethyexyl phosphate). Nd andIlıca-S(cid:2)amlıgranitoidplutonsareshowninTable3.Initialiso-
was loaded on the double Re-filaments with 0.005N H3PO4, and topevaluesofsampleswerecomputedusingages51.8Maforthe
itsisotopiccompositionwasdeterminedbyusingstaticmulti-col- Orhanelipluton,20.4MafortheÇataldag˘ plutonand21.9Mafor
lectionwithTritonTIMS.Analyticaluncertaintiesaregivenatthe theIlıca-S(cid:2)amlıpluton(Altunkaynaketal.,2012a,2012b).87Sr/86Sr
2-sigma error. 143Nd/144Nd data are normalized to 146Nd/144- and (87Sr/86Sr) ratios of the Orhaneli pluton are 0.706412–
i
Nd=0.7219.ThemeasurementoftheNdLaJollastandardgavea 0.707042 and 0.705581–0.706132. Those of Çataldag˘ pluton are
value of 0.511850±5 (n=3) which is within the accepted error 0.706923–0.711293and0.706283–0.707392and87Sr/86Srand(87-
range for this standard. No corrections were applied to the Nd Sr/86Sr) ratios of Ilıca-S(cid:2)amlı pluton are 0.707215–0.707651 and
i
andSrisotopiccompositionsforinstrumentalbias. 0.706842–0.707274. The e Nd values of these plutons are in the
range of (cid:2)3.51 to (cid:2)4.06, (cid:2)3.45 to (cid:2)7.06 and (cid:2)3.27 to (cid:2)3.59
5.Wholerockgeochemistry respectively.
Comparisonofisotoperesultstoagedatafrompreviousworks
The samples of the Ilıca-S(cid:2)amlı granitoid have a SiO content indicatesthatastheagebecomes younger,the(87Sr/86Sr) values
2 i
between 58.22% and 64.27%, Al O content between 14.99% and increase (Fig. 2). In the same diagram, isotope and age data of
2 3
Table3
SrandNdisotopeanalysesofOrhaneli,Çataldag˘andIlıca-S(cid:2)amlıgranitoids.
Sample Loc. Rocktype Rb Sr 87Rb/86Sr 87Sr/86Sr Std.error (87Sr/86Sr)i Sm Nd 147Sm/144Nd 143Nd/144Nd Std.error eNd(0)
(ppm) (ppm) 87Sr/86Sr (ppm) (ppm) 143Nd/144Nd
O-1 Orhaneli Granite 37.2 94.9 1.14 0.706412 ±6 0.705581 2.6 12.7 0.1292 0.512502 ±4 (cid:2)3.5
O-4 Granite 29.1 78.6 1.07 0.706408 ±6 0.705623 2.4 12.8 0.1184 0.512504 ±9 (cid:2)3.4
O-5 Granite 31.3 85.5 1.06 0.706414 ±3 0.705644 2.1 10.5 0.1262 0.512490 ±5 (cid:2)3.7
O-16 Granite 29.8 69.3 1.25 0.707042 ±5 0.706132 2.8 17.8 0.0993 0.512494 ±9 (cid:2)3.4
O-17 Granite 31.9 75.9 1.22 0.706567 ±5 0.705672 2.4 14.2 1.1067 0.512466 ±4 (cid:2)4.1
O-22 Granodiorite 22.3 87.7 0.74 0.706475 ±4 0.705934 2.6 14.5 0.1138 0.512471 ±7 (cid:2)4
Bo-3 Çataldag˘ Granite 60.6 65.6 2.68 0.707078 ±5 0.706302 3.9 22.4 0.1099 0.512467 ±5 (cid:2)3.7
Bo-4 Granite 66.7 86.4 2.24 0.706923 ±4 0.706283 5.3 30.8 0.1086 0.512477 ±3 (cid:2)3.5
Bo-6 Granite 49.8 66.5 2.17 0.706957 ±4 0.706334 5.3 31.2 0.1072 0.512471 ±45 (cid:2)3.6
Bo-7 Granodiorite 43.2 4.1 30.54 0.713613 ±5 0.706792 2.5 10.3 0.1532 0.512413 ±9 (cid:2)4.8
Bo-8 Granite 45.9 8.6 15.47 0.711293 ±5 0.706821 2.6 14.2 0.1156 0.512293 ±9 (cid:2)7.1
SU-1 Granite 74.8 20.1 10.78 0.710508 ±5 0.707392 2.6 14.8 0.1109 0.512367 ±9 (cid:2)5.6
