structure and geochemistry of the adakitic horoz granitoid, bolkar … · 2012-08-21 · structure...

Structure and geochemistry of the adakitic Horoz granitoid, BolkarMountains, south-central Turkey, and its tectonomagmatic evolution

Yusuf K. Kadioglua and Yildirim Dilekb*

aDepartment of Geological Engineering, University of Ankara, Tandogan, Ankara, Turkey;bDepartment of Geology, Miami University, Shideler Hall, Oxford, OH 45056, USA

(Accepted 6 April 2009)

High-Al granitic and granodioritic rocks of the 55 Ma Horoz pluton in the BolkarMountains of southern Turkey provide important new constraints on the early Cenozoicevolution of the eastern Mediterranean region. The ENE–WSW-trending, sill-likepluton is intrusive into late Palaeozoic–early Mesozoic metamorphic rocks of theCentral Tauride block, and is unconformably overlain by Plio-Pleistocene alluvialdeposits. The metaluminous to peraluminous granitoids have high-K calc-alkaline tohigh-K shoshonitic compositions, and show enrichment in large ion lithophile anddepletion in high-field strength elements relative to ocean ridge granite. Their highAl2O3 contents (15.9–20.06 wt%) and low SiO2, MgO, and Mg numbers are consistentwith adakitic compositions. These geochemical features, coupled with low Sr/Y andLa/Yb ratios and trace-element patterns, suggest that the Horoz magmas were producedin part by partial melting of a subduction-metasomatized mantle. The high-Al adakiticand calc-alkaline compositions are consistent with partial melting of a hydratedlithospheric mantle and an amphibolitic–eclogitic mafic lower crust that was triggeredby delamination-induced asthenospheric upwelling. We propose that, followingPalaeocene continental collision between the Tauride and Central AnatolianCrystalline Complex, the inferred lithospheric delamination was a result of founderingof the overthickened orogenic root. Asthenospheric upwelling beneath the youngorogenic belt thermally weakened the crust, and caused uplift and tectonic extensionleading to core complex formation (Nigde massif), development of an extensionalvolcanic province (Cappadocia), and tectonic collapse of the Central Tauride block(Bolkar Mountains). The shallow-level Horoz pluton was unroofed by ,23 Ma as acombined result of crustal uplift and erosion throughout the Palaeogene.

Keywords: Turkey; Tauride block; adakitic magmatism; lithospheric delamination;subduction-metasomatized mantle; granite and granodiorite plutons

Introduction

Granitoid magmatism was a significant component of crustal evolution and crustal growth

during the orogenic build-up in Anatolia (Turkey) throughout the latest Mesozoic and

Cenozoic (Bingol et al. 1982; Harris et al. 1994; Erdogan et al. 1996; Erler and Goncuoglu

1996; Boztug et al. 1997, 2006; Altunkaynak and Yilmaz 1999; Gessner et al. 2001;

Ilbeyli et al. 2004; Koksal et al. 2004; Koprubasi and Aldanmaz 2004; Arslan and Aslan

2006; Dilek and Altunkaynak 2007, 2009; Glodny and Hetzel 2007; Ozgenc and Ilbeyli

ISSN 0020-6814 print/ISSN 1938-2839 online

q 2010 Taylor & Francis

DOI: 10.1080/09507110902954847

http://www.informaworld.com

*Corresponding author. Email: [email protected]

International Geology Review

Vol. 52, Nos. 4–6, April–June 2010, 505–535

Downloaded By: [Dilek, Yildirim] At: 17:15 15 February 2010

2008; Oner et al. 2009, 2010). Granitoid plutons provide us with critical information and

insights about the tectonic evolution of these young orogenic belts, which have not yet

been deeply eroded. Active subduction tectonics, collisional, and post-collisional thermal

perturbation of a thickened continental crust and a lithospheric mantle, and asthenospheric

upwelling accompanied by lithospheric-scale continental extension, were the common

causes of granitoid magmatism in this region (Dilek and Altunkaynak 2009). However, it

is commonly difficult to differentiate between these geodynamic origins due to the lack of

systematic geochemical, isotopic, and geochronological studies of the granitoid plutons

and the well-constrained regional geology.

In this paper, we describe the geology and structure of an early Eocene granitoid

(Horoz pluton) in the central Tauride block in southern Turkey and present new

geochemical data from its granitic and granodioritic units. The Horoz pluton occurs

adjacent to the Inner Tauride Suture Zone between two continental blocks, the Tauride

platform and Central Anatolian Crystalline Complex (CACC). This tectonic position

makes the Horoz granitoid a critical geological entity to use in developing an internally

coherent and a regionally compatible geodynamic model for the latest Mesozoic–

Cenozoic evolution of the eastern Mediterranean region. We introduce our model as a

working hypothesis, which will be further tested with field-based petrological,

geochemical, geochronological, and isotopic studies in the future.

Regional geology

In this section, we describe the pertinent geological entities in southern Turkey that are

relevant to the tectonomagmatic evolution of the Horoz pluton.

Central Anatolian Crystalline Complex

The CACC consists mainly of Palaeozoic–Mesozoic metamorphic massifs and composite

plutons ranging in age from the Late Cretaceous to the Miocene (Figure 1; Gulec 1994;

Boztug 2000; Kadioglu et al. 2003, 2006; Ilbeyli et al. 2004). The three main massifs,

Kirsehir, Akdag, and Nigde, form the nucleus of the CACC and consist of interlayered

metacarbonate and metapelitic rocks. Despite apparent similarities in lithology, the

massifs can be distinguished by distinct metamorphic pressure–temperature–time paths,

particularly with respect to timing, rate, and primary mechanisms of unroofing (Whitney

and Dilek 1998).

Nigde massif

The Nigde massif in the southern part of the CACC (Figure 1) is exposed in a structural

dome (Gautier et al. 2002), which has been interpreted as a Cordilleran-type metamorphic

core complex (Whitney and Dilek 1997). A gently (,308) S-dipping detachment fault

bounding the Nigde massif along its southern edge juxtaposes multiply deformed marble,

quartzite, and schist in the footwall from clastic sedimentary rocks of the Ulukisla Basin

(UB) in the hanging wall. The central part of the Nigde massif consists predominantly of

upper amphibolite-facies metasedimentary rocks and the Miocene peraluminous Uckapili

granite.

The SW part of the CACC experienced relatively high-temperature metamorphism

associated with extensive Andean-type arc magmatism represented by the 80–70 Ma

CACC plutons (see below). It then underwent Barrovian metamorphism at mid-crustal

pressures (,5–6 kbar) and at high temperatures (.7008C) possibly associated with

Y.K. Kadioglu and Y. Dilek506


Figure 1. (a) Simplified tectonic map of Anatolia (Turkey) and (b) CACC, showing the plateboundaries, suture zones, active faults, and major plutons. BF, Burdur Fault; BZSZ, Bitlis–ZagrosSuture Zone; DSF, Dead Sea Fault; EAF, East Anatolian Fault; EF, Ecemis Fault; IAESZ, Izmir–Ankara–Erzincan Suture Zone; ITSZ, Inner-Tauride Suture Zone; LV, Lake Van; MS, MarmaraSea; NAF, North Anatolian Fault; NEAF, Northeast Anatolian Fault.

International Geology Review 507


orogenic crustal thickening during the latest Mesozoic–Palaeocene (Whitney and Dilek

1998). The Nigde core complex was exhumed to a depth of less than 2 km by tectonic

unroofing along low-angle detachment faults. Apatite fission track ages from the Nigde

rocks range from ,9 to 12 Ma and indicate slow to moderate cooling via exhumation at

rates of 30–88C/m.y. (Fayon et al. 2001).

