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ARTICLE
Age and tectonomagmatic setting of the Eocene
Çöpler–Kabataşmagmatic complex
and porphyry-epithermal Au deposit, East
Central Anatolia, Turkey
Ali İmer &Jeremy P. Richards &Robert A. Creaser
Received: 5 March 2012 /Accepted: 25 September 2012
#Springer-Verlag Berlin Heidelberg 2012
Abstract The Çöpler epithermal Au deposit and related
subeconomic porphyry Cu–Au deposit is hosted by the
middle Eocene Çöpler–Kabataşmagmatic complex in cen-
tral eastern Anatolia. The intrusive rocks of the complex
were emplaced into Late Paleozoic–Mesozoic metamor-
phosed sedimentary basement rocks near the northeastern
margin of the Tauride-Anatolide Block. Igneous biotite from
two samples of the magmatic complex yielded
40
Ar/
39
Ar
plateau ages of 43.75±0.26 Ma and 44.19± 0.23, whereas
igneous hornblende from a third sample yielded a plateau
age of 44.13±0.38. These ages closely overlap with
40
Ar/
39
Ar ages of hydrothermal sericite (44.44±0.28 Ma)
and biotite (43.84±0.26 Ma), and Re–Os ages from two
molybdenite samples (44.6±0.2 and 43.9±0.2 Ma) suggest-
ing a short-lived (<1 my) magmatic and hydrothermal his-
tory at Çöpler. No suitable minerals were found that could
be used to date the epithermal system, but it is inferred to be
close in age to the precursor porphyry system. The Çöpler–
Kabataşintrusive rocks show I-type calc-alkaline affinities.
Their normalized trace element patterns show enrichments
in large ion lithophile and light rare earth elements and
relative depletions in middle and heavy rare earth elements,
resembling magmas generated in convergent margins.
However, given its distance from the coeval Eocene
Maden–Helete volcanic arc, the complex is interpreted to
be formed in a back-arc setting, in response to Paleocene
slab roll-back and upper-plate extension. The tectonomag-
matic environment of porphyry-epithermal mineralization at
Çöpler is comparable to some other isolated back-arc por-
phyry systems such as Bajo de la Alumbrera (Argentina) or
Bingham Canyon (USA).
Keywords Porphyry Cu–Au .Epithermal Au .
Tauride-AnatolideBlock .Centraleastern Anatolia .Turkey .
Middle Eocene
Introduction
Convergent and collisional orogens worldwide are host to a
wide range of magmatic rocks and associated mineral de-
posit types (e.g., Janković1977; Solomon 1990; Hedenquist
and Lowenstern 1994;Kesler1997; Barley et al. 2002;
Richards 2003a,2009; Bierlein et al. 2009). The Tethyan
Alpine–Himalayan Belt stands as one of the best examples
of such an orogenic system, with a large endowment of
magmatic-hydrothermal ore deposits including porphyry
Cu ± Mo ± Au and epithermal Au–Ag deposits (Janković
1977; Richards 2003b; Hou and Cook 2009;Yiğit 2009).
The recently discovered (in 1998) Çöpler gold deposit is
located ∼120 km southwest of the city of Erzincan in central
eastern Turkey (Fig. 1). The deposit consists of early, low-
grade porphyry-type Cu–Au mineralization overprinted by
intermediate-sulfidation epithermal-style Au mineralization.
Çöpler is the first significant gold discovery in eastern
Anatolia, a region which had remained mostly unexplored
Editorial handling: T. Bissig
Electronic supplementary material The online version of this article
(doi:10.1007/s00126-012-0444-1) contains supplementary material,
which is available to authorized users.
A. İmer :J. P. Richards (*):R. A. Creaser
Department of Earth and Atmospheric Sciences,
University of Alberta,
Edmonton, AB, Canada T6G 2E3
e-mail: Jeremy.Richards@ualberta.ca
A. İmer
e-mail: Imer@ualberta.ca
R. A. Creaser
e-mail: Robert.Creaser@ualberta.ca
Miner Deposita
DOI 10.1007/s00126-012-0444-1
prior to the late 1990s. With proven and probable reserves of
4.4 million ounces (Moz) Au equivalent (95.4 million met-
ric tonnes at 1.4 g/t Au; http://www.alacergold.com), Çöpler
currently ranks as the second largest gold deposit in Turkey
after the Kışladağporphyry Au deposit in western Anatolia
(430 million metric tonnes at 0.74 g/t Au; http://
www.eldoradogold.com).
Porphyry-epithermal mineralization at Çöpler is spatially
associated with the middle Eocene calc-alkaline Çöpler–
Kabataşintrusive complex, which was emplaced into a
narrow structural corridor along the northern flank of the
eastern Taurus mountain range. The magmatic complex lies
on the northeastern margin of the Tauride-Anatolide orogen-
ic block (TAB), within a region of structural complexity
where the modern Eurasia–Arabia collision zone is juxta-
posed against at least two different suture zones marking the
closure of former Neotethyan ocean basins (Figs. 1and 2).
During the Late Mesozoic–Cenozoic, basin closure along
both margins of the TAB was accompanied by northward
subduction and continental arc magmatism. This was fol-
lowed by Late Cretaceous collision in the Pontides, and
protracted periods of subduction-related and postsubduction
magmatism from the middle Eocene onwards.
