Turkish Journal of Earth Sciences
Turkish J Earth Sci
(2014) 23: 645-667
© TÜBİTAK
doi:10.3906/yer-1312-7
http://journals.tubitak.gov.tr/earth/
Research Article
Geological, petrological, and geodynamical characteristics of the Karacaali Magmatic
Complex (Kırıkkale) in the Central Anatolian Crystalline Complex, Turkey
1
2,
3
2
Ömer ELİTOK , Şenel ÖZDAMAR *, Gürkan BACAK , Bektaş UZ
Department of Geological Engineering, Faculty of Engineering, Süleyman Demirel University, Isparta, Turkey
2
Department of Geological Engineering, Faculty of Mines, İstanbul Technical University, Ayazağa, İstanbul, Turkey
3
Department of Geological Engineering, Faculty of Engineering, Bülent Ecevit University, Zonguldak, Turkey
1
Received: 09.12.2013
Accepted: 11.07.2014
Published Online: 03.11.2014
Printed: 28.11.2014
Abstract: Mafic and felsic igneous rocks in the Karacaali Magmatic Complex (KMC) in the northwestern margin of the Central Anatolian
Crystalline Complex (CACC) are classified into 4 groups: i) granitoid pluton including granite, granodiorite, and monzonite; ii) a few
meter-scale porphyritic microgranite enclaves within the hybrid rocks; iii) hybrid rocks formed by mixing/mingling of mafic lavas
(basaltic/diabasic/lamprophyric), anorthositic, and/or rhyolitic lavas; iv) diabasic dykes/veins within the granitoid pluton. Major element
composition of the granitoid pluton and porphyritic microgranite enclaves within the hybrid rocks indicate subalkaline, calc-alkaline,
and mostly I-type characteristics. These rocks are mainly peraluminous with aluminum saturation index > 1, but mainly between 1 and
1.1, indicating transitional peraluminous. On the tectonomagmatic discrimination diagrams (Y vs. Nb and (Y+Nb) vs. Rb diagrams),
all the granitic and monzonitic rock suites from the complex fall mostly in the VAG+Syn-COLG and VAG fields respectively, suggesting
arc-related origin. On the R1 vs. R2 tectonic diagram, the granitic rocks display distribution from preplate collision to syncollision field,
but quartz-monzonitic samples plot within the postcollision uplift field. Based on limited geological, petrographic, and geochemical
results, the tectonomagmatic evolution of the KMC can be summarized as follow: i) initiation of subduction of the Inner Tauride
oceanic lithosphere beneath the CACC during the Late Cretaceous time; ii) underplating of partial melts derived from subducted slab
and/or mantle wedge, which provided enough heat for partial melting of the mafic lower crust and generation of granitic magma; iii)
slab detachment following the continent–continent collision that resulted in tensional forces within the overlying continental crust,
which allowed the intrusion of the granitic magma to the upper crust, also cutting the central Anatolian ophiolites, from the Late
Cretaceous to most likely the Paleocene time. The hybrid rocks formed by mixing/mingling of the mafic, anorthositic, and/or rhyolitic
magmas most likely indicate their injection into a partly crystalline granitic magmatic system just after crystallization of granitic magma
in the upper crust. However, this model is open to discussion and needs to be investigated using isotope data in future studies.
Key words: Granite, lamprophyre, mantle, Karacaali, Central Anatolian Crystalline Complex
1. Introduction
Granitoids may develop in different tectonic settings and
can be used as a geodynamic indicator only when correctly
typed and precisely dated (Barbarin, 1999; Bonin, 2007).
They can also be accompanied with mafic to intermediate
inclusions that resulted from late-stage injections of these
magma types in the early stages of the crystallization of
host felsic magma (Macdonald et al., 1986; Sheppard, 1995;
Atherton and Ghani, 2002; Awdankiewicz, 2007; Wang et
al., 2007; Prabhakar et al., 2009). In this case, chemically
and mechanically wide ranges of interactions arise between
the contrasting (felsic and mafic) magmas, including
mingling and/or mixing processes. The association of
mafic mantle-derived melts with granitoids has significant
importance in understanding crust–mantle interactions
*Correspondence: ozdamarse@itu.edu.tr
and tectonothermal activities at deep lithospheric levels.
The Central Anatolian Crystalline Complex (CACC;
Yalınız et al., 1996, 2000b; Düzgören-Aydın et al., 2001;
Whitney et al., 2001; Kadıoğlu et al., 2006), a triangularshaped continental fragment bounded by the Inner
Tauride Suture Zone (ITSZ) in the south and the İzmirAnkara-Erzincan Suture Zone (IAESZ) in the north,
comprises an assemblage of tectonic blocks represented
by the Paleozoic-Mesozoic metamorphic rocks (from
north to south, the Kırşehir, the Akdağ, and the Niğde
Massifs), dismembered suprasubduction zone-type (SSZtype) Tethyan ophiolites (Yalınız et al., 1996, 2000a, 2000c;
Yalınız and Göncüoğlu, 1998), and felsic to mafic plutons
that intruded into those of the metamorphic massifs and
ophiolitic rock assemblages (Whitney and Dilek, 1997;
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Görür et al., 1998; Yalınız and Göncüoğlu, 1998; Dilek
and Whitney, 2000; Yalınız et al., 2000a, 2000c; Clark
and Robertson, 2005) (Figure 1). Granitoids are also
associated with hybrid rocks formed by mingling/
mixing of mafic to felsic igneous rocks in the CACC
(Kadıoğlu and Güleç, 1996; Delibaş et al., 2011).
Tectonomagmatic evolution of the central Anatolian
region is closely related to pre- to postcollisional
geodynamic processes, especially including closure
of the northern Neotethyan ocean, crust–mantle
interactions, and lithospheric scale tectonic events, as
well as the eastern and western parts of Turkey.
The Karacaali Magmatic Complex (KMC) in the
northwestern edge of the CACC includes mafic to felsic
igneous rocks and hybrid rocks formed by mingling/
mixing of these magmas. In this paper, it is aimed
to i) review the geology of the Karacaali Magmatic
Complex, ii) present petrographic and geochemical
characteristics of the igneous rocks, and iii) discuss
the relation of mafic igneous rocks associated with the
granitoid pluton.
2. Geological background
Turkey is a segment of the Alpine-Himalayan orogenic belt
and consists mainly of an amalgamation of Gondwanaderived microcontinents (Şengör and Yılmaz, 1981;
Robertson and Dixon, 1984). Main continental collision
zones in Turkey are represented by various suture zones:
the IAESZ, ITSZ, and Bitlis-Zagros Suture Zone (BZSZ),
signifying the collision of the microcontinents. Based on
the present-day deformational structures, Turkey was
separated into 4 distinct tectonic provinces, namely the
East Anatolian Contractional Province and the North
Anatolian, Central Anatolian ‘Ova’, and West Anatolian
Extensional Provinces (e.g., Bozkurt, 2001). The Central
Anatolian ‘Ova’ Province includes Central Anatolian
sedimentary basins (e.g., the Haymana, Tuzgölü, Ulukışla,
Kızılırmak, Çankırı-Çorum, and Sivas basins) and rock
associations of the CACC including mainly igneous
rocks (namely a large number of disconnected granitic/
syenitic plutons with their volcanic associations),
Gondwana-derived crustal blocks (namely the Kırşehir,
Akdağ, and Niğde metamorphic massifs), and ophiolitic
Figure 1. Simplified geological map of central Anatolia (Turkey) (from Kadıoğlu et al., 2003; inset map from
Bozkurt, 2001).
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rock assemblages (Göncüoğlu et al., 1991). The Late
Mesozoic-Early Cenozoic evolution of the CACC
involves episodes of obduction of Tethyan ophiolites,
deformation, metamorphism, and magmatism associated
with contraction and collision along its boundaries
(Göncüoğlu et al., 1991; Koçak and Leake, 1994; Yalınız
et al., 1996, 1999, 2000a, 2000b; Whitney and Dilek,
2001; Kocak et al., 2005; Kadıoğlu et al., 2006; Özdamar
et al., 2012; Özdamar et al., 2013; Pourteau et al., 2013).