CACC plutons

The Late Cretaceous plutons intruded the W–SW part of the CACC after the emplacement

of the Cretaceous Tethyan ophiolites, which are rooted in the Izmir–Ankara–Erzincan

Suture Zone to the north (Figure 1). These plutons include designated Granite, Monzonite,

and Syenite Supersuites, which are distinguished by field occurrences and major

differences in their mineral and chemical compositions (Kadioglu et al. 2006). The Granite

Supersuite plutons commonly occur along the W–SW edge of the CACC (east of the Salt

Lake; Figure 1) and consist of calc-alkaline rocks ranging in composition from tonalite,

granodiorite, and biotite granite to amphibole biotite–granite and biotite–alkali feldspar

granite (Ataman 1972; Akıman et al. 1993; Kadioglu and Gulec 1996; Gulec and Kadioglu

1998; Boztug 2000). Plutons of the Monzonite Supersuite occur immediately east of the

Granite Supersuite plutons and are composed mainly of sub-alkaline quartz monzonite and

monzonite (Bayhan 1987; Kadioglu et al. 2006). The Syenite Supersuite represents the

youngest phase of plutonism in the Late Cretaceous (,69 Ma) and generally occurs in the

inner part of the CACC (Duzgoren-Aydin 2000; Ilbeyli 2004; Kadioglu et al. 2006;

Boztug et al. 2009). Rocks of this supersuite are composed of silica-saturated (quartz

syenite and syenite) and silica-undersaturated, nepheline- and pseudoleucite-bearing

alkaline rocks.

The CACC plutons show a progression from high-K calc-alkaline and high-K

shoshonitic compositions in the Granite Supersuite to typical shoshonitic compositions in

the Monzonite Supersuite rocks (Boztug et al. 1997; Kadioglu et al. 2006). Isotopic and

trace-element signatures of the Syenite Supersuite plutons suggest that their magmas were

more enriched in within-plate mantle components compared to the Granite and Monzonite

Supersuite plutons (Kadioglu et al. 2006). 40Ar/39Ar age data from these Granite,

Monzonite, and Syenite Supersuite plutons yield ages of 77.7 ^ 0.3, 70 ^ 1.0, and

69.8 ^ 0.3 Ma, respectively (Kadioglu et al. 2006), indicating a temporal shift towards

more alkaline magmatism inwards from the CACC margin.

Ophiolites, high-P rocks, and Inner-Tauride Suture Zone (ITSZ)

Discontinuous exposures of the Tethyan ophiolites and melanges define a major suture, the

ITSZ, surrounding the CACC in the south (Figures 1(a) and 2). The Inner-Tauride

ophiolites (ITO) exposed along this suture zone (i.e. Alihoca, Aladag, Mersin) consist

mainly of tectonized harzburgites, mafic–ultramafic cumulates, and gabbros, and

commonly are not associated with sheeted dikes and extrusive rocks (Parlak et al. 1996,

2002; Dilek et al. 1999a). They are underlain by thin (,200 m) thrust sheets of

metamorphic sole rocks, and both the ophiolitic units and the sole rocks are intruded by

mafic dike swarms composed of basaltic to andesitic rocks with island arc tholeiite (IAT)

affinities. 40Ar/39Ar hornblende ages of 92–90 and 90–91 Ma from the metamorphic sole

and dike rocks, respectively, indicate Cenomanian–Turonian ages for the ITO (Dilek et al.

1999a; Parlak and Delaloye 1999; Celik et al. 2006).



The ITSZ is also marked by discontinuous exposures of blueschist-bearing mafic–

ultramafic and carbonate rocks along the northern edge of the Tauride block (Figure 1(a);

Okay 1986). The occurrence of sodic amphibole-containing metasedimentary and

metavolcanic rocks in the Bolkar Mountains region (Blumenthal 1956; Van der Kaaden

1966; Gianelli et al. 1972; Dilek and Whitney 1997) extends into the Tavsanli Zone in NW

Anatolia and into the Pinarbasi zone in the eastern Taurides in East-Central Anatolia

(Okay 1984; Onen and Hall 1993; Okay et al. 1998). These high-P/low-T rock

assemblages show anticlockwise PTt trajectories of their metamorphic evolution and

indicate increasing P/T ratio with cooling that was associated with continuous subduction

within the Inner-Tauride Ocean (Dilek and Whitney 1997, 2000).

A ,300-m-thick klippen of a dismembered ophiolite, the Kiziltepe ophiolite, rests

tectonically on the recrystallized carbonates of the Bolkar Mountains (Figure 3). The

Kiziltepe ophiolite includes meta-lavas and serpentinized peridotites, underlain by a

metamorphic sole of thin sliver of foliated amphibolite. Hornblende in this sole is crosscut

Figure 2. Geological map of south–central Turkey, showing the distribution of major tectonicunits, faults, and the Horoz pluton in the Central Tauride block. BFF, Bolkar Frontal Fault.



and rimmed by sodic amphibole minerals, indicating blueschist-facies overprint recording

a minimum pressure of 7–8 kbar for a temperature range of ,300–5008C (Dilek and

Whitney 1997). These observations suggest that the Kiziltepe metamorphic sole was

dragged deeper into the subduction zone where the mineral assemblages were overprinted

by blueschist-facies minerals (crossite, Mg-riebeckite, albite, calcite, quartz) that resulted

from increasing P/T ratio. This anticlockwise PTt path of the Kiziltepe sole rocks shows

that the high-P metamorphic overprint was accompanied and succeeded by rapid uplift

along the northern edge of the Tauride block in the latest Cretaceous–early Tertiary (Dilek

and Whitney 1997).

Sedimentary basins

The Tuzgolu and Ulukisla sedimentary basins, which initially evolved as peripheral

foreland and/or forearc basins in the Late Cretaceous, delimit the CACC in the west and

the south (Figures 1(a) and 2). These basins developed in the latest Cretaceous when

compressional tectonics was dominant within the Neotethyan realm (Oktay 1982; Gorur

et al. 1984, 1998). They were filled with Upper Cretaceous to Oligo-Miocene volcanic and

sedimentary materials and became part of a larger, shallow intra-continental basin

consisting mainly of lacustrine and fluvial deposits that covered much of Central Anatolia

throughout the Miocene and Quaternary (Oktay 1982; Demirtasli et al. 1984: Cater et al.

1991; Clark and Robertson 2002).

The UB includes a thick succession (ca. 2 km) of upper Palaeocene–lower Eocene

basaltic to andesitic submarine pillow lavas, lava flows, volcaniclastic rocks, and

intercalated limestones (Halkapinar Formation; Figure 3) that are underlain by the Late

Cretaceous Alihoca ophiolite (Dilek et al. 1999a; Figure 2). These Palaeogene rocks were

Figure 3. View to the south towards the Bolkar Mountains. The upper Palaeocene–Eocene clastic,carbonate, and volcanic rocks of the Halkapinar Formation are in the foreground, and the upperPalaeozoic–lower Mesozoic marble and schist units of the Central Tauride block in the BolkarMountains are in the background. Nearly, ENE–WSW-running BFF in the valley south of theHalkapinar Formation juxtaposes the Cretaceous Alihoca ophiolite and ophiolitic melange againstthe Tauride carbonates. The reddish-brown Kiziltepe ophiolite at the elevation of 2975 m reststectonically on the Tauride carbonates and is underlain by an amphibolite sole with blueschist-faciesoverprint.



unconformably covered by Oligo-Miocene lacustrine to fluvial rocks. The UB formed

after the emplacement of the ITO and melanges onto the Tauride platform during the

Late Cretaceous and underwent late Eocene emergence, deformation, and onset of Oligo-

Miocene non-marine deposition (Blumenthal 1956; Demirtasli et al. 1984; Atabey et al.

1990; Gorur et al. 1998; Clark and Robertson 2002). The geochemical features of the

Palaeogene basaltic to andesitic volcanic rocks within the UB indicate relative enrichment

of the large ion lithophile (LILE) and light rare-earth elements (LREE) in comparison to

mid-ocean ridge basalts (MORBs) and relatively much less enrichment of Nb. The Nb

concentrations in these rocks are more enriched, however, than the less incompatible high-

field strength elements (HFSE) of Ti and Y. These geochemical features suggest a

subduction zone influence in the evolution of their magmas that involved low degrees of

partial melting in a within-plate setting (Clark and Robertson 2002).