Although these regional magmatic and tectonic events
have been the subject of several studies, understanding the
geotectonic significance of the Çöpler–Kabataşmagmatic
complex and nearby igneous rocks of similar age and chem-
istry has been hindered by a lack of geological and geochro-
nological data. The distal positioning of these intrusive
centers relative to the established Late Cretaceous–Eocene
arc magmatic belts in the Pontides and in southeast Anatolia
(Baskil–Maden; Fig. 1) has led to conflicting interpretations
regarding the nature and source of magmatism. Proposed
models for the Eocene central eastern Tauride magmatic belt
have ranged from typical continental arc settings (Özer and
Öner 1999) to postcollisional tectonic settings in which
EAFZ
NAFZ
BLACK SEA
CENTRAL
ANATOLIAN
BLOCK
PONTIDES
Diyarbakır
Çöpler
Karamadazı Maden
Baskil
GYFZ
MOFZ
36°E 38°E 40°E 42°E
41°
40°
Horoz
Erzincan
ARABIAN PLATFORM
38°N
40°N
42°N
BSZ
Eastern Pontide Magmatic Arc
CAFZ
UTM 37NUTM 36N
Karlıova junction
DFZ
NEAFZ
CATB
Helete
Tunceli
TAURIDE
ANATOLIDE
BLOCK
Afyon Zone
SAKARYA ZONE
iSTANBUL ZONE
DSFZ
CENTRAL
ANATOLIAN
BLOCK
ARABIAN PLATFORM
Menderes
Massif
BLACK SEA
MEDITERRANEAN SEA
Eastern Pontides
Central
Pontides
T
A
U
R
I
D
E
B
L
O
C
K
NAFZ
EAFZ
iAESZ
BSZ
IPSZ
0 km 400
BFZ
41°
40°
Eocene volcanic rocks
Eocene plutonic rocks
Late Cretaceous volcanic rocks
Late Cretaceous plutonic rocks
Cretaceous ophiolite complexes
Thrust fault
Strike-slip fault
International border
Undifferentiated basement and
cover rocks
N
0 km 100
A
N
A
T
O
L
I
D
E
Fig. 1 Simplified geological map showing the distribution of Late
Cretaceous to Eocene magmatic rocks and Cretaceous ophiolite com-
plexes of eastern Anatolia (modified from MTA 1989, and Bozkurt
2001). Areas shown in white represent undifferentiated Paleozoic–
Mesozoic basement rocks and Tertiary sedimentary/volcanic cover.
Karlıova junction marks the intersection of the North and East Anato-
lian Fault Zones. Box shows area of Fig. 2;inset map shows the major
tectonic elements of Turkey (Okay and Tüysüz 1999). Abbreviations:
BFZ Bornova Flysch Zone, BSZ Bitlis Suture Zone, CAFZ Central
Anatolian Fault Zone, CATB Central Anatolian Thrust Belt, DFZ
Dumlu Fault Zone, DSFZ Dead Sea Fault Zone, EAFZ East Anatolian
Fault Zone, GYFZ Göksu–Yazyurdu Fault Zone; İAESZ İzmir–
Ankara–Erzincan Suture Zone, IPSZ Intra-Pontide Suture Zone, MOFZ
Malatya–OvacıkFaultZone,NAFZ North Anatolian Fault Zone,
NEAFZ North East Anatolian Fault Zone
Miner Deposita
magmatism was induced by slab steepening and break-off
either (1) along the northern margin of the TAB (Önal et al.
2005) or (2) along the southern margin of the Tauride-
Anatolide Block (Kuşcu et al. 2007,2010).
This contribution provides new data on the age, geology, and
geochemistry of the Çöpler–Kabataşmagmatic complex and
associated porphyry deposit, in order to place it more clearly in
a regional tectonomagmatic and metallogenic context.
Tectonic Framework of Central Turkey
Turkey forms part of the extensive Alpine–Himalayan
Orogenic Belt that stretches from SW Europe to SE Asia
and is comprised largely of an assemblage of continental
fragments of Tethyan origin. These continental fragments,
once separated by Neotethyan basins, were amalgamated
during convergence between the Eurasian and Afro-
Arabian plates since at least late Mesozoic times (Fig. 2).
The ∼1500-km-long TAB, which hosts the Çöpler gold
deposit, is the largest of these continental fragments. During
the Late Permian–Early Triassic, the TAB and other
Cimmerian continents (including the laterally adjacent
Central Iranian Block) started to detach from the northern
Gondwana margin, initiating the southern Neotethys Ocean
basin (Şengör and Yılmaz 1981; Robertson and Dixon
1984; Stampfli et al. 1991). Closure of this ocean basin
commenced in the Early Cretaceous by north-dipping sub-
duction along the Bitlis Suture (Fig. 2), accompanied by
continental arc development (∼88–73 Ma) along the active
southern margin of the TAB (Baskil and Göksun-Afşin arcs,
Fig. 1;Şengör and Yılmaz 1981; Yazgan and Chessex 1991;
Yılmaz 1993;Rızaoğlu et al. 2009). At the end of the
Mesozoic, subduction-related calc-alkaline magmatic activ-
ity in the TAB was interrupted, possibly due to a decrease in
the rate of convergence between Arabia and Eurasia (Dewey
et al. 1989) or roll-back of the southern Neotethys slab
(Robertson et al. 2007; Kaymakçıet al. 2010). This subse-
quently led to widespread back-arc extension in the central
and eastern part of the TAB. In the Eocene, arc magmatism
along this margin resumed with eruption of the mafic-to-
intermediate composition Maden-Helete lavas, while back-
arc magmatism occurred intermittently along ENE-trending
transcurrent fault systems throughout the central and eastern
Taurides (Fig. 1; Yazgan 1984;Yılmaz 1993;Yiğitbaşand
Yılmaz 1996a; Elmas and Yılmaz 2003; Robertson et al.
2007). The Çöpler–Kabataşintrusive complex was formed
during this period in the TAB. Final closure of the southern
Neotethys Ocean along the Bitlis Suture took place during
the Miocene, when the Arabian Platform collided with the
TAB, which by this time was already part of the southern
Eurasian margin (Dewey et al. 1986;Şengör and Yılmaz
1981;Yiğitbaşand Yılmaz 1996b; Okay et al. 2010).
Contemporaneous with development of the southern
Neotethys Ocean in the Early Mesozoic, a back-arc basin
Pontides
Southern Neotethys
Pontides
Eastern Mediterranean
Northern Neotethys
Pontides
Southern Neotethys
Tauride-Anatolide Block
a Cretaceous
b Middle Eocene
c Early to Middle Miocene
Tauride-Anatolide Block
Afro-Arabian Continent
Tauride-Anatolide Block
Bitlis Suture
Arabian
Platform
Çöpler
Eastern Pontide Arc
Baskil Arc
Maden-Helete Arc
vvvvv
vvvv
v
vvvvvv
Cyprian Arc
Fig. 2 Simplified sketch diagram showing the Neotethyan evolution of
the Tauride-Anatolide Block and traces of Neotethyan suture zones from
aCretaceous to bMiddle Eocene, to cMiocene times. Also shown are the
approximate locations of the Çöpler deposit and the magmatic arcs that
are referred in the text. Note the southward jump of the southern Neo-
tethyan subduction zone during the Miocene (as shown in c)
Miner Deposita
known as the İzmir–Ankara–Erzincan Ocean (or northern
Neotethys; Fig. 2) was formed to the north of the TAB
(Robertson and Pickett 2000; Stampfli 2000; Tekin et al.