Discontinuous exposures of the Tethyan ophiolites
define 2 major suture zones surrounding the CACC, the
IAESZ in the north and the ITSZ in the south (Şengör
and Yılmaz, 1981; Robertson and Dixon, 1984; Dilek
and Moores, 1990; Dilek et al., 1999; Kadıoğlu et al.,
2006; Toksoy-Köksal et al., 2009; Lefebvre et al., 2013).
The metamorphic massifs and also the tectonically
overlying SSZ-type ophiolites emplaced between the
Early Santonian and Early Maastrichtian (Yalınız and
Göncüoğlu, 1998) are intruded by calc-alkaline and
alkaline plutons (Whitney and Dilek, 1997; Görür et al.,
1998; Yalınız and Göncüoğlu, 1998; Boztuğ, 2000; Dilek
and Whitney, 2000; Yalınız et al., 2000a, 2000c; Köksal et
al., 2001; Kuşcu et al., 2002; İlbeyli et al., 2004; Clark and
Robertson, 2005; Tatar and Boztuğ, 2005; Önal et al., 2005;
Kadıoğlu et al., 2006; Boztuğ and Jonckheere, 2007; Boztuğ
et al., 2007a, 2007b, 2008, 2009). The contact relations
between the central Anatolian ophiolites and granitoids
are characterized by the occurrence of chilled margins
and contact metamorphism, suggesting intrusive contact
relation and intrusion of granitoids later than ophiolite
emplacement (Yalınız and Göncüoğlu, 1998; Floyd et
al., 2000; Köksal and Göncüoğlu, 2008 and references
therein). Based on petrological characteristics, intrusive
rock types in the CACC were classified as: i) calc-alkaline,
ii) subalkaline-transitional, and iii) alkaline in similar
age (İlbeyli et al., 2004, 2009) or S-type, I-type, A-type,
and H-type (Köksal et al., 2008). Conversely, based on
40
Ar/39Ar ages of the granite to syenite supersuite rocks,
Kadıoğlu et al. (2006) suggested evolution of the CACC
magmatism from calc-alkaline to alkaline composition
with time. They also proposed a magmatic zonation for
the western edge of the CACC such that granitic plutons
mainly occur along the western edge of the CACC,
whereas syenitic plutons form smaller bodies that crop
out in the inner part. Düzgören-Aydın et al. (2001) stated
that the nature of magmatism in central Anatolia varies
through time from peraluminous to metaluminous to
alkaline. They concluded that these different magma
types reflect distinct stages of postcollisional magmatism
including various crust–mantle interactions. The complex
is covered with the Cenozoic sedimentary basins and
volcanic units. The evolution of these basins is subject to
debates about the fore-arc basin, back-arc basin, island
arc-related basin, and rift-related basin (Alpaslan et
al., 2006 and references therein). The central Anatolian
basins have been divided into 2 basic types: arc-related
(fore-arc and intra-arc) basins and collision-related
(peripheral foreland) basins (Görür et al., 1998; Gürer
and Aldanmaz, 2002 and references therein). It was also
suggested that the Kırıkkale basin was in an intra-arc
position during the Late Cretaceous to Eocene time.
3. Karacaali Magmatic Complex and surrounding units
The Karacaali Magmatic Complex, located to the
northwestern margin of the CACC, consists mainly of
felsic to mafic igneous rocks. Delibaş et al. (2011) mapped
a large area of the KMC and reported that the complex
includes plutonic (e.g., gabbro, monzonite, porphyritic
quartz-monzonite, fine-grained granite, and porphyritic
leucogranite) and volcanic (e.g., basalt, andesite, and
rhyodacite to rhyolite) associations. In this study, some
part of the complex has been mapped in detail (Figure
2). In the study area, mainly i) granitoid pluton including
granite, granodiorite, and quartz-monzonite; ii) hybrid
rocks formed by mingling/mixing of mafic (basaltic/
lamprophyric), anorthositic, and/or rhyolitic lavas; and
iii) a few meter-scale porphyritic microgranite enclaves
within the hybrid lavas were distinguished (Figure 3a).
However, it is not possible to show the contact relation of
these hybrid rock types in the geological map. Moreover,
granitoid pluton is cut by diabasic dyke/veins (Figure
3b) and aplitic dykes typically thinner than 50 cm. The
KMC contains iron, copper-molybdenum and lead
mineralizations (Delibaş and Genç, 2004, 2012; Delibaş
et al., 2011). To the western and northwestern sides of
the city of Kırıkkale, the Karacaali pluton intrudes the
Late Cretaceous mélange units and the Late Cretaceous
volcanoclastics (Koç and Kaya, 2002; Akıncı, 2008; Özer
et al., 2011). The Paleocene (the Dizilitaş Formation) and
the Eocene clastic sedimentary units (the Bulanıkdere,
the Karagüney, the Mahmutlar formations) overlie the
Late Cretaceous units, which are intruded by plutonic
rocks (Akıncı, 2008). The Upper Eocene ends with
nummulitic limestones, sandy-silty limestones, and
fine- to coarse-grained volcanogenic detrital deposits
(Akıncı, 2008). Clastic materials derived from quartzporphyry and granitoids widely occur within the basal
conglomerates of the Eocene units, suggesting preEocene exhumation of the granitoids in the study area
(Delibaş and Genç, 2004). Oligo-Miocene evaporitic
deposits, fine- to coarse-grained reddish volcanogenic
materials rest unconformably on the older magmatic
and detrital deposits (Akıncı, 2008). S-type, high-K calcalkaline Danacıobası biotite leucogranite (Behrekdağ
batholith) outcrops to the south of the city of Kırıkkale
(Tatar and Boztuğ, 2005).
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Figure 2. a) Geological map of the Karacaali Magmatic Complex in the NW Central
Anatolian Crystalline Complex, b) geological cross-section showing field relations of
the granitoid pluton and hybrid rocks.
4. Petrography
Igneous rocks in the study area consist mainly of i)
granitoid pluton including granite, granodiorite, and
monzonitic rocks; ii) a few meter-scale porphyritic
microgranite enclaves within the hybrid rocks; iii) hybrid
rocks formed by mixing/mingling of mafic (basaltic/
lamprophyric), anorthositic, and/or rhyolitic lavas; and
iv) diabasic dykes/veins within the granitoid pluton. The
granitic rocks of the pluton are mainly characterized by
equigranular to porphyritic texture and contain mainly
quartz, orthoclase, plagioclase, hornblende, biotite,
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augite, sphene, and opaque minerals. Orthoclase includes
quartz and plagioclase inclusions (Figures 4a and 4b),
and hornblende crystals are also included in some sphene
minerals. Some plagioclase minerals have embayed
grain margins and they can occur as inclusions in biotite
minerals and vice versa. Tiny biotite and opaque mineral
grains are found at the core of plagioclase minerals and
intracrystalline melting is observed around the cluster
of these tiny inclusions. Biotites, in places, are altered to
chlorite and they also occur as inclusions in amphiboles.
Augite minerals are colorless and they can be observed as
ELİTOK et al. / Turkish J Earth Sci
Figure 3. a) Porphyritic microgranite enclave within the hybrid rocks.
b) Diabasic vein/dykes in the altered granitoid pluton.
inclusions in plagioclase minerals. Accessory minerals are
mainly sphene, and opaque minerals that are surrounded in
turn by biotite and/or hornblende. Feldspars are replaced,
in places, with sericite and epidote. Some coarse-grained
granitic rocks include microcrystalline/microlitic feldspar
and amphibole minerals. Feldspar and quartz minerals
surrounded by microlitic crystals are corroded along
their margins and also intracrystalline melting appears in
feldspar minerals.