Cappadocian Volcanic Province

The south-central part of the CACC includes the Cappadocian Volcanic Province

(Figure 1(a)), containing upper Miocene to Quaternary volcanic–volcaniclastic rocks and

polygenetic volcanic centres (Toprak et al. 1994; Dilek et al. 1999b). The Cappadocian

Volcanic Province represents a broadly NE–SW-oriented volcanic field that includes

upper Miocene to Quaternary volcanic–volcaniclastic rocks and polygenetic volcanic

centres marked by stratovolcanoes, cinder cones, volcanic ridges, and calderas (Innocenti

et al. 1975; Ercan et al. 1994; Toprak et al. 1994; Guctekin and Koprubasi 2009). These

volcanic edifices commonly form linear clusters along and/or at the intersections of fault

systems.

Cappodocian volcanic rocks are made mainly of pyroclastic deposits and lava flows

that are calc-alkaline in character (Kurkcuoglu et al. 1998; Temel et al. 1998). Lava

compositions range from basalt to rhyolite (48.4–70.5 wt% SiO2) and pyroclastic

rocks–ignimbrites have andesitic to dacitic compositions. Alkaline basalts are also

common in the Cappadocian volcanic sequence (Guctekin and Koprubasi 2009). Calc-

alkaline rocks show relatively high-Sr and -Nd isotopic ratios (0.703434–0.705468;

0.512942–0.512600), whereas these ratios for alkaline basalts are in the range of

0.703344–0.703964 and 0.512920–0.512780 (Kurkcuoglu et al. 1998). The geochemical

features and isotopic signatures of all volcanic rock types of the Cappadocian Volcanic

Province indicate that their calc-alkaline magmas were the products of mixing of an ocean

island basalt-like (OIB) mantle melts with subduction-metasomatized asthenospheric

mantle melts (Guctekin and Koprubasi 2009). These magmas were then further modified

by crustal contamination and assimilation–fractional crystallization (AFC) during their

ascent through the extending CACC.

Tauride block

The Tauride block south of the ITSZ is represented by the deformed and uplifted platform

carbonates that consist of variably metamorphosed, Palaeozoic to Upper Cretaceous

carbonates with siliciclastic and volcanic intercalations (Figures 2 and 3; Ricou et al.

1975, 1979; Ozgul 1976, 1984; Demirtasli et al. 1984). The Tauride block has been

interpreted as a rifted fragment of Afro-Arabia (Robertson and Dixon 1984; Garfunkel

1998) and is tectonically overlain by discontinuous outcrops of the Cenomanian–

Turonian Neotethyan ophiolites along its entire length (Figure 2; Dilek and Moores 1990;



Dilek et al. 1999a; Parlak et al. 1996, 2002; Celik et al. 2006; Celik and Chiaradia 2008;

Elitok and Druppel 2008).

Platform carbonates in the Bolkar Mountains are multiply folded and imbricated along

thrust faults, which caused substantial shortening and crustal thickening within the

platform. These contractional structures and crustal shortening developed first during

the obduction of the ITO from the north in the Late Cretaceous, and subsequently during

the collision of the Tauride block with the CACC in the latest Palaeocene–Eocene (Dilek

et al. 1999b). The Tauride block experienced gradual uplift in the footwall of a north-

dipping frontal normal fault system (Bolkar Frontal Fault, BFF; Figure 3) along its

northern edge starting in the Miocene, and developed as a southward-tilted, asymmetric

mega-fault block with a rugged, alpine topography (Dilek et al. 1999b).

Geology, petrography, and age of the Horoz granitoid

Plutonic rocks

The Horoz granitoid is a sill-like pluton intrusive into the platform carbonates of the

Central Tauride Belt in the Bolkar Mountains (Figures 2 and 4). The NE–SW-trending

Horoz granitoid has a sharp contact with the Tauride carbonates along which hornfels and

calc-silicate contact metamorphic rocks occur discontinuously (Figure 5). It is

unconformably covered by the alluvial sediments of the Horoz stream along its southern

edge. The granitoid rocks show brittle to cataclastic deformation along N508W-trending

faults (Figure 4).

The Horoz granitoid is composed mainly of granodiorite and granite, both of which

include mafic microgranular enclaves ranging in size from 1 cm up to 12 cm (Figure 6).

Granite is more abundant than granitoid and occurs in the central and southern parts of

the pluton. Medium- to coarse-grained granite has phaneritic to porphyro-phaneritic

textures and is mainly composed of quartz, feldspar, and biotite in the hand specimen

(Figure 6(a)). Quartz, orthoclase, oligoclase, biotite, and zircon constitute the main primary

Figure 4. Geological map of the Horoz pluton.



mineral phases in a holocrystalline granular texture in the thin section (Figure 6(b)).

Epidote, chlorite, and sericite occur as secondary minerals in the granite. Granodiorite is

exposed in the northern part of the pluton against the marble and hornfels of the contact

metamorphic zone (Figure 4). It has a fine-grained phaneritic crystalline texture and is

mainly composed of quartz, feldspar, biotite, and amphibole in the hand specimen

(Figure 6(c)). It has a holocrystalline granular texture and consists of quartz, orthoclase,

oligoclase, biotite, amphibole, and opaque minerals in the thin section (Figure 6(d)).

Epidote, calcite, and chlorite occur in fractures as secondary minerals. A cataclastic mortar

structure is observed in the rock along the brittle, late-stage faults.

We determined the age of the Horoz pluton using U–Pb zircon dating of its granitic

end member. A relatively fresh, peraluminous granite sample yielded a 206Pb/238U zircon

age of 56.1 Ma (Y. Dilek, unpublished data), indicating an earliest Eocene (Ypresian)

crystallization age for the Horoz granitoid. Detailed documentation of the age and isotope

Figure 5. (A) Field photo of the Horoz pluton, showing the contact relations between the graniteand granodiorite units, hornfels, and the host rocks of the Tauride carbonates (view to the north).(B) Pervasively jointed Horoz granite is unconformably overlain by the Plio-Pleistoceneconglomerate of the Horoz stream (to the right). View to the NE.



data from the Horoz granitoid and other plutons in the Central Tauride block will be

reported elsewhere (Y. Dilek et al. in preparation).

Young felsic and mafic dikes

Mafic to felsic dikes crosscut the Horoz granitoid parallel to the main direction of the

intrusive body (Figure 5). Dikes range in thickness from 10 cm to 10 m and may continue

locally for 100–250 m along-strike. They have sharp contacts with their granitoid host

rocks and represent the youngest magmatic unit in the pluton. They commonly occur as

fresh and erosion-resistant rocks exposed at relatively higher topographic levels in the

field.

Felsic dikes were emplaced mainly along fracture and fault planes within the pluton

with a general orientation almost parallel to the trend of the whole intrusive body. They

comprise alkali feldspar granite and granite porphyry rocks. In the thin section, these dike

rocks are composed mainly of quartz, plagioclase, and orthoclase with biotite. The granite

porphyry dikes also include muscovite. Quartz occurs as euhedral to anhedral grains

ranging in size from 0.1 to 2 mm. Plagioclase is rather small in size (0.1–0.3 mm) and

mainly occurs in the granite porphyry. Orthoclase is mostly observed in the alkali feldspar

granite and in the granite porphyry rocks.

Doleritic (diabasic) mafic dikes intrude both the granite and granodiorite with sharp

contacts. In the thin section, these doleritic rocks have holocrystalline porphyritic and

hypocrystalline textures. They are composed mainly of plagioclase and pyroxene.

Fine-grained (up to 0.1 mm) plagioclase constitutes the bulk of the groundmass in the

dike rocks.

Figure 6. Photographs and photomicrographs of the granite (a, b) and granodiorite (c, d) units ofthe Horoz pluton.



Tab

le1

.M

ajo

ran

dtr

ace-

elem

ent

com

po

siti

on

so

fse

lect

edro

cksa

mp

les

fro

mth

eH

oro

zg

ran

ito

id,

Bo

lkar

Mo

un

tain

s,T

urk

ey.