2002; Okay et al. 2006). This short-lived basin was closed in
the Cretaceous, first by intra-oceanic subduction of un-
known polarity, and then by northward subduction beneath
the Eurasian margin to form the Eastern Pontide Magmatic
Arc (Figs. 1and 2). Collision between the Pontides and the
TAB occurred in the Late Cretaceous, with obduction of
ophiolites onto the north-facing margin of the TAB (Figs. 1
and 2; Okay and Şahintürk 1997; Rice et al. 2006; Tüysüz
and Tekin 2007).
In the Paleocene, continued N–S-directed convergence
along the collisional belt resulted in transpressional deforma-
tion of the eastern Pontides, accompanied by folding, thrusting,
and uplift (Okay and Şahintürk 1997;Kaymakçıet al. 2000).
Collapse of the crustally thickened orogen occurred during the
middle Eocene, initiating an episode of postcollisional calc-
alkaline magmatism (50–41 Ma) mainly within ENE- and E–
W-trending extensional basins in the Pontides, and along the
İzmir–Ankara–Erzincan Suture Zone (Fig. 1; Okay and
Şahintürk 1997; Topuz et al. 2005;Keskinetal.2008).
The Miocene collision of Eurasia and Arabia along the
Bitlis Suture heralded the start of continent–continent (as
opposed to microplate–continent) collision in this region.
Collision was followed by uplift and extensive deformation
of eastern Anatolia and by westward migration of the main
Anatolian Block along two new regional strike-slip structures,
the North and East Anatolian Fault Zones. These faults are
roughly concurrent with the pre-existing Neotethyan sutures
(Fig. 1; Dewey et al. 1986). Widespread postcollisional vol-
canism occurred throughout Anatolia from the Miocene on-
wards. In eastern Anatolia, it has been suggested that this
volcanic activity was associated either with delamination of
the subcontinental lithospheric mantle (Pearce et al. 1990;
Göğüşand Pysklywec 2008) or with slab steepening and
break-off following collision (Keskin 2003;Şengör et al.
2003; Faccenna et al. 2006; Lei and Zhao 2007). In contrast,
in western Anatolia, this volcanism is attributed to Miocene to
Recent extensional tectonics related to the opening of the
Aegean back-arc (McKenzie and Yılmaz 1991).
Regional Geological and Structural Setting
of the Tauride-Anatolide Block
The eastern part of the TAB consists of a number of tecto-
nomagmatic and stratigraphic units including the Paleozoic–
Mesozoic Keban metamorphic massif, the Munzur alloch-
thon (Late Triassic–Cretaceous platform and deep marine
carbonates), Cretaceous ophiolite complexes, Late
Cretaceous and Cenozoic igneous rocks, and Cenozoic sed-
imentary cover rocks of the Sivas Basin; Fig. 3; Michard et
al. 1984; Özgül and Turşucu 1984; Özer 1994). The Munzur
allochthon was overthrust onto the Permo–Triassic meta-
morphic basement in the Late Cretaceous (Özgül and
Turşucu 1984), forming an extensive east–west-trending
mountain range between Tunceli to the south and Erzincan
to the north (Fig. 1). The steep topography of the allochthon
gradually diminishes outwards towards the surrounding
Late Cretaceous–Tertiary sedimentary basins.
The Munzur allochthon comprises a thick succession of
deep marine and platform-type carbonate rocks (Özgül and
Turşucu 1984; Tunç et al. 1991). Its northern flank has been
extensively overlain by tectonic slivers of Cretaceous ophio-
litic rocks and melange that were accreted during Late
Cretaceous dextral transpression associated with closure of
the İzmir–Ankara–Erzincan ocean basin (Özgül et al. 1981;
Yılmaz 1985; Kaymakçıet al. 2000;Yalınız et al. 2000;
Okay et al. 2001). Both carbonate rocks and obducted
ophiolites were later intruded and covered by igneous rocks
of varying composition during three distinct magmatic epi-
sodes: an early bimodal alkaline intrusive event during the
Late Cretaceous, a more voluminous calc-alkaline intrusive
and extrusive event in the Eocene, and a widespread bimod-
al volcanic event in the Miocene.
The oldest magmatic phase in the vicinity of the Munzur
allochthon is represented by sporadic exposures of Late
Cretaceous bimodal intrusions including the Murmano and
Dumluca plutons near Divriği, and several small intrusive
centers located near Hekimhan (Figs. 1and 3). Intrusive
rocks of this stage are typically alkaline syenite-quartz mon-
zonite and diorite-gabbro suites with ages between ∼76 and
74 Ma (Zeck and Ünlü 1991;Yılmaz et al. 1993; Kadıoğlu
et al. 2006; Boztuğet al. 2007;Kuşcu et al. 2007,2010;
Marschik et al. 2008; Özgenç and İlbeyli 2009; this study).
Emplacement of these bimodal plutons seems to coincide
with break-up and collapse of the thickened eastern TAB
crust, the result of which was a reversal in stress directions
and a switch from transpression to transtension. From Late
Cretaceous until middle Eocene time, this transtensional
period led to the opening of several ENE-trending
foreland-type sedimentary basins (Cater et al. 1991; Temiz
et al. 1993), and exhumation of metamorphic complexes
(Gautier et al. 2002; Umhoefer et al. 2007; Whitney et al.
2008), mainly along Cretaceous thrust fault systems reacti-
vated as sinistral strike-slip faults (Figs. 1and 3; Koçyiğit
and Beyhan 1998; Poisson et al. 1996; Fayon et al. 2001).
Eocene magmatic rocks are widely scattered throughout
the northeastern Taurides and include the Çöpler–Kabataş
magmatic complex, the Çaltıand Bizmişen plutons, and an
east–west-trending belt of volcano-sedimentary rocks that
crop out adjacent to the İzmir–Ankara–Erzincan Suture
Zone (Figs. 1and 3). Intrusive rocks consist of calc-
alkaline diorite, quartz diorite, granodiorite, and quartz
monzonite, and volcanic rocks range from basaltic andesite
Miner Deposita
to rhyolite (Özer and Öner 1999; Önal et al. 2005;Kuşcu et
al. 2007; Keskin et al. 2008). Although their geochemical
characteristics are similar to global arc magmas, the Eocene
igneous rocks do not form a continuous narrow magmatic
belt as in many volcanic arcs, but rather occur as isolated
intrusive and volcanic complexes localized in structurally
favorable sites and distal to the presumed coeval subduction
zone and arc to the south.