Porphyritic microgranite enclaves in hybrid rocks
display holocrystalline porphyritic texture with quartz
and plagioclase phenocrystals, which are mainly corroded
along their margins by the matrix phase (Figure 4c). Quartz
minerals are in euhedral to anhedral forms, and plagioclase
minerals may be included in quartz minerals. Some quartz
minerals are covered by thin opaque zones along their
margins. Some feldspar minerals are altered to epidote
and the matrix phase in places to chlorite and calcite.
Additionally, intricate intergrowths in which the quartz
forms irregular patches in the orthoclase and plagioclase
crystals are observed (Figure 4d). This suggests rapid and
simultaneous crystallization of quartz and feldspar from the
residual melt (Nagudi et al., 2003 and references therein).
Phenocryst accumulations with microlitic amphiboles and
tiny opaque grains, and also microscale lamprophyric lava
injections, are present as veins in the matrix phase (Figure
4e). On the other hand, microscale plutonic rock fragments
consisting mainly of coarse-grained feldspar and epidote
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Figure 4. Thin-section photomicrographs showing a) quartz inclusions in orthoclase, b) plagioclase inclusion in orthoclase,
c) quartz and plagioclase phenocrysts in fine-grained matrix, d) granophyric intergrowths of quartz with feldspars in the
porphyritic microgranite enclave, e) feldspar phenocrysts with tiny opaque grains and thin lamprophyric lava injections in the
matrix phase of the porphyritic microgranite enclave, f) epidotes as partly embayed grains within feldspar laths and vice versa.
Epd: Epidote, Lmp: lamprophyre, M: matrix Opq: opaque, Ort: orthoclase, Pl: plagioclase, Q: quartz.
crystal occur in the matrix of the porphyritic microgranite
enclaves. Anhedral epidotes are present as partly embayed
grains within feldspar laths, presumably magmatic epidote
(Figure 4f). Zen and Hammarstrom (1984) suggested
650
that plutonic rocks bearing magmatic epidote must have
formed under moderately high pressures (pressures of at
least 8 kbar), corresponding to lower crustal depths, under
fairly oxidizing conditions.
ELİTOK et al. / Turkish J Earth Sci
Petrographically, hybrid rocks display heterogeneous
compositions characterized by mingling/mixing of mafic
(basaltic/lamprophyric), anorthositic, and/or rhyolitic
lavas. The quartz-poor hybrid rocks have heterogeneous
compositions. Some of them are plagioclase-dominated
with microlitic feldspar minerals, plagioclase phenocrysts,
and lesser amounts of actinolitic amphiboles (approximately
10%–15%) showing flow texture. Actinolitic amphiboles
are mainly in small prismatic forms and display light
green pleochroism. In these rocks, plagioclase minerals
are mainly corroded along their margins and, in places,
altered to chlorite. Actinolitic amphiboles are also present
within the corroded plagioclase minerals. Additionally,
rounded-subrounded ocelli features filled with small
actinolitic amphiboles exist within the matrix phase.
Some of these rocks have 2 portions. One side has
a composition of spessartite lamprophyre with high
amounts of actinolitic amphiboles and the other side
has an anorthositic composition consisting mainly of
plagioclase crystals of various sizes (Figure 5a). The
boundary between these 2 portions is either sharp or
irregular. In these rocks, plagioclase minerals are mainly
corroded along their margins and actinolitic amphiboles
are also present within the corroded plagioclase minerals
(Figure 5b). Rounded-subrounded globular structures
(ocelli) filled with actinolitic amphiboles may exist in
plagioclase-rich or actinolite-rich areas in the rocks
(Figure 5c). The groundmass in the ocellus is made of
actinolite amphiboles. Koç and Kaya (2002) asserted that
hydrothermal alteration resulted in alteration of pyroxenes
in basaltic and diabasic rocks to actinolite. Some hybrid
rocks are characterized by spessartite-type lamprophyric
lava dominated by amphibole minerals with globular
structure (Figure 5d). Ocellar features are interpreted to
represent late-stage magmatic segregation or magmatic
crystallization including 2 immiscible magmatic liquids
(e.g., İbrahim et al., 2010).
Quartz-rich hybrid rocks are characterized mainly
by 3 different heterogeneous compositions: mafic (mixed
basaltic/lamprophyric), anorthositic, and rhyolitic
compositions (Figure 5e). Flow texture can be seen in
the anorthositic portion with microlitic and phenocrystal
plagioclases. The rhyolitic portion of the rock is mainly
composed of microcrystalline quartz. Some quartz-rich
hybrid rocks display holocrystalline porphyritic texture
and plagioclase minerals corroded especially along
their margins form the phenocryst phase. Plagioclase
phenocrysts in anorthositic composition may be corroded
during mingling processes with the mafic lavas (Figure
5f). Intracrystalline melting can be observed within the
plagioclase minerals and small actinolite crystals may
occur in the melted areas (Figure 5g). In places, fineto medium-grained quartz-rich areas are observed in
the rock. Small actinolitic amphiboles exist in the rock
and some of them are partially altered to chlorite. Some
plagioclase minerals display a sieve texture along their
margins (Figure 5h).
Diabase samples taken from the dike or vein intruding
into the granitoid pluton are composed mainly of microlitic
plagioclase, scattered small-sized anhedral opaque
minerals, small-sized anhedral pyroxene minerals that are
colorless in plane polarized light, and a microcrystalline
matrix of these crystals.
5. Geochemistry
5.1. Sampling and analytical procedures
After petrographic investigation, 25 representative
rock samples were selected for geochemical analyses.
Geochemical analyses including major and trace element
analyses were conducted at the ACME Analytical
Laboratories in Canada. Total abundances of the major
oxides and several minor elements are reported for a 0.2g sample analyzed by inductively coupled plasma-atomic
emission spectroscopy, following a lithium metaborate/
tetraborate fusion and dilute nitric digestion. Loss on
ignition (LOI) is by weight difference after ignition at 1000
°C. Rare earth and refractory elements were determined
by inductively coupled plasma-mass spectrometry (ICPMS) following a lithium metaborate/tetraborate fusion
and nitric acid digestion of a 0.2-g sample. In addition, a
separate 0.5-g split was digested in aqua regia and analyzed
by ICP-MS to report the precious and base metals. The
chemical compositions of major, minor, and trace element
contents of the granitoid and hybrid rocks are presented
in the Table.
5.2. Granitoids and associated mafic rocks
On the total alkali vs. SiO2 and AFM diagrams, all the
granitic rock suites of the KMC define subalkaline and
calc-alkaline trends, respectively (Figures 6a and 6b).
On the normative Q-ANOR classification diagram by
Streckeisen and Le Maitre (1979), the rock assemblages
of the granitoid pluton plot within the monzogranite
and granodiorite field and the porphyritic microgranite
enclaves within the hybrid rocks compositionally scatter
from the granodiorite to tonalite field (Figure 7).
Major element contents of the granitoid suite from
granitic to monzonitic composition vary between 60 and
83.1 wt.% for SiO2, 0.11 and 0.45 wt.% for TiO2, 0.09 and
4.96 wt.% for CaO, and 0.7 and 4.48 wt.% for K2O. On the
primitive mantle-normalized trace element diagram, the
granitoid pluton displays enrichment in large-ion lithophile
elements (LILEs; Cs, Rb, K, Ba, Pb) with a relatively slightly
negative anomaly in Ba, and also enrichment in some high
field strength elements (HFSEs; U, Th) (Figure 8a). They
also show strong negative anomalies in Nb, Ta, and Ti and
variable negative Sr anomalies in some samples. Rb, Ba,
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Figure 5. a) Lamprophyric composition with high amount of actinolitic amphiboles and anorthositic composition with mostly plagioclase crystals in
various sizes. b) Corroded plagioclase minerals along their margins and actinolitic amphiboles within the corroded plagioclase minerals. c) Roundedsubrounded globular structures (ocelli) filled with actinolitic amphiboles. d) Spessartite-type lamprophyric magma with ocelli structure. e) Quartz-rich
hybrid rock with mafic, rhyolitic, and anorthositic lavas. f) Intracrystalline melting within the plagioclase minerals and small actinolite crystals in
the melted areas. g) Plagioclase minerals displaying mixing texture along their margins characterized by intracrystalline melting and small mineral
inclusions. h) Feldspar minerals intergrown with the sphene minerals. Act: Actinolite, Anor: anorthosite, Oc: ocelli, Sph: sphene, Lmp: lamprophyre, Pl:
plagioclase, Rhy: rhyolite.