GD

09

GD

11

GD

17

GD

22

GD

50

GD

52

GR

02

GR

04

GR

05

GR

06

GR

07

GR

08

GR

12

GR

13

SiO

25

8.9

86

3.3

26

3.4

36

3.7

26

5.4

36

5.6

56

6.1

06

7.3

27

1.0

26

8.1

26

8.3

76

7.2

77

0.0

56

8.8

2A

l 2O

31

7.7

91

5.3

61

6.6

31

5.9

02

0.0

61

9.7

81

7.7

51

5.9

31

3.9

81

5.1

91

5.8

01

6.3

81

4.1

81

7.8

4F

e 2O

36

.28

5.6

65

.01

5.7

43

.01

2.8

92

.29

2.9

11

.91

2.5

52

.65

1.3

62

.15

2.8

9M

nO

0.1

80

.08

0.0

90

.05

0.0

10

.06

0.0

20

.04

0.0

30

.04

0.0

60

.04

0.0

50

.01

Mg

O5

.25

2.9

03

.48

2.8

80

.47

0.5

20

.36

1.6

40

.69

1.2

11

.46

0.7

21

.23

1.9

3C

aO3

.98

4.7

82

.59

1.0

92

.48

1.9

42

.99

3.2

91

.95

2.3

32

.69

3.0

62

.18

0.5

7N

a 2O

4.4

54

.12

4.0

12

.97

3.9

14

.38

4.2

64

.81

4.2

53

.74

4.3

62

.84

3.5

25

.29

K2O

2.1

32

.12

3.1

35

.52

3.4

53

.43

3.9

72

.91

4.5

44

.58

3.7

46

.76

4.4

92

.95

TiO

20

.63

0.6

50

.68

0.9

30

.18

0.2

60

.37

0.3

30

.21

0.2

80

.28

0.2

70

.29

0.0

7P

2O

50

.40

0.2

50

.23

0.2

00

.04

0.0

20

.18

0.1

70

.12

0.1

80

.15

0.1

60

.12

0.2

1L

OI

0.8

40

.45

1.1

40

.91

0.6

50

.65

0.7

20

.40

0.4

81

.03

0.3

71

.01

0.9

90

.97

To

tal

10

0.9

39

9.6

91

00

.41

99

.91

99

.68

99

.59

99

.00

99

.75

99

.18

99

.25

99

.94

99

.86

99

.25

99

.56

Alk

6.5

86

.24

7.1

48

.49

7.3

67

.80

8.2

27

.73

8.7

98

.32

8.1

09

.60

8.0

18

.24

Mg

#0

.51

0.3

90

.47

0.3

90

.16

0.1

90

.17

0.4

20

.31

0.3

70

.41

0.4

00

.42

0.4

6F

eþ

Mg

11

.54

8.5

68

.48

8.6

23

.48

3.4

12

.65

4.5

42

.60

3.7

64

.12

2.0

83

.39

4.8

3C

NK

10

.57

11

.02

9.7

39

.58

9.8

49

.74

11

.22

11

.02

10

.74

10

.64

10

.79

12

.66

10

.18

8.8

1

Ba

40

8.7

05

10

.00

55

3.6

06

75

.10

42

2.0

04

11

.00

42

0.0

04

48

.30

53

0.8

04

64

.50

74

5.3

07

66

.00

42

0.6

06

13

.50

Sr

51

2.6

06

77

.00

55

6.2

03

26

.20

35

4.0

03

76

.00

34

0.7

05

40

.40

41

2.9

03

79

.00

59

8.9

03

48

.30

37

8.8

04

93

.30

Y3

9.3

01

8.2

01

7.3

03

1.3

01

5.4

01

2.4

51

1.6

01

5.8

01

1.8

01

3.2

01

4.5

01

7.9

01

2.6

01

3.2

0Z

r1

54

.90

20

0.0

02

22

.70

28

4.6

01

87

.00

19

6.0

01

95

.30

16

5.6

01

53

.00

15

5.5

01

59

.10

14

4.3

01

14

.40

13

9.2

0C

o2

0.5

03

1.4

02

9.3

04

1.6

02

3.2

12

6.5

42

1.2

03

9.2

04

8.1

01

1.3

03

0.6

01

4.2

01

4.4

01

9.3

0Z

n5

6.4

07

6.3

05

7.9

03

3.5

01

8.0

01

1.0

01

9.6

02

6.9

02

2.8

02

2.4

02

7.9

01

3.9

02

0.8

02

8.8

0G

a2

2.8

01

8.7

01

8.0

01

9.4

01

4.5

01

6.3

21

7.0

01

6.8

01

5.6

01

5.5

01

7.3

01

5.2

01

5.1

01

6.1

0G

e1

.10

1.0

00

.40

0.7

01

.00

1.3

41

.60

1.4

01

.60

1.0

01

.40

1.1

01

.50

1.3

0R

b5

6.5

06

3.4

07

0.3

01

88

.20

12

1.0

01

25

.00

92

.80

75

.80

12

0.4

01

06

.10

83

.70

13

7.7

01

20

.20

95

.50

Nb

46

.60

16

.70

16

.10

20

.90

19

.00

16

.70

20

.70

18

.00

18

.10

20

.80

20

.50

28

.50

24

.60

18

.70

Sn

7.1

01

.10

1.8

01

.80

2.1

22

.20

2.4

02

.10

1.1

00

.90

0.9

01

.30

1.2

01

.20

Cs

2.6

04

.60

2.6

09

.90

3.3

03

.20

3.7

06

.80

4.8

05

.00

2.6

05

.50

3.7

08

.90

La

18

.00

30

.10

26

.90

47

.20

26

.00

31

.00

24

.60

34

.00

28

.70

31

.90

39

.60

18

.50

21

.10

32

.80

Ce

50

.10

49

.90

49

.90

87

.40

55

.40

46

.67

42

.40

55

.70

42

.70

50

.80

62

.80

36

.60

36

.40

53

.10

Hf

6.0

03

.90

5.1

06

.80

3.4

03

.50

2.6

04

.10

2.5

04

.00

4.0

03

.70

3.9

03

.70



Tab

le1

–continued

GD

09

GD

11

GD

17

GD

22

GD

50

GD

52

GR

02

GR

04

GR

05

GR

06

GR

07

GR

08

GR

12

GR

13

Ta

7.3

04

.40

4.8

05

.80

6.4

56

.30

6.5

07

.20

5.9

03

.00

4.5

04

.60

2.5

04

.20

Te

1.2

00

.60

1.2

01

.20

1.4

01

.22

1.2

01

.30

0.9

01

.20

1.0

01

.20

1.2

01

.80

Pb

1.4

07

.60

7.0

05

.30

2.4

02

.60

2.2

05

.00

3.1

05

.00

5.3

04

.70

6.6

05

.60

Bi

0.6

00

.60

0.5

00

.60

0.7

60

.64

0.5

00

.70

0.8

00

.50

0.7

00

.50

0.4

00

.50

Th

6.3

09

.80

10

.50

13

.30

13

.20

11

.00

13

.20

12

.60

21

.40

25

.90

15

.50

17

.30

17

.00

13

.20

U4

.80

3.6

02

.10

2.9

02

.30

2.5

01

.70

2.2

02

.80

2.9

02

.90

4.4

03

.20

2.6

0

GR

14

GR

18

GR

21

GR

25

GR

49

GR

51

GR

53

GR

54

GR

55

GR

56

GR

57

GR

58

GR

59

GR

60

SiO

26

8.1

36

6.9

36

8.6

56

7.1

26

7.9

26

6.1

26

6.3

26

6.6

96

5.9

86

6.5

46

6.7

66

6.5

46

6.1

26

6.5

5A

l 2O

31

5.0

41

8.9

01

6.0

41

5.6

81

8.3

61

8.6

81

8.6

01

8.7

01

8.6

11

9.0

31

8.8

61

8.4

81

8.8

71

8.7

2F

e 2O

32

.81

3.3

32

.52

3.2

03

.10

2.9

62

.92

2.8

52

.81

2.8

02

.79

2.7

22

.69

2.7

6M

nO

0.0

60

.03

0.0

40

.04

0.0

20

.04

0.0

20

.04

0.0

20

.01

0.0

50

.01

0.0

40

.02

Mg

O1

.19

0.8

90