The Karamadazı, Horoz, and Doğanşehir plutons are
other regionally significant Eocene intrusive systems, which
follow the same general structural trend to the southwest
(Fig. 1; see discussion below). All three plutons are reported
to be Eocene in age (∼50–48 Ma), and consist of felsic to
intermediate subalkaline lithologies (Gençalioğlu-Kuşcu et
al. 2001; Karaoğlan and Parlak 2006; Karaoğlan et al. 2009;
Kadıoğlu and Dilek 2010;Kuşcu et al. 2010).
Throughout the northeastern TAB, much of the Late
Cretaceous–Middle Eocene magmatism appears to have been
controlled by two prominent ENE-trending structures, the
sinistral Central Anatolian and Göksu–Yazyurdu Fault
Zones (Fig. 1), which accommodated a component of the
transtensional deformation. Shallow level pluton emplace-
ment is favored at times of oblique transtensional or
transpressional movement (e.g., Hutton 1982;1990;Glazner
1991; Román-Berdiel et al. 1997; Tosdal and Richards 2001).
During the Eocene transtensional period, a total sinistral dis-
placement of 74 km is recorded along the Central Anatolian
Fault Zone (Koçyiğit and Beyhan 1998), but the offset along
the Göksu–Yazyurdu Fault Zone to the south is not known.
The northeastern TAB experienced a final stage of wide-
spread postcollisional magmatism in the Miocene, erupted
along strike-slip fault systems. For example, basaltic tra-
chyandesite to dacite volcanic rocks form the 19–11 Ma
Yamadağvolcanic center to the southwest of Çöpler
(Fig. 3; Arger et al. 2000; Kürüm et al. 2008; Ekici et al.
2009). These magmas are interpreted to have formed during
postcollisional readjustments by melting of subduction-
modified lithospheric sources remnant from earlier
Neotethyan subduction events (Arger et al. 2000; Keskin
2003; Kürüm et al. 2008; Ekici et al. 2009).
Local geological setting of the Çöpler Au deposit
The Çöpler gold deposit is located in the central eastern part
of the TAB, along the northern flanks of the Munzur
340000E380000E420000E 460000E 500000E
4360000N4310000N
38º00’E
39º00’N
39º00’E
Keban Dam
Çöpler
Hekimhan
GYFZ
MOFZ
Kemaliye
Euphrates R.
Sivas Sedimentary Basin
Munzur
Carbonate Platform
Yamada
Volcanic Center
zmir-Ankara-Erzincan Suture Zone
N
Oligocene-Pliocene sedimentary rocks
Miocene volcanic rocks
Eocene sedimentary rocks
Eocene volcanic/plutonic rocks
Late Cretaceous-Paleocene sedimentary rocks
Late Cretaceous plutonic rocks
Cretaceous ophiolite rocks and ophiolitic mélange
Mesozoic carbonate rocks
Paleozoic-Early Mesozoic metamorphic rocks
Fault (dashed when concealed or inferred)
Thrust fault
Strike-slip fault
Major deposit
Major mine
Quaternary
0 10 km 20
Fig. 3 Simplified geological map of the eastern Tauride-Anatolide
Block. Compiled from the 1:500,000 geological map of Turkey, Sivas,
and Erzurum quadrangles (MTA 2002a,b; UTM Zone 37N). Structural
data are modified from Kaymakçıet al. (2006). Abbreviations: GYFZ
Göksu–Yazyurdu Fault Zone, MOFZ Malatya–Ovacık Fault Zone
Miner Deposita
Mountains, roughly 3 km southeast of the Euphrates River
(Fig. 3). The deposit is spatially related to an Eocene com-
posite stock forming the northwestern extension of the
Çöpler–Kabataşmagmatic complex (Figs. 4and 5), which
intruded a basement of Late Paleozoic–Cretaceous sedimen-
tary and ophiolitic rocks (Figs. 3,4,5, and 6). The intrusive
system at Çöpler is exposed within a 1 ×2 km wide, bowl-
shaped, ENE-trending structural window (the Çöpler win-
dow; Figs. 4and 5), along which block-faulted rocks have
been exposed underneath the regional thrust sheet of the
Munzur carbonate allochthon. The intrusive complex
appears to postdate thrusting and locally intrudes the base
of the thrust sheet causing contact-metamorphism to marble.
Paleozoic–Mesozoic Basement Units
The basement in the Çöpler area consists of an 800-m-thick
succession of regionally metamorphosed Permo–Triassic
siliciclastic sedimentary rocks, which belong to the
Yoncayolu Formation of the Keban metamorphic massif
(Özgül and Turşucu 1984). This unit is exposed in the
western part of the Çöpler window and in the vicinity of
Kabataşvillage (Figs. 4and 5). The metasedimentary suc-
cession consists of uniformly alternating layers of shelf-type
clastic rocks, which underwent low-grade greenschist facies
metamorphism in conjunction with Late Cretaceous obduc-
tion of ophiolites onto the northern TAB margin (Özgül et
al. 1981; Özgül and Turşucu 1984). These rocks are char-
acterized by a mineral assemblage of chlorite + quartz ±
sericite ± epidote; however, brown-colored biotite-rich and
pale green-colored diopside-rich hornfels are locally devel-
oped at contacts with the Eocene intrusions.