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Table. Major, minor, and trace element contents of the selected samples from the Karacaali Magmatic Complex.
Sample no,
KR-1
KR-29
Rock type
Granitoid pluton
N11A
N-7
KR-3
KR-10A KR-10B KR-13
KR-17
KR-22
KR-23
N-14
Q-monz Porphyritic microgranite enclave
Major oxides (wt.%)
SiO2
66.6
83.1
74.7
60
63.2
75.1
75.9
76.3
78.5
79.4
68.7
76.7
TiO2
0.33
0.13
0.11
0.45
0.36
0.26
0.24
0.23
0.07
0.1
0.55
0.2
Al2O3
14.7
9.7
12.2
15.9
15.45
12.4
11.85
11.5
10.6
11.25
15.1
10.65
Fe2O3
4.15
1.06
1.3
7.81
4.95
2.22
2.18
2.77
1.32
0.53
2.57
2.16
MnO
0.07
0.02
0.02
0.19
0.07
0.05
0.05
0.07
0.03
0.005
0.05
0.03
MgO
1.34
0.25
0.49
2.28
1.77
0.73
0.7
0.61
0.16
0.99
1.66
0.63
CaO
3.63
0.09
1.27
4.96
4.44
1.02
0.99
1.12
0.12
0.2
2.6
0.95
Na2O
2.74
0.1
4.88
3.67
2.85
6.28
6.01
5.42
1.44
5.33
5.09
5.13
K2O
4.48
2.2
0.7
3.31
4.11
0.12
0.11
0.18
5.34
0.3
0.9
0.08
P2O5
0.10
0.02
0.005
0.2
0.13
0.04
0.02
0.03
0.02
0.005
0.08
0.05
LOI
0.5
3.48
1
1.23
1.3
1.6
1.5
1.36
1.06
1.36
2.05
0.94
SUM
98.8
100
96.7
99.72
98.9
99.8
99.6
99.6
98.7
99.5
99.4
97.53
Trace elements (ppm)
Ba
1035
373
115
1055
1585
21.8
24.3
43.2
259
15.2
78.6
26.4
Sr
292
73.7
106
345
357
43.4
41.8
52.8
39.4
41.2
127
68
Rb
165.5
89.3
18.5
106
112
3.7
3.3
7.2
185
14
32
1.4
Cs
6.63
4.05
1.35
6.31
3.98
2.14
1.93
1.3
4.09
1.01
14.4
0.6
Th
34.7
14.5
3.71
19.1
24.6
0.75
0.76
0.61
28
1.16
1.07
1.77
U
4.97
3.16
0.86
3.65
2.66
0.26
0.24
0.2
5.71
0.32
0.32
0.49
Co
8.2
1.5
2.4
13.7
8.5
2.1
2
5.4
2.3
0.8
3
4.8
Zr
115
114
97
189
102
79
77
75
80
142
108
73
Y
14.2
13.4
22.9
18.3
15.1
31.8
31.6
22.2
18.3
62.6
33.9
26.5
V
66
12
8
142
81
10
8
12
2.5
2.5
37
23
Ga
12.7
9.7
11.1
15.2
13.6
11.7
10.9
11.5
9.6
10.9
14.5
7.6
Hf
3.2
3.4
4.2
4.9
2.8
2.6
2.6
2.6
2.7
4.6
3.4
2.3
Nb
9.5
6.3
1.9
6.8
8
1.4
1.4
1.2
10.4
2.6
2.2
1.6
Ta
0.8
0.6
0.2
0.5
0.7
0.1
0.1
0.1
1.4
0.2
0.1
0.1
Zn
51
112
25
102
44
27
27
46
30
16
66
22
Cu
103
6
10
36
16
21
11
16
14
2.5
2.5
34
Ag
0.5
0.5
0.05
0.5
0.5
0.5
0.5
0.5
0.5
0.5
0.5
0.5
W
1
2
6
2
1
0.5
0.5
1
3
1
1
0.5
Mo
1
5
1
1
1
1
1
1
1
1
1
1
Pb
29
17
7
56
24
9
9
15
64
2.5
34
10
Sn
1
2
1
2
1
0.5
0.5
0.5
4
1
1
1
Ni
5
17
2.5
17
2.5
12
5
2.5
2.5
2.5
2.5
5
Cr
10
20
5
30
10
10
10
10
5
5
10
10
Rare earth elements (ppm)
La
32.1
24.9
10
31.8
23.9
2.7
2.5
2.0
34.5
2.7
5.7
6.7
Ce
53.5
42.9
28.6
58.8
42.6
7.0
6.6
5.6
58.5
7
15
15.7
653
ELİTOK et al. / Turkish J Earth Sci
Table. (Continued).
Pr
5.4
4.46
3.7
6.18
4.57
1.15
1.09
0.93
5.78
1.35
2.34
2.16
Nd
18
15.1
16.1
20.8
16.3
6.3
5.8
5.1
17
7.3
11.9
9.3
Sm
3.12
2.59
3.95
3.94
3.07
2.33
2.17
1.81
2.9
3.51
3.77
2.67
Eu
0.79
0.41
0.29
1.13
0.95
0.69
0.64
0.41
0.15
0.97
1.23
0.49
Gd
3.25
2.67
3.68
3.54
3.12
3.6
3.49
2.64
2.52
6.38
4.79
3.42
Tb
0.46
0.38
0.55
0.52
0.47
0.74
0.74
0.53
0.41
1.45
0.89
0.61
Dy
2.47
2.16
3.65
3.26
2.65
5.33
5.2
3.78
2.72
10.5
5.95
4.32
Ho
0.48
0.47
0.78
0.64
0.53
1.18
1.18
0.86
0.57
2.36
1.27
0.94
Er
1.59
1.5
2.57
1.88
1.65
3.64
3.73
2.83
1.88
7.4
3.92
2.92
Tm
0.22
0.23
0.46
0.3
0.22
0.56
0.56
0.43
0.33
1.1
0.56
0.48
Yb
1.68
1.64
3.35
1.93
1.67
3.87
3.77
3.1
2.41
7.5
3.92
3.21
Lu
0.26
0.25
0.61
0.3
0.26
0.59
0.57
0.51
0.39
1.14
0.58
0.54
ACNK
0.92
3.58
1.1
0.85
0.9
1.01
1
1.03
1.27
1.19
1.07
1.04
(La/Sm)n
6.64
6.21
1.63
5.21
5.03
0.75
0.74
0.71
7.75
0.5
0.98
1.62
Eu/Eu
0.75
0.47
0.5
0.91
0.93
0.73
0.71
0.57
0.17
0.62
0.88
0.85
Mg num
39.31
32.11
43.05
36.93
41.77
39.74
39.17
30.64
19.56
78.93
56.44
36.91
*
Table. (Continued).