.99

1.1

10

.45

0.5

10

.57

0.5

00

.49

0.7

80

.80

0.6

70

.90

0.8

5C

aO2

.57

1.2

62

.80

2.3

42

.47

2.4

81

.88

2.1

12

.07

2.1

32

.45

2.0

81

.96

2.0

1N

a 2O

4.5

02

.91

4.7

84

.04

3.9

04

.30

4.4

84

.47

4.5

34

.20

4.2

24

.31

4.3

54

.22

K2O

3.8

64

.08

3.1

24

.48

2.2

63

.49

3.5

93

.52

3.6

83

.71

3.7

13

.73

3.7

53

.62

TiO

20

.27

0.3

50

.30

0.3

10

.26

0.2

50

.22

0.2

30

.19

0.1

80

.25

0.2

60

.27

0.2

5P

2O

50

.19

0.1

90

.18

0.1

80

.02

0.1

60

.13

0.0

40

.04

0.1

70

.02

0.0

40

.01

0.0

2L

OI

0.7

80

.92

0.8

00

.87

1.7

50

.79

0.8

60

.91

0.6

50

.26

0.7

70

.85

0.8

00

.65

To

tal

99

.41

99

.79

10

0.2

29

9.3

61

00

.51

99

.78

99

.59

10

0.0

49

9.0

79

9.8

21

00

.68

99

.68

99

.75

99

.68

Alk

8.3

76

.99

7.9

08

.52

6.1

67

.80

8.0

87

.99

8.2

07

.92

7.9

38

.04

8.1

07

.85

Mg

#0

.35

0.2

50

.33

0.3

10

.16

0.1

80

.20

0.1

80

.18

0.2

60

.27

0.2

40

.30

0.2

8F

eþM

g4

.00

4.2

23

.51

4.3

13

.55

3.4

73

.48

3.3

53

.30

3.5

83

.59

3.3

93

.59

3.6

1C

NK

10

.94

8.2

51

0.7

01

0.8

68

.63

10

.28

9.9

61

0.1

01

0.2

71

0.0

51

0.3

81

0.1

21

0.0

69

.85

Ba

58

7.0

04

57

.00

56

6.4

06

85

.70

41

2.0

04

10

.00

40

1.0

03

98

.00

35

4.0

03

65

.00

38

7.0

04

12

.00

42

1.0

04

27

.00

Sr

45

8.3

01

99

.40

48

5.6

04

93

.40

34

2.0

03

65

.00

36

1.0

03

61

.00

37

6.0

03

89

.00

34

1.0

03

32

.00

36

5.0

03

77

.00

Y1

4.2

01

4.6

01

3.1

01

6.6

01

4.5

01

5.6

51

6.4

31

7.7

61

7.0

01

8.7

01

.68

21

.00

20

.10

22

.00

Zr

16

1.6

02

12

.10

20

8.0

02

05

.60

17

6.0

01

93

.00

18

5.0

01

88

.00

19

0.0

01

89

.00

19

5.0

01

91

.00

19

3.0

01

92

.00

Co

25

.40

14

.70

36

.50

34

.10

22

.00

24

.20

23

.10

27

.00

25

.00

23

.60

26

.00

26

.30

24

.30

24

.11

Zn

25

.10

40

.10

25

.30

27

.20

21

.00

12

.00

13

.00

11

.20

13

.30

14

.00

12

.00

14

.40

16

.30

12

.03

Ga

16

.50

16

.60

18

.00

16

.80

14

.34

13

.33

15

.32

14

.32

12

.54

13

.22

13

.32

11

.20

15

.30

14

.25



Tab

le1

–continued

GR

14

GR

18

GR

21

GR

25

GR

49

GR

51

GR

53

GR

54

GR

55

GR

56

GR

57

GR

58

GR

59

GR

60

Ge

1.4

01

.10

0.7

00

.90

1.2

01

.30

1.3

21

.20

1.3

11

.40

1.4

31

.33

1.3

11

.23

Rb

10

5.6

01

19

.00

79

.10

11

9.5

09

8.3

01

23

.00

11

2.0

01

27

.00

12

1.0

01

28

.00

12

2.0

09

8.0

01

10

.00

11

2.0

0N

b2

0.5

02

0.9

01

5.8

02

0.5

02

1.0

01

6.3

02

0.1

01

7.0

01

6.6

51

7.3

01

8.3

01

5.7

01

8.3

01

3.2

3S

n1

.00

1.3

00

.90

3.0

02

.30

2.5

42

.54

2.1

22

.54

2.2

02

.34

2.4

32

.43

2.5

4C

s4

.40

8.1

06

.70

4.0

03

.20

3.0

02

.40

3.4

03

.80

3.5

03

.30

3.0

03

.10

3.2

0L

a3

0.5

05

2.9

04

0.3

04

2.6

02

8.0

03

2.0

03

3.0

03

6.1

02

6.4

03

0.0

02

6.6

02

8.3

02

9.3

02

7.3

0C

e5

1.8

08

5.6

06

2.6

06

9.8

05

3.0

05

3.5

04

9.5

45

1.3

25

3.4

35

2.4

34

8.5

04

8.4

55

3.4

35

1.2

2H

f3

.80

4.2

03

.60

4.0

02

.40

2.5

03

.70

3.3

23

.60

3.5

00

.39

3.4

03

.65

3.7

6T

a4

.90

3.8

04

.70

4.8

06

.50

6.4

06

.70

6.8

07

.50

7.5

07

.50

6.8

06

.30

6.9

8T

e1

.20

1.2

01

.20

0.9

01

.32

1.2

01

.70

0.9

80

.94

1.3

41

.30

1.1

01

.70

1.6

3P

b6

.00

3.1

03

.80

6.5

02

.45

2.4

02

.70

2.3

02

.22

2.8

02

.60

2.1

22

.51

2.4

1B

i0

.60

0.5

00

.40

0.6

00

.56

0.6

50

.65

0.6

50

.76

0.6

00

.87

0.8

70

.81

0.5

4T

h1

6.7

01

4.8

01

3.9

01

4.6

01

2.3

01

2.0

01

4.3

01

4.0

01

4.1

01

2.3

01

1.3

31

2.3

41

1.3

41

2.3

4U

4.4

03

.10

2.2

02

.90

3.2

02

.40

3.7

03

.65

3.6

53

.65

3.6

53

.65

4.2

33

.90

GR

61

GR

62

GR

63

GR

64

GR

65

GR

66

GR

67

GR

68

GR

69

GR

70

GR

71

GR

72

GR

73

GR

74

SiO

26

6.7

66

6.4

36

5.1

46

6.4

16

6.5

46

6.3

26

6.3

36

7.2

36

8.3

26

7.2

36

6.4

56

7.6

76

6.4

76

6.2

4A

l 2O

31

8.7

51

9.8

81

9.8

11

9.3

31

9.1

61

8.7

51

9.5

11

8.1

61

8.3

31

8.5

31

8.8

01

8.7

11

9.6

41

9.5

0F

e 2O

32

.76

2.5

02

.95

2.5

52

.63

2.7

42

.73

2.5

72

.51

2.6

13

.13

2.6

72

.62

2.9

1M

nO

0.0

20

.01

0.0

30

.05

0.0

10

.04

0.0

10

.02

0.0

20

.02

0.0

20

.06

0.0

70

.02

Mg

O0

.79

0.9

81

.01

1.0

11

.13

0.7

30

.85

1.0

10

.84

0.7

60

.67

0.6

20

.52

0.5

9C

aO2

.01

1.3

21

.29

1.1

51

.13

1.2

61

.24

1.0

10

.94

1.2

81

.26

1.0

41

.09

0.8

1N

a 2O

4.2

44

.44

4.3

94

.47

4.4

74

.55

4.7

24

.59

4.6

04

.43

4.3

84

.22

4.2

14

.54

K2O

3.6

73

.79

3.8

63

.94

3.6

53

.75

3.9

33

.85

3.9

43

.90

3.9

84

.07

4.2

14

.36

TiO

20

.16

0.1

50

.12

0.1

40

.15

0.1

90

.12

0.1

40

.13

0.1

50

.12

0.2

50

.24

0.1

3P

2O

50

.17

0.1

10

.12

0.1

30

.09

0.0

70

.09

0.1

40

.09

0.0

20

.14

0.1

80

.11

0.1

7L