Structurally overlying the metamorphic basement is the
Late Triassic to Cretaceous allochthonous Munzur carbon-
ate platform, which displays an overall younging trend from
south to north (Özgül and Turşucu 1984). The northern
section of this allochthon, which is exposed between
Çöpler and Kabataşvillages, consists of a 300-m-thick
succession of Cenomanian to Campanian rudist-bearing
limestones (Özgül and Turşucu 1984).Thebaseofthe
54
12
38
48
24
Çöpler Yakuplu
4365000N
460000E465000E
4360000N
Quaternary
Granodiorite porphyry
Hornblende diorite porphyry
Diorite porphyry
Quartz diorite
Conglomerate
Late Cretaceous ophiolite complexes
Jurassic-Cretaceous limestone
Eocene
Permian-Triassic metasedimentary rocks
Normal fault
0 1 2 km
Thrust fault
Settlement
Deposit
45 Dip/strike
N
Strike-slip fault
Fig. 4 Geological map of the
Çöpler–Kabataşmagmatic
complex, modified from Özer
(1994)
Miner Deposita
limestone sequence is poorly exposed, but in the southwest-
ern sector of the Çöpler window, metasedimentary rock
injections into the Munzur limestone were observed
(Fig. 7a). These textures are interpreted to reflect south-
1400
1300
1200
1200
1300
1300
1400
1400
1200
1400
1300
1200
1350
1350
1350
1250
1250
1350
Marble
Contact
Zone
Manganese
Mine Zone
Approximate outer
limit of
propylitic alteration
Outer limit of
potassic alteration
Approximate outer
limit of
phyllic alteration
Çöpler North
Fault
Çöpler South
Fault
55
30
15
50
70 75
459000458500458000
457500 459500 460000 460500
4363500 4364000 4364500
4363000
N
500 m
1300
Limestone
Marble
Hornblende diorite porphyry
Granodiorite porphyry
Permian-Triassic metasedimentar y rocks
Fault (dashed where probable)
Strike-slip fault
Stream
Quaternary
Jurassic-Cretaceous
Contour (m)
Dip/strike
Thrust fault
Sample location
Ore zones
Eocene
45
C-162: 43.90 ± 0.20 Ma (Re-Os)
C-161: 44.60 ± 0.20 Ma (Re-Os)
C-164: 43.75 ± 0.26 Ma (Ar-Ar)
C-169: 43.84 ± 0.26 Ma (Ar-Ar)
C-166: 44.13 ± 0.38 Ma (Ar-Ar)
C-138: 44.91 ± 0.16 Ma (Ar-Ar)
Main Zone
Fig. 5 Geological map of the Çöpler deposit, modified from a map
prepared by Anatolia Minerals Development Limited (UTM Zone
37N). The Çöpler intrusive system is exposed in the structural window
defined by the steeply-dipping Çöpler North and South Faults
dissecting the Paleozoic–Mesozoic basement lithologies. The extents
of the main alteration facies are outlined by surface projection of
drillhole data. Also shown are the sample locations for
40
Ar/
39
Ar and
Re–Os geochronology
Fig. 6 Photograph showing the main Çöpler window, looking east.
Dashed red lines indicate traces of the Çöpler North and South Faults.
Also outlined is the approximate extent of the porphyry–epithermal
mineralization (white line;∼900 m wide in this view). Resistant hills
lying to the south and north of these faults are carbonate rocks of the
Munzur platform. The main peak in the background (approximately
4 km to the east) is a Cretaceous ophiolite nappe thrust onto these
carbonate rocks. The low-lying area in the far left (northeast) is part of
the Tertiary Sivas Basin
Miner Deposita
vergent décollement thrusting of the carbonate platform
during the Campanian–Maastrichtian interval (Özgül et al.
1981; Özgül and Turşucu 1984). The limestones are meta-
morphosed to sugary-textured white marble for several hun-
dred meters around the intrusive contacts (Fig. 5).
The Eocene Çöpler–KabataşMagmatic Complex
The Çöpler–Kabataşmagmatic complex intrudes the
Paleozoic–Mesozoic basement and overlying limestones as
several stocks that range in width from a few hundred
meters to several kilometers (Fig. 4). The intrusive rocks
are porphyritic to equigranular and intermediate composi-
tion, with ubiquitous and abundant plagioclase (andesine).
Quartz is also a common constituent of many of these
igneous lithologies, whereas K-feldspar was not observed
in unaltered rocks. Green-colored hornblende is the predom-
inant mafic phase and is present in most igneous lithologies,
whereas biotite and clinopyroxene are sparse.
Granodiorite porphyry The predominant phase in the
Çöpler–Kabataşmagmatic complex is a granodiorite por-
phyry that crops out in the main Çöpler window (Figs. 4and
5) and also near Kabataşvillage (Fig. 4). At Çöpler, this unit
is mainly exposed between the Çöpler North and South
Faults and also occurs as two lobes to the north and south
of these structures (Fig. 5). Granodiorite porphyry contains
abundant plagioclase, hornblende, and sparse biotite
phenocrysts set in a fine-grained groundmass of plagio-
clase, quartz, and lesser magnetite (Figs. 7b and 8a).
Euhedral to subhedral phenocrysts, ranging in size from
0.5 to 4 mm, make up to about 70 vol% of the rock.
Rounded, biotite-rich mafic xenoliths are occasionally
present in the granodiorite porphyry (Fig. 7b). Both in
Çöpler and Kabataş, granodiorite porphyry has under-
gone widespread hydrothermal alteration, and its least-
altered varieties display weak propylitic alteration with partial
replacement of mafic phases by chlorite and epidote, together
with sparse carbonate.
Fig. 7 Photographs of the main
lithologic units in the Çöpler–
Kabataşarea. aPermo-Triassic
metasedimentary basement
rocks and the overlying Munzur
limestone. The contact between
the two units is characterized by
deformation structures with
metasedimentary rock injec-
tions into the base of the over-
lying limestone (0457248E,
4362979N). bGranodiorite
porphyry intrusion from the
Çöpler main zone with
centimeter-sized biotite-rich
xenoliths (CDD-002, 293–
294 m; 0458972E, 4363881N).
cRelatively fresh hornblende
diorite porphyry from the man-
ganese mine zone (near
0460177E, 4364450N); the
slightly green coloration is due
to weak propylitic alteration of
the matrix. dWeakly propyli-
tized quartz diorite containing
hornblende-plagioclase-rich
xenoliths, exposed approxi-
mately 1 km to the east of the
Çöpler area (0461485E,
4365002N)
Miner Deposita
Hornblende diorite porphyry Hornblende diorite porphyry
is exposed as several small stocks in the northeast and
southwest sectors of the Çöpler window, in close association
with east–west-trending structures (Figs. 5and 7c). The
hornblende diorite porphyry contains abundant plagioclase
and hornblende phenocrysts within a fine-grained plagio-
clase–quartz–magnetite groundmass, with a significantly
lower phenocryst to groundmass ratio than the granodiorite
porphyry (Fig. 8b). Its relationship with the granodiorite
porphyry is unclear because it has mostly been intensely
altered. Least-altered samples of hornblende diorite porphyry
exhibit weak propylitic alteration as indicated by partial re-
placement of hornblende by chlorite and by the presence of
sparse epidote and carbonate in the groundmass.