YK-4 Ilica-S(cid:2)amli Granodiorite 37.8 69.5 1.58 0.707325 ±6 0.706842 4.1 24.7 0.1048 0.512475 ±5 (cid:2)3.6
YK-5 Granite 33.4 80.7 1.20 0.707215 ±5 0.706841 4.6 26 0.1117 0.512482 ±5 (cid:2)3.4
KD-3 Granite 36.7 86.8 1.23 0.707651 ±5 0.707274 3.7 19.7 0.1186 0.512473 ±4 (cid:2)3.6
IL-3 Granite 32 84.7 1.09 0.707530 ±5 0.707193 3.1 16.9 0.1158 0.512488 ±4 (cid:2)3.2
YK-10 Granodiorite 39.5 127 0.90 0.707273 ±5 0.706992 3.1 18.4 0.1063 0.512492 ±12 (cid:2)3.3
eNd(0)=104*((143Nd/144Nd)sample(0)/(143Nd/144Nd)CHUR(0)(cid:2)1).
(87Sr/86Sr)i=(87Sr/86Sr)sample(t)(cid:2)(Rb/Sr)*ekt(cid:2)1.
k(87Rb)=1.42*10(cid:2)5Ma.
k(147Sm)=1.42*10(cid:2)5Ma.
(143Nd/144Nd)CHUR(0)=0.512638.
D.Çelebi,N.Köprüba(cid:2)sı/JournalofAsianEarthSciences93(2014)275–287 281
Fig.2. 87Sr/86SrversusagediagramforthenorthwesternAnatoliangranitoids.
Fig.4. ThemolecularAl2O3/Na2O+K2O(A/NK)versusAl2O3/CaO+Na2O+K2O(A/
theArmutluandKapıdag˘plutoninthenorthofthestudiedregion CNK)(ManiarandPiccoli,1989)plotsshowingthepredominantlymetaluminous
are also plotted. Increasing (87Sr/86Sr) values are attributed to characterofEocenetoMiocenegranitoidsfromnorthwesternAnatolia.
i
increasingcrustalcontaminationeffect.
intothemetaluminousfield.Afewsamplesplotintoperalumini-
ousandperalkalinefield.
7.Discussion
InHarkerdiagramswheremajorandtraceelementabundances
of samples are plottedagainst their SiO contents (Fig. 5), trends
7.1.Petrogenesis 2
reflectseveralprocessesincludingfractionalcrystallization,partial
melting, magma mixing and contamination, which exerted pri-
ThesamplesoftheOrhaneliplutonplotintoquartzmonzonite,
marycontrolonthecrystallizationofmagmaticrocks.
monzonite, granodiorite and diorite fields; Çataldag˘ samples are
In Harker diagrams, samples from the Orhaneli granitoid dis-
represented by granite, syenite and quartz monzonite and Ilıca-
playapeculiarRb–SiO trendthattendstoyieldasomewhatsmall
S(cid:2)amlı samples plot into monzonite and quartz monzonite fields 2
increase.TheincreaseintheRbcontentisduetothereplacement
(Fig.3).Mostofthesamplesareofsub-alkalinecharacterandonly
ofKbyRbinalkalifeldspar,biotiteandamphibole(hornblende).
afewareofalkalinetype.ThediagraminFig.2indicatesthatrocks
The decreasing Sr trend might be explained by a fractionation of
oftheseplutonsarecharacterizedbysimilarandcontinuousmag-
Ca-richplagioclaseasaresultofthereplacementofCabySr.The
maticseries.
negativeBatrendwhichisnotsignificantascomparedwithother
In order to determine aluminum saturation of the Çataldag˘,
plutonsisattributedtobiotitefractionation.Thepeculiarnegative
Ilıca-S(cid:2)amlı and Orhaneli plutonic rocks, A/NK (Al O /Na O+K O)
2 3 2 2 trendinYisduetoamphibolefractionation.
and A/CNK (Al O /CaO+Na O+K O) values were calculated in
2 3 2 2 Samples from the Çataldag˘ granitoid are represented by more
molarbasisandplottedontheManiarandPiccoli(1989)diagram
significant trends in comparison to those of the Orhaneli pluton.