OI

0.6

40

.72

0.7

30

.75

0.7

40

.76

0.3

00

.76

0.4

20

.30

0.9

10

.66

0.6

40

.78

To

tal

99

.97

10

0.3

49

9.4

59

9.9

19

9.7

09

9.1

79

9.8

29

9.4

71

00

.15

99

.24

99

.88

10

0.1

49

9.8

21

00

.06

Alk

7.9

28

.23

8.2

58

.41

8.1

28

.31

8.6

58

.44

8.5

58

.32

8.3

68

.29

8.4

28

.90

Mg

#0

.27

0.3

30

.30

0.3

30

.35

0.2

50

.28

0.3

30

.30

0.2

70

.21

0.2

30

.20

0.2

0F

eþM

g3

.55

3.4

83

.96

3.5

53

.76

3.4

73

.58

3.5

83

.35

3.3

83

.81

3.2

93

.14

3.5

0



Tab

le1

–continued

GR

61

GR

62

GR

63

GR

64

GR

65

GR

66

GR

67

GR

68

GR

69

GR

70

GR

71

GR

72

GR

73

GR

74

CN

K9

.92

9.5

59

.54

9.5

59

.24

9.5

79

.89

9.4

59

.49

9.6

19

.62

9.3

39

.51

9.7

1B

a4

18

.00

41

5.0

04

25

.00

43

0.0

04

34

.00

39

8.0

03

89

.00

40

5.0

04

07

.00

41

8.0

04

19

.00

41

7.0

04

22

.00

42

2.0

0S

r3

87

.00

35

3.0

03

22

.00

36

5.0

03

54

.00

32

1.0

03

52

.00

34

1.0

03

34

.00

35

4.0

03

40

.00

35

1.0

03

42

.00

32

1.0

0Y

26

.30

23

.65

23

.25

22

.60

21

.30

21

.00

18

.30

16

.00

19

.00

22

.01

16

.30

15

.43

16

.43

14

.87

Zr

19

4.0

01

92

.00

19

3.0

01

99

.00

19

2.0

01

93

.00

19

1.0

01

92

.00

18

7.0

01

89

.00

18

7.0

01

84

.00

18

7.0

01

85

.00

Co

23

.20

24

.54

25

.11

23

.11

23

.00

26

.00

27

.00

23

.00

27

.00

22

.00

27

.00

25

.00

22

.76

24

.70

Zn

12

.60

11

.00

16

.00

18

.00

21

.00

14

.00

16

.00

13

.00

13

.30

12

.20

12

.65

12

.65

13

.21

12

.54

Ga

13

.54

13

.21

12

.76

17

.98

14

.65

16

.54

12

.00

18

.30

16

.00

17

.00

14

.98

15

.20

14

.76

13

.76

Ge

1.4

31

.34

1.1

21

.54

1.3

21

.23

1.2

11

.22

1.5

41

.30

1.2

01

.50

1.6

01

.20

Rb

12

3.0

01

21

.00

12

5.0

01

26

.00

12

4.0

01

22

.00

12

6.0

01

23

.00

12

6.0

01

28

.00

12

2.0

01

27

.00

12

8.0

01

29

.00

Nb

13

.90

17

.00

17

.30

12

.98

16

.32

18

.00

16

.30

15

.32

16

.32

17

.32

18

.32

15

.32

15

.87

16

.30

Sn

2.5

03

.03

3.3

93

.20

2.4

02

.54

2.5

42

.54

2.4

72

.54

2.4

42

.44

2.6

52

.55

Cs

3.8

73

.40

2.7

52

.65

3.9

82

.87

3.7

82

.63

2.5

43

.28

3.1

73

.19

3.2

03

.03

La

27

.30

26

.32

29

.54

32

.00

31

.00

30

.00

32

.10

32

.30

31

.30

32

.30

28

.30

27

.10

26

.90

28

.87

Ce

52

.11

50

.35

51

.40

49

.65

51

.60

50

.00

46

.70

43

.20

48

.50

44

.40

43

.00

45

.00

46

.70

52

.00

Hf

3.5

43

.35

3.6

13

.76

4.0

23

.20

3.7

63

.53

3.6

53

.69

3.2

53

.26

3.2

23

.24

Ta

7.5

07

.40

7.9

47

.40

7.5

47

.45

6.8

46

.64

6.9

26

.72

5.8

75

.98

5.8

76

.05

Te

1.7

31

.31

1.8

31

.33

1.3

71

.73

1.2

21

.20

1.2

31

.13

1.3

00

.93

1.3

81

.98

Pb

2.3

12

.22

2.1

22

.40

2.1

32

.11

2.6

02

.17

2.3

22

.43

2.2

02

.24

2.4

71

.76

Bi

0.4

80

.87

0.8

10

.84

0.7

80

.67

0.1

90

.59

0.5

10

.63

0.7

00

.76

0.8

40

.64

Th

12

.34

13

.21

11

.32

12

.32

13

.20

12

.40

12

.30

13

.32

14

.20

13

.22

12

.33

13

.43

13

.43

14

.21

U3

.87

4.2

13

.00

4.3

24

.50

4.2

04

.21

3.7

83

.87

4.2

04

.10

4.2

34

.24

4.5

6

GR

75

DB

15

DB

19

DB

23

HF

48

SiO

26

6.5

85

4.7

64

3.5

44

1.9

89

4.6

5A

l 2O

31

9.4

81

8.4

21

1.0

02

.57

2.1

8F

e 2O

32

.51

9.8

09

.68

18

.15

1.4

2M

nO

0.1

20

.17

0.1

70

.85

0.0

1M

gO

0.6

38

.21

19

.09

6.9

10

.83

CaO

1.1

00

.95

15

.50

28

.54

0.0

2N

a 2O

4.4

12

.67

0.0

60

.08

0.0

6K

2O

4.2

72

.88

0.0

70

.18

0.2

2



Tab

le1

–continued

GR

75

DB

15

DB

19

DB

23

HF

48

TiO

20

.25

1.2

00

.31

0.1

10

.12

P2O

50

.18

0.5

20

.01

0.0

50

.04

LO

I0

.64

0.8

90

.68

0.8

30

.77

To

tal

10

0.1

71

00

.46

10

0.1

11

00

.25

10

0.2

1

Alk

8.6

85

.54

0.1

40

.26

0.2

9M

g#

0.2

40

.51

0.7

10

.33

0.4

3F

eþM

g3

.14

18

.01

28

.77

25

.06

2.2

5C

NK

9.7

96

.50

15

.63

28

.80

0.3

1

Ba

43

2.0

07

42

.00

6.8

01

6.8

09

3.8

0S

r3

53

.00

10

1.9

01

13

.70

17

.50

3.7

0Y

17

.10

27

.40

8.3

07

.60

3.6

0Z

r2

01

.00

30

7.8

06

.20

50

.30

37

.80

Co

27

.00

35

.30

91

.30

26

.00

40

.50

Zn

14

.21

73

.10

60

.30

89

.40

22

.40

Ga

13

.25

18

.60

9.6

01

1.5

03

.00

Ge

1.2

01

.00

1.3

06

.90

1.6

0R

b1

30

.00

71

.20

1.2

02

.40

17

.20

Nb

17

.65

20

.90

0.9

06

.10

2.3

0S

n3

.07

1.8

00

.90

18

.20

0.7

0C

s2

.87

2.6

02

.60

3.2

06

.90

La

30

.08

37

.10

4.9

06

.00

11

.40

Ce

51

.00

77

.60

5.8

07

.00

20

.80

Hf

3.1

65

.90

4.1

03

.20

1.3

0T

a6

.54

4.3

01

1.0

07

.10

4.9

0T

e1

.73

1.2

01

.00

1.2

01

.20

Pb

1.5

06

.10

2.6

01

.50

3.8

0B

i0

.74

0.7

00

.60

0.9

01

.20

Th

14

.30

10

.50

1.5

01

.50

1.0

0U

4.0

82

.30

1.5

05

.80

1.5

0

GD

,G

rano

dio

rite

;G

R,

Gra

nit

e;D

B,

Dia

bas

e;H

F,

Ho

rnfe

ls.