Quartz diorite Quartz diorite occurs as NW-oriented lensoi-
dal bodies to the east of Çöpler, along the eastern side of a
NNW-trending structure (Fig. 4). This unit, previously
namedtheYakupluPluton(Özer1994; Özer and Öner
1999), consists of medium-grained, subhedral to euhedral
phenocrystic quartz, plagioclase, biotite, and hornblende,
with minor magnetite (Figs. 7d and 8c). Similar to the
granodiorite porphyry, quartz diorite also commonly con-
tains mafic enclaves (Fig. 7d). The quartz diorite exhibits
weak propylitic alteration readily recognized by crosscutting
veinlets of epidote, and mafic phenocrysts partially rimmed
by chlorite along with lesser amounts of epidote and
carbonate.
Diorite porphyry A relatively small stock of diorite porphy-
ry occurs to the northeast of Kabataş(Fig. 4). The diorite
porphyry is unaltered and consists of phenocrystic plagioclase
and clinopyroxene, in a groundmass of plagioclase micro-
crysts and substantial amounts of magnetite (Fig. 8d).
Euhedral plagioclase phenocrysts (0.1–0.5 mm) display either
polysynthetic twinning or oscillatory zoning, whereas clino-
pyroxene phenocrysts (0.2–0.5 mm) commonly occur in
glomeroporphyritic clusters.
Structure
The Çöpler intrusive system and the underlying basement
sequence are disrupted by several sets of high-angle faults.
The predominant structural features within the Çöpler
Fig. 8 Photomicrographs in aplane- and b–dcross-polarized light of
intrusive rocks from the Çöpler–KabataşMagmatic Complex. aGrano-
diorite porphyry from the Çöpler main zone, with biotite, hornblende,
and plagioclase phenocrysts, set in a groundmass of quartz, plagio-
clase, and magnetite (sample C-164; CDD-140, 106 m; 0458723E,
4363842N). bHornblende diorite porphyry from the Çöpler manga-
nese mine zone, with large hornblende and plagioclase phenocrysts, set
in a quartzofeldspathic groundmass (sample C-166; CDD-159, 26 m;
0460072E, 4364353N). cEquigranular quartz diorite from east of the
Çöpler window, with abundant plagioclase, biotite, and lesser quartz
and hornblende (sample CR-02; 0464761E, 4362274N). d
Clinopyroxene-bearing diorite porphyry from near Kabataş, with abun-
dant plagioclase and glomeroporphyritic clinopyroxene phenocrysts,
set in a glassy groundmass containing plagioclase microcrysts (sample
CR-03; 0467648E, 4362274N)
Miner Deposita
window are the ENE-trending Çöpler North and South
Faults that are related to Late Cretaceous–Eocene sinistral
deformation along the regional Göksu–Yazyurdu Fault Zone
(Fig. 5). NE–SW-trending extensional structures linking the
ENE-trending faults and E–W-trending sinistral faults also
developed in relation to middle Eocene transtensional defor-
mation, and facilitated shallow level magma emplacement and
hydrothermal mineralization at Çöpler. The NE–SW-trending
structures were later reactivated as reverse faults during later
minor contractional deformation. A fourth set of NNW-
trending faults truncates the granodiorite porphyry, and locally
offsets the earlier fault sets. All structures at Çöpler have been
reactivated on several occasions as evidenced by postem-
placement faulting and brecciation (Fig. 5).
Porphyry Cu–(Au) and epithermal Au mineralization
and alteration at Çöpler
A brief account of the alteration and mineralization styles at
Çöpler is provided below as a context for the geochrono-
logical data. A more detailed account will appear in a later
publication that focuses on ore formation.
Low-grade porphyry Cu–Au and superimposed epither-
mal Au mineralization occur in three different zones at
Çöpler: the Main Zone, the Marble Contact Zone, and the
Manganese Mine Zone (Fig. 5). Each zone displays distinct
hydrothermal alteration and mineralization features. The
Main Zone is characterized by high-temperature porphyry-
style alteration and Cu–(Au) mineralization centered around
the granodiorite porphyry. Here, early potassic alteration,
consisting of hydrothermal biotite and K-feldspar, forms an
inner core with associated quartz–magnetite–chalcopyrite–
pyrite ± molybdenite veinlets. The central potassic alteration
zone grades outwards into a laterally more extensive phyllic
alteration zone, which is readily distinguished by pervasive
sericite–quartz alteration and stockwork quartz–pyrite vein-
lets. Both alteration styles are enveloped by a propylitic
alteration assemblage of chlorite–epidote–carbonate devel-
oped peripheral to the Main Zone.
Epithermal-style mineralization is locally superimposed
on the early porphyry-style mineralization within the Main
Zone, but is best developed in the Marble Contact and
Manganese Mine Zones. The Marble Contact Zone is prox-
imal to the Main Zone and occupies the southeast margin of
the granodiorite porphyry, whereas the Manganese Mine
Zone is delimited by two E–W-trending secondary fault
systems and related extensional structures in the northeast-
ern sector of the property (Fig. 5). Both zones consist of Au-
bearing quartz–carbonate–sulfide ± barite veins and Au-
bearing manto-type carbonate replacement bodies of mas-
sive sulfides along the basal contact of the Munzur lime-
stone, which have largely been oxidized to gossan,
particularly in the Manganese Mine Zone. In these oxidized
zones, hypogene Mn carbonates (rhodochrosite or manga-
nocalcite) have been altered to manganese wad.
Sampling and analytical methods
Sample selection
Samples for petrographic, whole-rock geochemical, and
geochronological analysis were collected from diamond
drill core at the Çöpler deposit, and outcrop exposures
within or nearby the Çöpler–Kabataşmagmatic complex.
A summary of sample descriptions and locations is provided
in the Electronic Supplementary Material (ESM 1).
Twelve drill core and outcrop samples of least-altered (6)
and altered (6) igneous rocks from the Çöpler–Kabataş
magmatic complex were analyzed for their major and trace
element compositions. In addition, nine other samples of
fresh igneous rocks from elsewhere across the central east-
ern Taurides were collected and analyzed for comparison
purposes. Five of these regional samples were obtained from
Eocene intrusions near Bizmişen, Çaltı,Doğanşehir, Horoz,
and Karamadazı(Figs. 1and 3), three samples were collect-
ed from Late Cretaceous intrusions near Divriği, and one
sample was collected from the Miocene Yamadağvolcanic
center to the south of Divriği.
Altered samples from the Çöpler–Kabataşmagmatic
complex contain either an overprinting propylitic alteration
assemblage of chlorite, epidote, and carbonate, or a phyllic
alteration assemblage consisting of sericite replacing mafic
minerals and plagioclase, as reflected in their relatively high
loss-on-ignition values (Table 1).