(Fig.4).TheIlıca-S(cid:2)amlıplutonranges0.9,Çataldag˘ plutonranges
Although the course of fractionation process is the same as the
0.8andtheOrhaneliplutonranges0.9.Thewholesamplesofthe
Orhanelipluton,scatteredtrendsintheÇataldag˘samplesareasso-
Ilıca-S(cid:2)amlı pluton are located in the metaluminous field. The
ciatedwiththecrustalcontaminationratherthanfractionation.In
majorityofthesamplesoftheÇataldag˘ andOrhaneliplutonsplot
the chondrite-normalized diagrams all light rare earth elements
showenrichmentpatterns(Fig.6).NegativeEuanomalyissignifi-
cantinalldiagrams.Thisanomalyisrelatedtofractionalcrystalli-
zationofK-feldsparandplagioclaseinfelsicmagmas.
7.1.1.Traceelementandisotopicevidence
Inallthesamplesfromthestudiedplutons,rareearthelements
displayanupward-concaveshape,andheavyREEandMREE(e.g.
Gd, Er) are represented by a relatively depleted trend which is
attributedtotheseparationofamphibole,asamaincrystallization
phase,fromthegranitoidmelt.
The comparison of MORB-normalized values of granitoids to
negativeanomaliesofHFSelements(Ti,Hf,Zr,NbandTa)andnor-
malvaluesofLILEs(Rb,Ba,Th,U,K)showsthatallgranitoidsam-
ples are enriched in LILE elements (Fig. 6). Although negative
anomaliesofNbandotherHFSEelementsmightberelatedtocrus-
tal contamination, theyare the characteristic features of subduc-
tion related magmas, and this arises from relative enrichment of
mantlesourceviaLILEadditionfromsubductingslabtothemantle
(McCullochandGamble,1991).IntheNb–Ydiagram(Pearceetal.,
Fig.3. Totalalkalis(Na2O+K2O)versussilicadiagram(Middlemost,1994).Redline 1984)constructedfortheOrhaneli,Çataldag˘ andIlıca-S(cid:2)amlıgran-
boundarydistinguishesalkalicandsubalkalicrocksaccordingtoIrvineandBaragar
itoidplutons,allsamplesplotintotheVAG(volcanicarcgranites)
(1971).(Forinterpretationofthereferencestocolorinthisfigurelegend,thereader
isreferredtothewebversionofthisarticle.) and Syn-COLG (syn-collisiongranites) fields (Fig. 7a). In the
282 D.Çelebi,N.Köprüba(cid:2)sı/JournalofAsianEarthSciences93(2014)275–287
Fig.5. SelectedHarkervariationdiagramsfortheOrhaneli.Çataldag˘andIlıca-S(cid:2)amlıgranitoidsfromnorthwesternAnatolia.
Rb–Y+Nbdiagram(Pearceetal.,1984),thesamesamplesploton fromatypicalmantlesourceandseemtobeaffectedbyafraction-
volcanicarcgranitesandpost-collisionalfields(Fig.7b). ationprocessratherthancrustalcontamination(Fig.9).Otherplu-
InthediagramproposedbyBatchelorandBowden(1985),the tons, however, are predominantly affected by a crustal
R1andR2valueswerecalculatedandsamplelocationsweredeter- contamination similar to the Early Miocene Aegean volcanics
mined accordingly. In this plot, most of the samples are repre- (Güleç,1991).
sented by a mantle fraction and post-orogenic character (Fig. 8).