Geochemistry of the Horoz pluton

Major and trace-element analyses of a total of 42 representative samples were performed

using XRF and ICP in Petrology Research Laboratory housed in the Department of

Geological Engineering at the University of Ankara (Turkey). The results of these

analyses are given in Table 1. Analytical methods are described in Oner et al. (2009, this

issue).

As the SiO2 contents of the analysed rocks decrease systematically from the

granodiorite (65.7–59.0 wt%) to the granite series (71.0–65.1 wt%), the Na2O þ K2O

Figure 7. Alkali vs. silica diagram of Irvine and Baragar (1971), with the Horoz samples plottingmainly in the sub-alkaline field.

Figure 8. AFM diagram of Irvine and Baragar (1971). Granite–granodiorite samples from theHoroz pluton define a nearly linear trend in the calc-alkaline field.



contents increase (Table 1). On the total alkali vs. silica (TAS) diagram, the granodiorite

and granite samples plot in the sub-alkaline field (Figure 7). They are calc-alkaline

in nature and display a linear trend, suggesting a transitional change in composition

(Figure 8). The analysed granodiorite and granite samples plot in the fields of high-K calc-

alkaline and high-K shoshonitic series on the SiO2 vs. K2O diagram (Figure 9). In general,

most of the granitic and granodioritic samples have high-Al2O3 contents (15.90–20.06

wt%), and these high-Al rocks have lower SiO2, MgO, and Mg numbers (Table 1) and

lower concentrations of compatible elements such as Cr, Ni, and Sc.

Figure 9. SiO2 vs. K2O diagram of Rickwood (1989). Granite–granodiorite samples from theHoroz pluton plot mainly in the high-K calc-alkaline field with few samples falling into the medium-Kcalc-alkaline and shoshonitic fields.

Figure 10. SiO2 versus Fe2O3 þ MgO diagram.



The analysed samples display a linear trend on the SiO2 vs. Fe2O3 þ MgO diagram

(Figure 10), showing increases in their Fe2O3 þ MgO, as SiO2 decreases in the granitic to

granodioritic rocks. Conversely, decreasing Al2O3 contents from the granodiorite to

granite correlate with decreases in the total amount of CNK (CaO þ Na2O þ K2O;

Figure 11).

The Fe2O3, TiO2, MgO, CaO, and Al2O3 contents decrease with increasing SiO2 in

the Harker diagrams, whereas the K2O and Na2O appear to increase with increasing

SiO2 values, although somewhat scattered (Figure 12(A)). This phenomenon suggests

that the Horoz pluton magmas may have involved crystal fractionation processes

coupled with assimilation of the host platform carbonates. There is a negative

correlation of Zr, Y, and Ta but a positive correlation of Th with increasing SiO2

contents (Figure 12(B)).

Figure 13 shows the distribution of inter-elemental patterns in granitoid rocks on an

ocean ridge granite (ORG)-normalized (hypothetical ORG) diagram. In general, all

samples of the granite and granodiorite series show enrichment in LILE and depletion in

HFSE relative to ORG (Figure 13), similar to the patterns of rocks formed in subduction

and/or collision tectonic environments (Cox 1987; Wilson 1989).

On the tectonic discrimination diagrams of Pearce et al. (1984), all analysed samples

of the granite and granodiorite plot within the volcanic arc granite þ collision

granite þ ocean ridge granite (VAG þ COLG þ ORG) fields based on the correlation

of Y and Nb with silica (Figure 14). The Y vs. Nd diagram is used to differentiate

VAG þ Syn-COLG, within-plate granite (WPG), and ORG affinities of the rocks, and the

Y þ Nb vs. Rb diagram is used to differentiate between VAG and ORG, WPG, and Syn-

COLG affinities. Most samples plot mainly in the VAG field, close to the intersection of

the Syn-COLG, WPG, and VAG fields, suggesting that their magmas may have been

derived from a subduction-metasomatized mantle source.

Figure 11. Shand’s index diagram for the Horoz granitoid (Shand 1927). A/CNK, molarAl2O3/(CaO þ Na2O þ K2O); A/NK, molar Al2O3/(Na2O þ K2O). Granite–granodioritesamples from the Horoz pluton plot both in the metaluminous and peraluminous fields, showing atransition from I-type to S-type granites.



Petrogenetic and tectonic evolution of the Horoz pluton

Petrogenesis

Geochemical features of the granite and granodiorite series of the Horoz pluton suggest

that the magmas of these rocks were derived from a mantle source that was enriched from

dehydration melting of metamorphosed basaltic (amphibolite and eclogite) and

sedimentary rocks, and that these magmas experienced fractional crystallization and

assimilation during their ascent through the continental crust. We used Y vs. Sr/Y, SiO2 vs.



MgO, and SiO2 vs. Mg# [MgO þ (0.79Fe2O3)] patterns to better understand the nature of

the magmas of the Horoz pluton (Figure 15(A–C)). Both granitic and granodioritic

samples of the Horoz pluton generally plot in the Adakite, the Archean Tonalite–

Trondhjemite–Diorite (TTD), and the Archean Tonalite-Trondhjemite-Granodiorite

Figure 12. Harker diagrams of the Horoz granitoid illustrating the variations of (a) major oxidesand (b) trace elements with SiO2.



(TTG) fields (Condie 2005; Thorkelson and Breitsprecher 2005). There is also a strong

geochemical resemblance between the Horoz granitoid rocks and the late Mesozoic

adakitic andesites from the Sulu collisional belt in eastern China (Figure 15). The adakitic

andesites in the Sulu orogenic belt were erupted after the continental collision between the

north China and Yangtze blocks in the Triassic, and their magmas were produced by

partial melting of a LILE- and LREE-enriched eclogitic lower continental crust (Guo et al.

2006). These authors suggested that delamination of the thickened lower crust led to

asthenospheric upwelling, which in turn induced melting of both the delaminated crust and

the eclogitic lower crust in the upper plate. We envision a similar tectonomagmatic

scenario for the adakitic Horoz granitoids. However, lower Sr/Y and La/Yb ratios (Figures 15

and 16) and lower MgO contents and Mg numbers of the Horoz granitoid rocks in

comparison to the typical adakites of southern Tibet (Gao et al. 2007) and elsewhere (Kay

1978; Kay and Kay 1993; Kay et al. 1993; Yogodzinski et al. 1995) indicate that the Horoz

magmas were strongly influenced by melt components derived from a subduction-

metasomatized mantle. This feature is reflected on the arc affinity of the Horoz granitoid

rocks and their geochemical resemblance to the Archean TTG and TTD (Figures 15 and

16; Rapp et al. 1991).

Tectonic model

We interpret the tectonomagmatic evolution of the early Eocene Horoz granitoid

within the regional geological framework of the ITSZ and the bounding Tauride and

CACC blocks. Our earlier studies of both the CACC and the Tauride ophiolites (TO)

Figure 13. ORG-normalized multi-element patterns for the granodiorite and granite samples fromthe Horoz pluton. ORG normalization values are from Pearce et al. (1984).



provide important constraints on the nature and timing of the tectonic, magmatic, and

metamorphic events that controlled the crustal evolution of the Tauride and CACC

continental blocks and the ITSZ. The occurrence along the entire ITSZ of the

Cenomanian–Turonian suprasubduction zone ophiolites and the spatially and

temporally associated metamorphic sole and blueschist rocks and the existence of

the latest Cretaceous granitic–monzonitic–syenitic plutons along the W–SW edge of

the CACC collectively indicate that the Tauride and CACC continental blocks were

separated by a Tethyan basin, the Inner Tauride Ocean (Sengor et al. 1984; Dilek and

Moores 1990; Dilek et al. 1999a) during much of the Mesozoic. During the Late

Cretaceous, partial melting of the subduction-metasomatized mantle beneath the CACC

produced the granitic suites of the Andean-type magmatism (Figure 17(a)); partial

subduction of the northern edge of the Tauride continental block at the subduction

zone dipping north beneath the CACC facilitated the formation of the high-P

blueschist metamorphic assemblages (e.g. Kiziltepe).