Sample no, KR8A KR9
Rock type
KR11 KR12 KR14 KR8B
Q-poor hybrid rocks
KR15
KR19
KR4
KR20
N11L
N21
N22B
Q-rich hybrid rocks
Mafic hybrid rocks
Diabasic dyke
Anorthosite
intruding granite
Major oxides (wt.%)
SiO2
50.9
55.4
52.2
51.2
51.8
63.4
57.0
61.0
49
44.1
43.1
49.9
49.4
TiO2
0.47
0.83
0.56
0.51
0.71
0.43
0.57
0.57
0.9
0.73
0.84
0.8
1.73
Al2O3
13.85
17.05
16.9
16.5
17.4
16.1
20.1
18.25
18.25
16.05
19.65
14.15
14.9
Fe2O3
9.54
7.3
7.72
7.57
10
6.35
6.54
6.43
11.7
14.7
14.3
11.15
12.9
MnO
0.29
0.14
0.32
0.25
0.23
0.06
0.09
0.08
0.16
0.27
0.15
0.16
0.18
MgO
9.98
4.75
7.82
8.32
5.74
1.88
3.16
2.77
5.87
7.7
3.65
3.98
4.92
CaO
9.51
3.58
6.8
9.72
6.34
4.21
1.29
1.78
10.9
12.25
13.3
3.28
2.75
Na2O
2.46
6.24
4.08
2.78
4.16
4.74
3.41
4.01
2.64
1.02
1.27
4.72
4.54
K2O
0.12
0.24
1.14
0.54
0.62
0.75
1.04
3.28
2.33
0.19
0.5
0.11
0.38
P2O5
0.02
0.09
0.02
0.04
0.06
0.16
0.04
0.06
0.04
0.06
0.1
0.12
0.21
LOI
3.12
2.43
2.88
2.62
2.38
2.14
3.19
2.4
2.21
2.22
2.18
6.08
6.63
SUM
100.47 98.98
99.88
99.6
99.6
100.58 98.7
99.7
101.9
99.7
98.7
94.74
98.29
Trace elements (ppm)
Ba
28
103.5
115.5
135
83.4
232
294
143.5
65
70.6
39.4
41.9
27.6
Sr
121
136
183
235
144.5
324
99.2
96.1
167
269
333
101
91.6
Rb
6.7
40.8
16.8
16.5
23
48.1
48
29.6
4.2
14.3
3.8
9.6
2.2
Cs
4.13
5.02
6.18
6.33
12.95
9.75
3.9
4.27
1.93
4.32
5.66
4.52
1.51
Th
0.09
0.32
0.42
0.1
0.21
25
1.17
0.8
0.52
3.68
3.69
0.65
0.17
U
0.22
0.19
0.1
0.05
0.13
3.32
0.08
0.06
0.27
0.59
1.54
0.16
0.06
Co
24.9
12.2
28.4
19.4
7.6
7.4
6.5
4.2
12.4
19
29.3
32.5
33.2
Zr
23
65
31
23
39
115
161
108
36
33
62
29
40
654
ELİTOK et al. / Turkish J Earth Sci
Table. (Continued).
Y
15.5
24.4
15.9
11.5
23
25.7
41.9
27.6
21.5
16.5
26.2
14
20.7
V
256
363
278
232
313
141
45
24
457
281
392
330
403
Ga
11.8
18.9
14.9
12.3
14.3
15.5
24.3
15.6
15.7
15.1
18.6
14.6
16.4
Hf
0.7
1.9
1
0.8
1.2
3.1
4.8
3.3
1.2
1.1
1.9
0.9
1.2
Nb
0.4
1.4
0.8
0.4
1.1
10.6
4.4
2.9
1.2
1.8
3.8
0.8
0.8
Ta
0.05
0.1
0.05
0.05
0.1
0.8
0.3
0.2
0.1
0.1
0.3
0.1
0.1
Zn
113
84
163
98
95
43
115
48
96
95
70
88
147
Cu
45
29
81
111
24
15
2.5
2.5
30
47
14
26
10
Ag
0.05
0.05
0.05
0.5
0.5
0.05
0.5
0.5
0.05
0.5
0.05
0.05
0.05
W
1
1
2
1
0.5
1
0.5
0.5
1
1
3
0.05
0.05
Mo
1
1
1
1
1
1
1
1
1
2
1
1
1
Pb
17
47
55
16
12
21
6
7
25
14
11
5
8
Sn
1
1
1
1
1
2
2
1
1
1
2
1
1
Ni
113
21
31
29
14
11
17
9
34
29
24
7
7
Cr
560
40
50
40
10
10
10
10
20
40
50
10
10
Rare earth elements (ppm)
La
0.9
2.9
1.50
0.9
0.7
32.4
8.3
5.4
3.8
4.8
16.7
2.2
1.6
Ce
2.8
7.5
4.5
2.8
1.9
56.5
20
13.9
9.8
9.9
35.1
5.4
5.3
Pr
0.63
1.21
0.77
0.52
0.38
6.32
3.39
2.09
1.65
1.34
4.51
0.82
0.97
Nd
4
6
4.2
3.1
2.5
22.3
17.5
10.7
8
5.9
17.7
4.1
5.4
Sm
1.91
2.05
1.61
1.12
1.31
4.82
5.57
3.4
2.56
1.8
4.19
1.37
2.05
Eu
0.74
0.66
0.75
0.5
0.53
1.2
1.96
1.17
1.19
0.65
1.28
0.6
0.89
Gd
2.76
3.09
2.33
1.59
2.54
4.77
7.12
4.3
3.3
2.35
4.52
2.04
2.96
Tb
0.45
0.58
0.41
0.32
0.55
0.72
1.39
0.83
0.56
0.46
0.7
0.36
0.52
Dy
2.9
4.01
2.84
2.16
4
4.48
8.89
5.47
3.72
3.05
4.37
2.45
3.58
Ho
0.58
0.87
0.59
0.46
0.88
0.88
1.83
1.17
0.78
0.65
0.88
0.53
0.73
Er
1.65
2.6
1.69
3.73
2.73
2.56
5.41
3.55
2.27
1.87
2.59
1.54
2.17
Tm
0.23
0.41
0.26
0.19
0.38
0.38
0.76
0.51
0.34
0.27
0.4
0.24
0.34
Yb
1.56
2.59
1.63
1.29
2.77
2.32
5.38
3.59
2.07
1.71
2.48
1.6
1.96
Lu
0.24
0.41
0.26
0.19
0.41
0.36
0.81
0.53
0.33
0.26
0.41
0.26
0.32
(La/Sm)n
0.3
0.91
0.72
0.52
0.34
4.34
0.96
1.03
0.96
1.72
2.57
1.04
0.5
Eu/Eu*
0.98
0.8
1.18
1.15
0.87
0.76
0.95
0.94
1.25
0.97
1.45
1.49
1.52
Mg num
67.72
56.62
67.02
68.79
53.12
37.26
49.22
46.35
50.16
51.23
33.86
41.72
43.34
and Sr are LILEs and are present in major mineral phases
such as feldspars and micas, and their behavior can be
used to model the role of these minerals in the evolution
of granite magmas (e.g., Leite et al., 2006). During normal
granite magma fractionation, Sr is usually the first to have
compatible behavior as a result of plagioclase removal,
and it is commonly followed by Ba that is taken up by
K-feldspar (Leite et al., 2006). Presumably, significant Sr
and Ba depletion resulted from a larger degree of feldspar
fractionation, since it is the main repository phase for Sr
and Ba. Positive Pb anomaly is a common features of all
rock suites in the study area. The rare earth element (REE)
distribution of the granitoid pluton shows moderately
fractionated REE patterns with (La/Sm)N ratios of 1.63–
6.64 and variable negative Eu anomalies with Eu/Eu* =
0.47–0.91, indicating plagioclase fractionation (Figure 8b).
The porphyritic microgranite enclaves in this group
are mainly characterized by higher SiO2 contents (63.2–
79.4 wt.%) but lower K2O content (0.08–0.9 wt.%)
corresponding to tonalitic composition, except for
655
ELİTOK et al. / Turkish J Earth Sci
Figure 6. Karacaali Magmatic Complex rock suites in a) (K2O+Na2O) vs. SiO2 diagrams and b) AFM diagrams. The line
separating the alkaline and calc-alkaline fields in a) is from Irvine and Baragar (1971).
Figure 7. Q’-ANOR classification (Streckeisen and Le Maitre, 1979) of the analyzed
samples of the KMC.