The diagram in Fig. 9 was constructed using the data given in 7.1.2.FCandAFC
Table3,andthedatafromgranodioriticrocksoutcroppinginthe Assimilation and fractional crystallization processes are mod-
northwestern Anatolia were also plotted on the same diagram. eledusing(87Sr/86Sr) versusSiO diagram(Fig.10).Thisdiagram
i 2
ThedataoftheAegeanvolcanics,KulabasaltsandBodrumvolcan- highlights significant variation in silica content with limited
ics separated in the diagram are from Altunkaynak et al. (2010), change in Sr isotope ratios, which can best be explained by frac-
and the data of asthenospheric mantle melting and lithospheric tional crystallization of isotopically near-homogeneous magma.
mantle melting are taken from Dilek and Altunkaynak (2007). Thismaysuggestthattheeffectofcontaminationbycrustalrocks
RegardingotherplutonsoutcroppinginthenorthwesternAnatolia, with contrasting isotopic ratios was minimal, and the dominant
the data of Armutlupluton (Köprübasi and Aldanmaz, 2004) and petrologicalprocesswasfractionalcrystallization.
Kapıdag˘andKarabigaplutons(Karacıketal.,2008)werealsoused. Fractionationtrends,whicharetheoreticallypreparedforcrys-
OntheeNd–(87Sr/86Sr) diagram,almostallsamplesarewithin tallization of a certain mineral or mineral assemblage, are com-
i
themantlearray,andexceptforafewsamples,themostsamples pared with proposed trends to examine the role of fractionation
fromthestudiedplutonsplotintotheAegeanvolcanicsfield.Sam- intheevolutionofrocks.Theoreticalfractionationtrendsarecal-
plesfromtheArmutlu,Kapıdag˘ andKarabigaplutonsarederived culated using Rayleigh equation (C/C =F(D(cid:2)1)). Mineral vectors
L 0
D.Çelebi,N.Köprüba(cid:2)sı/JournalofAsianEarthSciences93(2014)275–287 283
Fig.6. (a–c)N-MORB-normalizedmulti-elementpatternsfortheOrhaneli,Çataldag˘andIlıca-S(cid:2)amlıgranitoidsinnorthwesternAnatolia.N-MORBnormalizingvaluesare
fromSunandMcDonough (1989).(d–f) ChondritenormalizedREE patternsfortheOrhaneli. Çataldag˘ andIlıca-S(cid:2)amlıgranitoidsin northwesternAnatolia.Chondrite
normalizingvaluesarefromSunandMcDonough(1989).
Fig.7. Trace-elementdiscriminationdiagramsofthenorthwesternAnatoliangranitoids.(a)NbversusYand(b)RbversusY+NbfieldsarefromPearceetal.(1984).The
shadedareadenotescompositionsofpost-collisiongranitoids.Abbreviations:WPG=within-plategranite;VAG=volcanic-arcgranite;syn-COLG=syn-collisionalgranite;
ORG=ocean-ridgegranite.
284 D.Çelebi,N.Köprüba(cid:2)sı/JournalofAsianEarthSciences93(2014)275–287
Fig.10. (87Sr/86Sr)iversusSiO2diagramforthenorthwesternAnatoliangranitoids
showingtheeffectsoffractionalcrystallizationandAFC.
Fig.8. R1–R2diagramforOrhaneli.Çataldag˘andIlıca-S(cid:2)amlıgranitoidsBatchelor
andBowden(1985).
a single mineral phase cannot be questioned. In Ba–Rb diagram
(Fig.11c), thetheoretically formedmineralassemblageisconsis-
tentwith(plagioclase34%+biotite10%+alkalifeldspar56%).Like
intheY–Srdiagram,itisevidentthatsingle-phasecrystallizationis
noteffective.
In theoretical modeling studies, fractionationwas found to be
an effective process for all pluton samples. In addition, in order
to determine the degree of crustal contamination effect on sam-
ples,Th/YbandNb/Ybratioswereplotted.AlthoughNb/Ybratios
ofsamplesareclosetoN-MORB,Th/Ybratiosaresignificantlyhigh,
indicatinganextremeenrichmentinTh.Theseratiossuggestthat
samples were subjected to notable subduction-zone enrichment,
and therefore, the plutons are believed to be formed by magmas
derivingfromadepletedsourcewithasignificantarccomponent.