Three samples containing igneous biotite and/or horn-
blende were selected for
40
Ar/
39
Ar incremental step-
heating analysis from a suite of least-altered plutonic rocks
from the Çöpler–Kabataşmagmatic complex. Two potassic
(biotite) and phyllic (sericite) altered samples were also
analyzed to constrain the timing of hydrothermal alteration
related to porphyry mineralization at Çöpler. In addition,
three samples of fresh rock containing igneous biotite and/or
hornblende were selected from the Bizmişen, Çaltı,and
Divriği intrusions in order to constrain the timing of intru-
sive magmatism elsewhere in the central eastern Taurides.
In order to constrain the timing of porphyry-style miner-
alization, two molybdenite samples obtained from quartz–
magnetite–sulfide veinlets within the Çöpler Main Zone
were analyzed by the Re–Os method.
Whole-rock geochemistry
Sample preparation and whole-rock geochemical analyses
of 21 igneous rock samples were carried out at Actlabs
Miner Deposita
Table 1 Major and trace element analyses of least-altered and altered igneous rocks from the Çöpler–Kabataşmagmatic complex and least-altered igneous lithologies from the surrounding area
Location Çöpler–KabataşDivriği YamadağÇaltıBizmişen Çöpler–
Kabataş
Doğanşehir KaramadazıHoroz
Sample no. C-014 C-104 C-163 C-164 C-166 C-169 C-173 CR-01 CR-02 CR-03 CR-05 CR-07 CR-08 CR-09 CR-10 CR-11 CR-12 CR-14 CR-24 CR-28 CR-31
Lithology
a
Hbl
Diorite
Porphyry
Grd.
Porphyry
Grd.
Porphyry
Grd.
Porphyry
Hbl
Diorite
Porphyry
Grd.
Porphyry
Grd.
Porphyry
Quartz
Diorite
Quartz
Diorite
Diorite
Porphyry
Quartz
Diorite
Quartz
Monzonite
Quartz
Monzonite
Alk.
Feld.
Granite
Basaltic
Andesite
Tonalite Diorite Hbl
Diorite
Porphyry
Tonalite Granite Granite
Alteration Least-alt. Least-alt. Alt.
(prop)
Alt.
(prop)
Alt.
(prop)
Alt. (K) Least-alt. Least-
alt.
Least-
alt.
Least-alt. Alt.
(phyl)
Least-alt. Least-alt. Least-
alt.
Least-alt. Least-
alt.
Least-alt. Alt.
(prop)
Least-alt. Least-alt. Least-
alt.
Weight % Method
(detection
limit)
SiO
2
Fusion-ICP
(0.01)
64.05 64.44 59.01 60.63 54.29 62.69 65.25 67.50 65.75 57.11 62.58 62.98 65.10 72.04 55.11 65.19 54.92 54.23 65.91 76.48 73.11
Al
2
O
3
Fusion-ICP
(0.01)
15.98 16.37 16.06 16.64 16.30 16.48 15.88 65.75 16.13 17.73 15.53 16.36 17.16 14.04 16.26 15.84 16.46 16.11 16.47 12.20 14.38
Fe
2
O
3(T)
Fusion-ICP
(0.01)
4.79 4.01 5.37 4.15 4.78 4.44 4.20 3.59 4.33 6.96 3.89 4.26 2.70 1.50 8.21 4.32 8.95 5.20 4.08 0.90 2.05
MnO Fusion-ICP
(0.001)
0.10 0.06 0.03 0.09 0.24 0.04 0.05 0.05 0.07 0.08 0.14 0.06 0.03 0.02 0.13 0.05 0.15 0.03 0.01 0.03 0.01
MgO Fusion-ICP
(0.01)
1.74 1.76 2.50 1.55 0.91 1.99 1.53 1.64 1.74 2.36 1.12 1.64 0.16 0.13 4.87 1.68 4.11 1.80 1.74 0.08 0.67
CaO Fusion-ICP
(0.01)
5.11 3.61 4.44 5.54 11.30 4.26 3.90 3.98 4.68 7.30 4.71 3.64 2.34 0.47 7.71 4.66 8.20 11.19 4.52 0.66 2.18
Na
2
O Fusion-ICP
(0.01)
3.37 3.02 1.76 2.50 2.65 2.78 2.85 3.50 3.60 3.36 2.92 4.23 4.97 3.88 3.78 3.51 3.59 2.57 4.33 3.30 3.82
K
2
O Fusion-ICP
(0.01)
3.05 3.50 2.75 2.82 2.98 3.46 3.11 2.44 2.20 1.76 3.21 4.37 5.46 6.05 1.14 2.27 1.77 4.09 1.76 4.72 3.52
TiO
2
Fusion-ICP
(0.001)
0.46 0.41 0.532 0.54 0.55 0.52 0.44 0.35 0.43 0.78 0.36 0.57 0.41 0.18 1.17 0.41 0.95 0.59 0.46 0.09 0.22
P
2
O
5
Fusion-ICP
(0.01)
0.21 0.18 0.24 0.26 0.25 0.23 0.19 0.11 0.15 0.16 0.16 0.25 0.10 0.02 0.20 0.15 0.18 0.26 0.15 0.03 0.11
LOI Fusion-ICP
(0.01)
1.61 2.77 6.50 5.18 6.65 3.90 3.30 1.19 0.85 1.45 4.49 0.45 1.83 0.71 0.61 1.09 0.89 4.59 0.81 0.25 0.64
Total 100.50 100.10 99.18 99.91 100.90 100.80 100.70 100.30 99.94 99.05 99.11 98.82 100.3 99.02 99.19 99.18 100.20 100.70 100.20 98.72 100.70
ppm (except
unless
indicated)
Au (ppb) INAA (1) 42 17 53 70 8 138 14 <d.l. <d.l. <d.l. 2 <d.l. 1 6 <d.l. <d.l. <d.l. 6 <d.l. <d.l. <d.l.
Ag MULT INAA/
TD-ICP-
MS (0.5)
<d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l.
As INAA (1) 2 2 <d.l. 14 8 3 6 <d.l. <d.l. <d.l. 2 3 7 8 <d.l. <d.l. <d.l. 8 <d.l. <d.l. 2
Ba Fusion-ICP
(1)
771 717 561 634 762 691 736 623 665 290 571 983 547 108 245 708 464 836 733 125 534
Be Fusion-ICP
(1)
2 2 2 2 2 2 2 111 25 7 6 2 1 1 3 3 3 3
Bi Fusion-ICP-
MS (0.1)
0.1 0.1 0.1 0.2 0.3 0.4 0.1 0.1 2.7 0.3 0.3 0.2 0.4 0.3 <d.l. 0.1 0.3 <d.l. <d.l. <d.l. <d.l.