KR3 and KR17 with K2O of 4.11 wt.% and 5.34 wt.%,
respectively. They have low MgO (0.16–1.77 wt.%) and
low to moderate CaO contents (0.12–4.44 wt.%). The
aluminum saturation index [ASI = mol Al2O3 / (CaO +
Na2O + K2O)] of the granitoid pluton and porphyritic
microgranite enclaves ranges from 0.92 to 3.58 but the
656
porphyritic microgranite enclaves are mostly between
1 and 1.1 (transitional peraluminous). On the primitive
mantle-normalized trace element diagram, porphyritic
microgranite enclaves display subparallel trace element
patterns to the rock assemblages of the granitoid pluton.
In this diagram, the porphyritic microgranite enclaves are
ELİTOK et al. / Turkish J Earth Sci
Figure 8. Primitive mantle-normalized trace element variation and chondrite-normalized REE variation diagrams for the granitoid pluton (a, b),
porphyritic microgranite enclave in hybrid rocks (c, d), quartz-poor hybrid rocks (e, f), quartz-rich hybrid rocks (g, h), diabasic vein/dyke and mafic
hybrid rocks (i, j), and anorthosites (k, l) from the KMC (normalizing values from Sun and McDonough, 1989). Symbols as in Figure 7.
657
ELİTOK et al. / Turkish J Earth Sci
Figure 8. (Continued).
characterized by significant Cs and Pb enrichment, with
relatively positive U-Th and K anomaly and relatively
negative Ba, Nb, Ta, Ti, and Sr anomalies. Negative Ba and
Sr anomalies are considered to result from partitioning
into plagioclase (Figure 8c). In contrast to the granitoid
pluton, they exhibit a slightly depleted to enriched pattern
of light rare earth element (LREEs) with (La/Sm)N ratios
of 0.5–7.75 (Figure 8d). They display various negative
Eu anomalies with Eu/Eu* = 0.17–0.93, suggesting role
of plagioclase fractionation. Mg# are mainly below 50
(between 19.56 and 41.77), except KR22 and KR23 (78.93
and 56.44, respectively). The porphyritic microgranite
enclaves are slightly peraluminous [molar Al2O3 / (CaO +
Na2O + K2O) between 1.27 and 1.03, except KR3 (0.9)].
Major oxide content of the quartz-poor hybrid rocks
ranges from 50.9 to 55.4 wt.% for SiO2, 0.47 to 0.83 wt.%
for TiO2, 7.3 to 10 wt.% for Fe2O3, 0.14 to 0.32 wt.% for
MnO, 4.75 to 9.98 wt.% for MgO, and 0.24 1.14 wt.% for
K2O. They are characterized by various enrichments in Cs,
Rb, Ba, Pb, and K, with slightly positive U and Sr anomalies
and relatively negative Nb, La, and Ce and slightly negative
Ti anomalies (Figure 8e). Negative Nb-Ta anomalies are
usually regarded as a signature of subduction-related and/
or crust-derived magmas (Whalen et al., 1996). However,
on the chondrite-normalized rare earth element diagram,
they display a slightly to highly LREE-depleted pattern
658
with (La/Sm)N ratios of 0.3–0.91, and slightly positive to
negative Eu anomaly with Eu/Eu* = 0.8–1.18 (Figure 8f).
Major oxide content of the quartz-rich hybrid rocks
ranges from 57 to 63.4 wt.% for SiO2, 0.4 to 0.57 wt.% for
TiO2, 6.35 to 6.54 wt.% for Fe2O3, 1.88 to 3.16 wt.% for
MgO, and 1.04 to 3.28 wt.% for K2O. They show various
enrichments in Cs, Rb, Ba, Pb, and K like the quartzpoor ones with a slightly negative Nb, Ta, La, Ce, and
Ti anomalies (Figure 8g). However, on the chondritenormalized rare earth diagram, they display nearly flat
REE to LREE enriched patterns with (La/Sm)N ratios of
0.96–4.34 and slightly negative Eu anomaly with Eu/Eu* =
0.76–.95 (Figure 8h).
Some selected major oxide contents of mafic rocks
(KR4 and KR20) in the hybrid rocks are 44.1–49 wt.%
for SiO2, 11.7–14.7 wt.% for Fe2O3, 5.87–7.7 wt.% for
MgO, 10.9–12.25 wt.% for CaO, 0.19–0.5 wt.% for K2O,
and 1.02–2.64 wt.% for Na2O. Major oxide contents of the
diabasic rock intruding into the granitoid pluton are 43.1
for SiO2, 14.3 for Fe2O3, 3.65 for MgO, 13.3 for CaO, 0.11
for K2O, and 1.27 for Na2O.
On the primitive mantle-normalized trace element
diagram, they display mainly enrichment in Cs, U and
Pb and differ from the other rock associations with their
positive Sr anomaly, except the quartz-poor hybrid rocks
(Figure 8i). Th content is inversely proportional to the SiO2
ELİTOK et al. / Turkish J Earth Sci
content such that the samples with SiO2 contents between
44.1 and 49 wt.% have Th content from 3.68 to 0.52 ppm,
respectively. The mafic rocks are characterized by variable
negative Nb anomalies but slightly negative Ti anomaly,
which may also point to subduction-related tectonic
setting. On the chondrite-normalized REE diagram,
mafic samples from the hybrid area display slightly LREEenriched and depleted patterns with (La/Sm)N of 0.96 and
1.72, and relatively positive and negative Eu anomaly with
Eu/Eu* = 0.97–1.25 (Figure 8j). Diabase samples taken
from the dyke within the granitoid pluton display an
enriched pattern with Eu/Eu* = 1.45. Enriched trending
in the LREEs as well as enrichment in incompatible LILEs
signifies that the source rock may be originated from an
enriched mantle.
Some selected major oxide contents of the anorthositic
rocks (N21 and N22B) in the hybrid rocks are 49.4–49.9
wt.% for SiO2, 11.5–12.9 wt.% for Fe2O3, 3.98–4.92 wt.%
for MgO, 2.75–3.28 wt.% for CaO, 0.12–0.38 wt.% for K2O,
and 4.54–4.72 wt.% for Na2O. However, they have high LOI
values (6.08 and 6.63 wt.%) and the sum is considerably
below 100 wt.% (94.74 and 98.29 wt.%). Thin-section
studies show that nearly 5% to 15% of the anorthositic rocks
were altered due to the carbonation within plagioclases
and to a lesser amount of chloritization as well as Fe-oxide
formations. On the primitive mantle-normalized trace
element diagram, they display enrichment in Cs; relatively
positive K, Pb, and Ti anomalies; and relative depletion in
Nb (Figure 8k). They display a nearly flat pattern in heavy
rare earth elements (HREEs) and slight enrichment and
depletion in LREEs (Figure 8l).
The granitoids and porphyritic microgranite enclaves
of the current study are evaluated together in the chemical
and tectonomagmatic discrimination diagrams proposed
for granitoids. Granitoid rocks especially display a
distribution from metaluminous to peraluminous, but
mainly peraluminous, and they occupy mostly the I-type
field (Figure 9a). The rock composition of the granitoid
pluton, which consists mainly of quartz, orthoclase,
plagioclase, hornblende, biotite, augite, sphene, and
opaque minerals, also strongly suggests the metaluminous
source of the rocks.
For establishing the tectonic setting, discrimination
diagrams based on both major and trace elements have
been used. All the granitoid rocks from the study area are
plotted in the (VAG+Syn-COLG) field on the Y versus
Nb diagram (Figure 9b). The (Y+Nb) vs. Rb diagram is
used to discriminate between VAG and Syn-COLG. All
the granitic and monzonitic rock suites fall mostly in the
VAG field in this diagram (Figure 9c), suggesting arcrelated origin. In the tectonic discriminant diagram by
Batchelor and Bowden (1985), analyses of the granitoid
pluton and porphyritic microgranite enclaves plot mainly
from preplate collision to syncollision field, but quartzmonzonite samples plot within the postcollision uplift
field (Figure 9d).