ThepositionsofsamplesinFig.12yieldthatÇataldag˘ samplesare
much more affected by subduction-zone enrichment than
Ilıca-S(cid:2)amlı and Orhaneli samples. In addition, it is also clear that
othernorthwesternAnatolianplutonsplottedinthediagramseem
tobelessaffectedbysubduction-zoneenrichmentwithrespectto
studiedplutons(Fig.12).
In Fig. 12, element ratios of E–W extending Armutlu, Kapıdag˘
andLapsekiplutonslocatedinthefarnorthofthestudiedplutons
werealsoplotted.Itisimportanttonotethattheseplutonsarenot
affected by the crustal contamination as much as the Çataldag˘,
Fig.9. (a)eNdversus(87Sr/86Sr)idiagramfornorthwesternAnatoliangranitoids. Ilıca-S(cid:2)amlıandOrhaneliplutons.
ThefieldsforasthenosphericandlithosphericmantlemeltingarefromDilekand Petrographic and geochemical data of the Orhaneli, Çataldag˘
Altunkaynak(2007)Kapıdag˘andKarabigagranitoidsdataaretakenKaraciketal. and Ilıca-S(cid:2)amlı pluton samples show that magma mixing and
(2008).(b)eNd(i)versus(87Sr/86Sr)idiagramfornorthwesternAnatoliangranitoids. assimilation processes played an important role in the develop-
KulaBasaltsandBodrumVolcanicsdataaretakenAltunkaynaketal.(2010).
mentoftheserockgroups.Inordertoexaminethiseffect,thethe-
oretical AFC (Assimilation–Fractional Crystallization) modeling
used in the modeling were constructed using the computer pro- (DePaolo,1981)wastestedusingtraceelementdata.Inthemodel,
gram by Keskin (2002). Fractional crystallization models for the an‘r’valueisusedastheAFCnumericindex.
Ilıca-S(cid:2)amlı,Çataldag˘ andOrhaneligranitoidicrocksareillustrated Models were prepared for correlating the Nd–Sr isotope data
in Fig. 11a–c. with trace element contents (Th, U, Rb). Fig. 13 was drawn to
PetrographicdeterminationsyieldthattheIlıca-S(cid:2)amlı,Çataldag˘ examinetheeffectsofAFCprocessandtoshowthatallofthesam-
and Orhaneli granitoid samples are composed of quartz+alkali plesplotclosetomodeledrvalues.Highvaluesofr,whichisthe
feldspar+plagioclase+amphibole+biotite and titanite and opa- ratioofvaryingcontamination/fractionratio,indicatethatsamples
queminerals.Inordertoexaminefractionalcrystallizationeffects aresignificantlyaffectedbythecontaminationprocess.Inthedia-
onplutons,theserock-formingmineralswereconsideredandmin- gram,samplenoK-93-80ofAlıcıetal.(2002)wasusedastheman-
eral compositions of vectors were also specified which are tle component and the value for crust component is taken from
expressedasmulti-mineralcompositionsusedinconstructedthe- TaylorandMcLennan(1985).Startingandend-membercomposi-
oreticalvectors.ItisshownfromBa–Thdiagramthatallsamples tionsare144Nd/143Nd=0.512773and87Sr/86Sr=0.70349forman-
areaffectedbyalkalifeldsparandplagioclasefractionation;how- tle (Alıcı et al., 2002) and 144Nd/143Nd=0.511994 and
ever,amongthetheoreticallycomputedmineralassemblages,the 87Sr/86Sr=0.711700forcrust(TaylorandMcLennan,1985).
trendof(50%alkalifeldspar+50%plagioclase)yieldsamorecon- In the AFC diagrams constructed based on these results, sam-
sistentresult(Fig.11a). plesarefoundtobemuchmoreaffectedbythecontaminationpro-
IntheY–Srdiagram(Fig.11b),theoreticalmineralassemblage cess. In addition, among the studies carried out for the plutons,
and (plagioclase 56%+amphibole 8%+alkali feldspar 36%) seem Çataldag˘ is the most affected pluton by the contamination and
tobeconsistent.Thatis,inthisdiagram,thecrystallizationofonly theseresultsareconsistentwithdatashowninFig.13.