Following the demise of the Inner-Tauride oceanic lithosphere at the NE-dipping

subduction zone and the emplacement of the incipient arc–forearc ophiolites (Dilek and

Flower 2003) onto the northern edge of the Tauride block, subduction was arrested by

the underplating of the buoyant Tauride continental crust. The leading edge of the

subducted Tethyan slab broke off from the rest of the Tauride continental lithosphere,

resulting in the development of an asthenospheric window (Figure 17(b)). The

juxtaposition of this asthenospheric heat source against the overlying continental

Figure 14. Trace-element tectonic discrimination diagrams for the granodiorite and granitesamples from the Horoz pluton (fields from Pearce et al. 1984). VAG, volcanic arc granites; WPG,within plate granites; ORG, ocean ridge granites; Syn-COLG, syn-collision granites.



Figure 15. (a) Y vs. Sr/Y diagram, showing the distribution of the Adakite and classical arc seriesfields (after Defant and Drummond 1990; Defant et al. 2002). Horoz granite and granodioritesamples plot both in the Adakite and arc fields. Adakitic rocks from the Sulu orogenic belt (from Guoet al. 2006) and south Tibet (from Gao et al. 2007) are also shown for comparison. (b) MgO vs. SiO2

diagram, showing the fields that represent Adakites, experimental basaltic melts, Archean TTD, andarc xenolith glass inclusion. (c) Mg# vs. SiO2 diagram, showing the distribution of the Adakite,TTG , 3.0 and TTG . 3.0 fields. Mg# ¼ [MgO þ (0.79Fe2O3)]. After Defant and Kepezhinskas(2001).



lithosphere caused melting of the metasomatized mantle layers, producing the high-K

shoshonitic magmas of the monzonitic plutons and then the more-enriched alkaline

magmas of the syenitic plutons (Figure 17(b)). This process is similar to slab breakoff-

related collisional magmatism described from other orogenic belts (Davies and von

Blackenburg 1995 and references therein) and in the early Cenozoic of Western

Anatolia (Dilek and Altunkaynak 2007).

Continued convergence between the Tauride and CACC blocks resulted in a

continental collision in the Palaeocene that led to deformation, crustal thickening, and

metamorphism in the hinterland, and to southward transport of the already-emplaced TO

and melanges and flysch formation together with fold and thrust belt development in the

foreland (Figure 17(c)). Significant crustal thickening and development of a dense mafic

lower crust (eclogitic?) beneath the young orogenic belt resulted in foundering of the

orogenic root and eventually in partial delamination of the thickened lithosphere

(Figure 17(d)). Asthenospheric upwelling around and above the delaminated root provided

excess heat and enhanced geothermal gradient that triggered partial melting of the

hydrated lithospheric mantle and lower crustal rocks. This melting event produced the

high-Al adakitic magmas of the Horoz granitoid. The inferred asthenospheric upwelling

was also responsible for crustal uplift in the overlying Tauride and CACC blocks and for

thermal weakening of the orogenic crust, leading to tectonic extension in and across the

CACC (Figure 17(d)).

The Horoz pluton and the northern part of the Tauride block underwent a rapid

uplift in the footwall of the BFF during the Oligo-Miocene (Figure 17(e)). Apatite

fission track ages of 23.6 ^ 1.2 Ma from the Horoz granitoid support this interpretation

(Dilek et al. 1997). A south-dipping detachment fault along the southern edge of the

CACC accommodated top-to-the-south extension and crustal exhumation of the Nigde

core complex around 12–9 Ma (Figure 17(e); Whitney and Dilek 1997). Apatite fission

track ages from the Nigde massif are consistent with this timing and indicate

Figure 16. La/(Yb)N vs. (Yb)N diagram, showing the distribution of the Adakite and typical arcseries (modified after Jahn et al. 1981; Martin 1986). Horoz granite and granodiorite samplesstraddle the boundary between the Adakite and arc fields.



exhumation-induced slow to moderate cooling of its mid-crustal rocks (Fayon et al.

2001). The sinistral Ecemis Fault Zone facilitated the vertical displacement and

unroofing of high-grade metamorphic rocks in the eastern part of the Nigde massif

during the late Tertiary (Dilek and Whitney 1998). The UB transitioned from a

remnant, restricted basin in the Palaeogene to a terrestrial depocentre in the Neogene

that had a supradetachment basin character along its northern part overlying the Nigde

metamorphic core complex.

The Cappadocian Volcanic Province developed within a fault-controlled, broad

topographic depression during the middle to late Miocene (Figure 17(e)). The early and

intermediate stages of volcanism in Cappadocia (13.5–2.7 Ma) are mainly characterized

by the eruption of widespread ignimbrite and felsic lavas accompanied by high-K dacitic

and andesitic flows; intrusion of domes and plugs dominated the magmatic output during

these stages, which was contemporaneous with the extensional deformation and crustal

exhumation in and across Central Anatolia (Dilek et al. 1999b). The bimodal nature of

volcanism with increasing amounts of alkaline basaltic (OIB-like) lava eruption during

this phase suggests the involvement of the asthenospheric mantle in melt generation

(decompressional melting; Guctekin and Koprubasi 2009) in response to further

lithospheric extension and thinning (Figure 17(e)).

Conclusions

The early Eocene (55–54 Ma) Horoz granitoid is intrusive into late Palaeozoic–early

Mesozoic marble and schist units of the Central Tauride block in the Bolkar Mountains.

It is an ENE–WSW-trending, sill-like pluton exposed in the footwall of the north-dipping

BFF immediately south of the ITSZ. The Horoz pluton consists mainly of granitic and

granodioritic rocks that have high-K calc-alkaline to high-K shoshonitic bulk-rock

compositions. These rocks show enrichments in LILE and depletions in HFSE relative to

ORG, and their trace-element patterns suggest a subduction zone influence. Their high-Al

contents and lower SiO2, MgO, and Mg numbers, combined with the above geochemical

features, are reminiscent of adakitic rocks formed in convergent margin and collisional

tectonic settings.

The adakitic Horoz granitoid is a post-collisional pluton that was emplaced at

shallow crustal depths following the CACC–Tauride continental collision in the

Palaeocene. Asthenospheric upwelling, facilitated by the delamination of the

overthickened orogenic root, triggered partial melting of the mafic lower crust and

the hydrated lithospheric mantle, producing high-Al adakitic magmas of the Horoz

pluton. This asthenospheric upwelling was also instrumental in thermal weakening and

uplift of the orogenic crust, and in the onset of regional tectonic extension and core

complex formation. The Horoz pluton was unroofed by the early Miocene as a result of

both crustal uplift and erosion.

Figure 17. Sequential tectonic diagram, depicting the evolution of the ITSZ and the Tauride–CACC collisional orogenic belt. AFC, assimilation fractional crystallization; AHO, Alihocaophiolite; CACC, Central Anatolian Crystalline Complex; EF, Ecemis Fault; HG, Horoz granitoid;ITO, Inner-Tauride ophiolite; ITSZ, Inner-Tauride Suture Zone; KTB, Kiziltepe blueschist; MO,Mersin ophiolite; SMM, subduction-metasomatized mantle; SSZ, suprasubduction zone; TO,Tauride ophiolite; UB, Ulukisla Basin; UG, Uckapili granite. See text for discussion.

R



Acknowledgements

This study was supported in part by grants to Y.K. Kadioglu from the Scientific and TechnicalResearch Council of Turkey (TUBITAK) and Devlet Planlama Teskilati (DPT 2003-K-120-190-4-1),and to Y. Dilek from the National Science Foundation (NSF EAR-9317100); we acknowledge thesefunds gratefully. We thank our colleagues, S. Altunkaynak, H. Furnes, C. Genc, N. Gulec, and N. Ilbeyli,for insightful discussions on the Mesozoic–Cenozoic magmatism in Turkey. Constructive comments byC. Eddy helped us improve the paper.

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