6. Discussion
In the KMC, the granitoid suite including both main
granitoids and porphyritic microgranite enclaves plots
within the VAG field on the Rb vs. (Y+Nb) tectonic setting
discrimination diagram, confirming arc-related origin.
They lie within the metaluminous to peraluminous and
also the I-type granite field (Figure 9a). The majority of the
granitoid components from the CACC plutons show a calcalkaline affinity, with a metaluminous to peraluminous
character, and they mainly plot within the volcanic
arc and collisional granite field on the trace element
discrimination diagrams (Akıman et al., 1993; Kuşcu
et al., 2002; Kadıoğlu et al., 2003 and references therein;
İlbeyli et al., 2009). Metaluminous to peraluminous I-type
granitoids are interpreted to have originated in a volcanic
arc setting (Kim et al., 2005). In the Q-ANOR diagram,
the rock suites of the granitoid pluton and porphyritic
microgranite enclaves occurring within the hybrid rocks in
the study area plot within the monzogranite-granodiorite
and granodiorite-tonalite fields, respectively. Different
processes have been reported for the derivation of tonalitic
magma: i) fractional crystallization of basaltic magma or
by partial melting of basaltic rocks (amphibolites with
or without) (Hickey-Vargas, 2005; Philipp et al., 2008),
ii) partial melting of amphibolite or amphibolitic lower
crust (Rushmer, 1991; Whalen et al., 2002), iii) evolution
of the lamprophyric mafic magma to give a batch with
the geochemical composition of tonalite (Christofides et
al., 2007). Wenge et al. (2005) experimentally showed that
tonalitic and granodioritic melts can be formed by solid
dehydration melting of amphibolite at 2.0 GPa and 850–
1000 °C. On the other hand, tonalitic arc magmatism was
reported from oceanic subduction zone settings (Giunta et
al., 2006; Shervais, 2008). Yan et al. (2010) also suggested
2 possible sources for the origin of tonalitic magma in
the granitic rocks from the Nansha microblock (South
China Sea): i) partial melting of Precambrian continental
basement and Precambrian rocks, and ii) mantle-derived
magma, which results from the interaction of released
fluids from subducted slab and the overlying mantle
wedge.
Petrographic analyses also indicate that hybrid rocks in
the KMC are characterized by mingling/mixing of mafic
(characterized mainly by mixed basaltic and lamprophyric
magma), anorthositic, and/or rhyolitic magmas. There are
numerous examples for the association of anorthositic rocks
with granitoid and monzonitic rocks (Wright, 1975; Kolker
et al., 1990; Fazlnia et al., 2007). There are some suggestions
related to the genesis and association of anorthositic rocks
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ELİTOK et al. / Turkish J Earth Sci
Figure 9. Plot of the magmatic rocks from the Karacaali Magmatic Complex on the a) A/NK (Al2O3/Na2O+K2O) vs. A/CNK (Al2O3/
CaO+Na2O+K2O) (Maniar and Piccoli 1989), b) Nb vs. Y, and c) Rb vs (Y+Nb) discrimination diagrams of Pearce et al. (1984), and
d) R1-R2 diagram (Batchelor and Bowden, 1985). VAG: Volcanic arc granites, syn-COLG: syncollision granites, WPG: within-plate
granites, ORG: ocean-ridge granites. Symbols as in Figure 7.
with the granitic intrusions: i) fractional crystallization of
melts of upper mantle or deep crustal origin (Duchesne
and Demaiffe, 1978); ii) differentiation of basaltic magma
and accumulation of buoyant plagioclase at the top of deepseated magma chambers (i.e. at the crust-mantle interface
or in the lower crust), then followed by diapiric uprising
of low-density plagioclase mushes toward midcrustal
level in the anorthositic composition due to gravitational
instability (Czamanske and Bohlen, 1990; Longhi et al.,
1993; Mitchell et al., 1996; Namur et al., 2011); iii) partial
melting of the lower crust resulting in intrusion of both
anorthositic and granitic magma (Fazlnia et al., 2007); iv)
fractionation of mantle-derived melts resembling high-Al
gabbro of varied composition (Maji and Ghosh, 2010). Of
these, presumably, anorthositic magma in the hybrid rocks
660
of KMC formed by differentiation of basaltic magma and
accumulation of buoyant plagioclase at the top of deepseated magma chambers (i.e. at the crust-mantle interface
or in the lower crust).
The lamprophyres can be produced by partial melting
of the enriched mantle as a result of a heat source formed in
several ways, e.g., i) hotspot plume (Dacheng et al., 2004),
ii) decompression melting of mantle lithosphere (Bea
et al., 1999), or iii) slab-break-off (Atherton and Ghani,
2002). Plá Cid et al. (2006) reported that lamprophyres are
related to orogenic settings, since oceanic plate subduction
may promote metasomatism in the lithospheric mantle.
The intrusion of lamprophyres within a convergent margin
setting containing calc-alkaline magmatism is significant
because it indicates that rifting and crustal extension occur
ELİTOK et al. / Turkish J Earth Sci
simultaneously with subduction (Jackson et al., 1998).
The processes responsible for the origin of lamprophyre
are suggested to include magma differentiation, crustal
contamination, mantle enrichment, and melting (Wang et
al., 2007). Xu et al. (2007) summarized the petrogenesis of
lamprophyres as follows: i) partial melting of metasomatic
and enriched mantle source, either in a subduction-related
environment or in the subcontinental lithospheric mantle;
ii) continental crust contamination of mafic magmas;
and iii) mixing of upwelling basaltic magma with varying
amounts of ultrapotassic lithospheric mantle melts, which
is related to heating and/or thinning of subcontinental
lithospheric mantle, or of mantle-derived basaltic or
lamproite melts and crustally derived silicic melts.
Therefore, occurrence of lamprophyric melts within the
hybrid rocks associated with the granitoids in the study
area indicates the role of the lithospheric mantle in the
petrogenesis of the magmatic complex.
The genesis and evolution of mafic to felsic plutons in
the CACC are still matters of debate. Akıman et al. (1993)
interpreted that, on a regional scale, the western margin
granitoids of the CACC have been derived mainly from the
continental crust and formed in a collisional environment,
where partial melting took place in a shortened and
thickened crust, and were then emplaced in a continental
platform metamorphosed by ophiolite obduction and
collision. Boztuğ (2000) identified separate magmatic
episodes along the passive margin of the Anatolides such
as a syncollisional peraluminous episode, a postcollisional
calc-alkaline hybrid, and a postcollisional within-plate
alkaline episode. The I-type intrusions in central Anatolia
are considered to be postcollisional (Önal et al., 2005; Boztuğ
and Arehart, 2007; Delibaş et al., 2011). Boztuğ (1998)
considered that at the end stages of crustal thickening,
lithospheric delamination could generate underplating
of mafic magma, which also melts the lowermost part
of crust that yields the voluminous postcollisional,
calc-alkaline, I-type monzonitic-granodioritic hybrid
association in central Anatolia. After the emplacement
of this magmatic pulse, the tectonic regime could have
been changed from compression to tension, which may
cause the partial melting of the upwelling mantle material
under the conditions of adiabatic decompression, which
produces postcollisional alkaline magma. However,
Kadıoğlu et al. (2003) stated that some postcollisional
granitoids in the CACC may also plot in the upper parts of
the VAG field or may cover compositions plotting in both
Syn-COLG and VAG fields. Kadıoğlu et al. (2006) found
that the inferred subduction zone’s influence on the CACC
magmatism requires a careful evaluation of the existing
models for its postcollisional origin within the framework
of the Mesozoic geodynamic evolution of the eastern
Mediterranean region. They proposed a different tectonic
model for the evolution of granitoid rocks, especially in
the western CACC. The east-west trending İzmir-AnkaraErzincan ocean basin bounded the northern CACC
terminally closed by a subduction zone dipping northward
beneath the Pontides and away from the complex later in
the Paleocene-Eocene. In the southern CACC, subduction
of the Inner Tauride oceanic lithosphere beneath the
CACC initiated during the Late Cretaceous (92–88 Ma
ago; Dilek et al., 1999), and continued convergence
between the Tauride and the CACC blocks resulted
in a continental collision in the Paleocene (Kadıoğlu
and Dilek, 2010). Kadıoğlu and Dilek (2010) suggested
that partial melting of the subduction metasomatized
mantle beneath the CACC produced the granitic suites
of the Andean-type magmatism. It is mainly debated
that the subduction-related characteristics of the CACC
magmatics are thought to be the result of northeastward
dipping subduction of the oceanic lithosphere of the Inner
Tauride basin (in the present coordinate system) (Kadıoğlu
et al., 2003,2006; Kadıoğlu and Dilek, 2010). The majority
of the CACC plutons have intrusion (emplacement)
ages of around the Campanian-Maastrichtian [e.g.,
Terlemez granitoid around 81.5 ± 1.9 Ma (Yalınız et al.,
1999); I-type Baranadağ and A-type Çamsarı granitoids
during the Campanian (74.0 ± 2.8 and 74.1 ± 0.7 Ma,
respectively, in Köksal and Göncüoğlu (2008)]. Kadıoğlu
et al. (2003) suggested a model in which the arrival and
partial subduction of the northern edge of the Tauride
platform at the north-dipping subduction zone resulted
in slab break-off and development of the asthenospheric
window beneath the continental lithosphere of the
complex. In their model, rising hot asthenosphere caused
melting of the metasomatized lithosphere, producing the
high-K calc-alkaline and high-K shoshonitic magmas
of the granite and monzonite supersuites. Delibaş et al.,
(2011) carried out geochronological studies on single
zircons from the KMC. They obtained 73.1 ± 2.2 Ma (95%
confidence) from the porphyritic quartz monzonite and 67
± 13 Ma (95% confidence) from the rhyolite/rhyodacite,
which is considered to be the intrusion or crystallization
age, corresponding to the Late Cretaceous. Based on the
field relations and age data, they suggested that there
is a coeval relationship between plutonic and volcanic
rocks. They considered that the overlapping ages between
monzonite and rhyolitic rocks reflect a long-lasting
magma production and crystallization in one or several
zoned magma chambers.
6.1. Geodynamic Interpretations
The following scenario for the emplacement of the Karacaali
magmatic rock suite may be envisaged. Turkey, situated in
critical segment of the Alpine-Himalayan orogenic belt,
has witnessed the Paleotethyan and Neotethyan ocean
basin evolutions from the Paleozoic to the present time,
661
ELİTOK et al. / Turkish J Earth Sci
respectively (Şengör and Yılmaz, 1981; Robertson and
Dixon, 1984). With the closure of the Paleotethys during
the middle-late (?) Jurassic, only 2 oceanic areas were
left in Turkey: the multiarmed northern branch of the
Neotethys that developed within the IAESZ, and relatively
simpler southern branches of the Neotethys (Şengör and
Yılmaz, 1981; Robertson and Dixon, 1984). The southern
strand of the northern branch of the Neotethys, the Inner
Tauride ocean, most probably opened during the Jurassic
(Şengör and Yılmaz, 1981) and evolved between the
CACC to the north and the Tauride carbonate platform
to the south during the Late Mesozoic (Şengör and
Figure 10. Petrogenetic model for the evolution of the Kırıkkale Magmatic Complex. CACC:
Central Anatolian Crystalline Complex, TAP: Tauride Anatolide Platform (modified from
Kadıoğlu et al., 2003).
662
ELİTOK et al. / Turkish J Earth Sci
Yılmaz, 1981; Tankut et al., 1998; Dilek et al., 1999). That
is to say, the CACC including the study area was located
between the main northern branch of the Neotethys and
its southern strand. Therefore, the Kırıkkale area lies
in a complex geodynamic setting that was subjected to
subduction-obduction and collision-related deformation
events. The subduction signature in the granitic rocks
might have resulted from either south-dipping subduction
of the Paleotethyan oceanic lithosphere or subduction of
the Inner Tauride oceanic lithosphere beneath the CACC
since the Late Cretaceous. During the Late Cretaceous,
the leading edge of the northern margin of the CACC was
pulled down into the mantle depths at the subduction zone,
and simultaneously ophiolites were obducted onto the
passive northern margin of the CACC (Dilek and Moores,
1990; Okay et al., 2001). The east-west trending İzmirAnkara-Erzincan ocean basin terminally closed later in the
Paleocene-Eocene during the diachronous collisions of the
Sakarya-Pontide (to the north) with the Anatolide-Tauride
and Kırşehir continental blocks (to the south) (Okay and
Tüysüz, 1999). With the onset of northeastward-dipping
subduction of the oceanic lithosphere of the Inner Tauride
basin (in the present coordinate system) during the Late
Cretaceous, fluids ± melts derived from the slab invaded
and metasomatized the mantle wedge (Figure 10a). Further
fluid ± melt derivation from the slab induced melting in
the metasomatized upper mantle (formation of basaltic
and lamprophyric magma) and these melts underplated at
the base of the CACC (Figure 10b). Mantle-derived and
underplated melts were injected into the continental crust
of the CACC along its northwestern edge (Figures 10c and
10d). The injection of the mantle-originated melts caused
a temperature increase and initiation of the partial melting
in the crust, giving rise to the evolution of the silicic magma
chamber at the crustal level (Figure 10e). At the same
time, anorthositic magma was formed by differentiation of
underplated basaltic magma and accumulation of buoyant
plagioclase at the top of deep-seated magma chambers
(Figures 10f and 10i). Thermal instability produced
convection, mechanical interaction, and hybridization
among mafic, anorthositic, and felsic magmas (Figures
10g and 10j), as suggested by Kadıoğlu et al. (2003). It is
widely accepted that most continental collisions initiate
with the attempted subduction of the continental passive
margin, which follows the subducted oceanic lithosphere
into the trench (Davies and von Blanckenburg, 1995). The
continental lithosphere, due to its thick crust, is buoyant
and resists subduction, while the cold and dense oceanic
lithosphere generates a large downward force, resulting in
detachment from the continental lithosphere (Davies and
von Blanckenburg, 1995). The pronounced slab breakoff
is followed by syn- to postcollisional magmatism and
metamorphism, and it generates uplift due to the removal
of a large load, giving rise to rapid isostatic uplift (Davies
and von Blanckenburg, 1995). It is likely that following the
collision of the Tauride-Anatolide platform with Central
Anatolia, slab detachment resulted in tensional forces
above the subduction zone and within the overlying the
CACC, which allowed the intrusion of the granitic magma
into the upper crust with the mafic parts from the Late
Cretaceous to the Paleocene. The hybrid rocks most likely
indicate products of injection of basaltic/lamprophyric
and anorthositic magma into partly crystalline granite.
Conformably, Delibaş et al. (2011) interpreted the
continuous input of mafic magma into the semievolved
acid magma chamber. That is to say, mafic and hybrid
magma intruded into the granitic magmatic system just
after crystallization of granitic magma in the upper crust.
It is commonly known that the cessation of subduction
and replacement of the cold oceanic lithosphere by
the asthenosphere resulted in rapid isostatic uplift and
erosional denudation of the collisional area (Davies
and von Blanckenburg, 1995), characterized by basal
conglomerates of the Eocene units in the Kırıkkale area.
The Paleocene (the Dizilitaş Fm.) and the Eocene clastic
sedimentary units (the Bulanıkdere Fm., the Karagüney
Fm., the Mahmutlar Fm.) overlie the Late Cretaceous
units intruded by plutonic rocks (Akıncı, 2008). Clastic
materials derived from quartz-porphyry and granitoids
widely occur in the basal conglomerates in the Eocene
units, suggesting pre-Eocene exhumation of the granitoids
in the study area (Delibaş and Genç, 2004).
Acknowledgment
The authors are grateful to Zafer Aslan and Nurdane
İlbeyli for their excellent suggestions, which improved the
scientific content of the paper.
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