Br INAA (0.5) <d.l. 0.9 <d.l. <d.l. 1 <d.l. 1.3 <d.l. 1 1.1 <d.l. <d.l. 1.4 2.1 <d.l. <d.l. 1.3 <d.l. <d.l. 1 <d.l.
Cd TD-ICP (0.5) <d.l. <d.l. <d.l. 0.5 <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. 0.5 <d.l. <d.l. <d.l. <d.l. <d.l. <d.l.
Co INAA (0.1) 9.2 5 10 10.6 16.9 10 7.1 7.4 8.7 15.7 8.6 7.8 2.9 2.5 31.3 8.8 21.8 14 8 3 5
Cr INAA (0.5) 10.8 7.7 8.2 6.6 <d.l. 5.5 5.6 9.5 13.5 5.7 13.6 14.9 4.8 6.7 135 14.5 22.7 29 61 66 26
Cs Fusion-ICP-
MS (0.1)
0.4 1.1 2.3 4.1 1.6 1.9 1.5 0.9 0.9 0.6 1.1 2.3 3.5 3.2 2.1 0.7 1 0.9 0.2 2.2 1
Cu TD-ICP (1) 185 149 561 221 20 734 246 143 26 23 40 9 9 9 38 9 14 33 13 4 3
Ga Fusion-ICP-
MS (1)
18 17 16 16 17 18 17 14 16 19 16 19 23 22 17 15 17 17 17 11 16
Ge 1.6 1.5 1.3 0.9 0.9 1.7 1.6 1.4 1.5 1.4 1.4 1.3 1.4 1.4 1.1 1.4 1.5 1.2 1.3 1.7 1.2
Miner Deposita
Table 1 (continued)
Location Çöpler–KabataşDivriği YamadağÇaltıBizmişen Çöpler–
Kabataş
Doğanşehir KaramadazıHoroz
Sample no. C-014 C-104 C-163 C-164 C-166 C-169 C-173 CR-01 CR-02 CR-03 CR-05 CR-07 CR-08 CR-09 CR-10 CR-11 CR-12 CR-14 CR-24 CR-28 CR-31
Lithology
a
Hbl
Diorite
Porphyry
Grd.
Porphyry
Grd.
Porphyry
Grd.
Porphyry
Hbl
Diorite
Porphyry
Grd.
Porphyry
Grd.
Porphyry
Quartz
Diorite
Quartz
Diorite
Diorite
Porphyry
Quartz
Diorite
Quartz
Monzonite
Quartz
Monzonite
Alk.
Feld.
Granite
Basaltic
Andesite
Tonalite Diorite Hbl
Diorite
Porphyry
Tonalite Granite Granite
Alteration Least-alt. Least-alt. Alt.
(prop)
Alt.
(prop)
Alt.
(prop)
Alt. (K) Least-alt. Least-
alt.
Least-
alt.
Least-alt. Alt.
(phyl)
Least-alt. Least-alt. Least-
alt.
Least-alt. Least-
alt.
Least-alt. Alt.
(prop)
Least-alt. Least-alt. Least-
alt.
Fusion-ICP-
MS (0.5)
Hf Fusion-ICP-
MS (0.1)
3.3 3.1 2.7 3.1 2.8 3.3 3.6 2.9 3 3.7 3.2 6.5 10.7 5.4 3.2 2.8 3.3 2.8 3.5 4.5 3
Hg INAA (1) <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l.
In Fusion-ICP-
MS (0.1)
<d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l.
Ir (ppb) INAA (1) <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. 21 <d.l. <d.l. <d.l.
Nb Fusion-ICP-
MS (0.2)
8.6 8.3 6.9 8.7 7.1 8.1 8.4 6.4 6.8 5.4 8.3 21 71.5 54.8 6.8 7.4 7.2 7.4 13.1 26.3 12.3
Ni TD-ICP (1) 3 3 3 74 96 21 22 3 5 3 8 5 1 1 45 5 5 5 9 4 4
Pb TD-ICP (5) 9 9 8 37 10 <d.l. 5 7 7 7 13 12 11 7 10 7 7 17 <d.l. 6 <d.l.
Rb Fusion-ICP-
MS (2)
63 76 66 83 68 101 91 62 61 40 49 167 218 308 36 54 36 82 36 190 80
S (%) TD-ICP
(0.001)
0.26 0.49 0.59 1.75 1.86 0.76 0.315 0.013 0.002 <d.l. 0.016 <d.l. 0.002 0.003 0.003 0.002 0.052 0.62 0.006 0.002 0.001
Sb INAA (0.1) <d.l. 0.5 <d.l. 1 0.8 0.3 0.3 <d.l. <d.l. 0.3 3 0.4 1.3 1.9 <d.l. <d.l. <d.l. 0.9 0.1 0.1 0.1
Sc INAA (0.01) 9.4 8.26 11.8 11.7 11.8 10.6 8.33 7.18 7.92 17.7 7.4 6.49 1.88 0.86 20.7 8.93 27.2 11.9 7.5 1.9 2.8
Se INAA (0.5) <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. 0.5 0.5 0.5 0.5
Sn Fusion-ICP-
MS (1)
<d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. 4 4 4 <d.l. <d.l. 1 1 1 2 1
Sr Fusion-ICP
(2)
549 449 263 408 615 426 391 271 394 473 214 348 202 34 333 347 350 642 356 40 439
Ta Fusion-ICP-
MS (0.1)
0.7 0.7 0.6 0.6 0.6 0.6 0.7 0.7 0.5 0.4 0.8 2.1 8.1 8.5 0.6 0.7 0.4 0.5 1.1 3.2 1.1
Th Fusion-ICP-
MS (0.05)
7.55 7.95 5.96 9.21 5.88 9.44 7.21 8.06 5.49 4.81 8.98 18.9 70.3 116 6.45 6.73 3.7 5.75 8.88 32.1 14.9
U Fusion-ICP-
MS (0.05)
1.95 1.89 1.56 3.25 3.3 2.33 2.44 1.62 1.55 1.6 2.74 7.89 12.5 8.26 2.19 1.69 1.35 2.19 1.95 7.93 2.69
V Fusion-ICP
(5)
102 84 134 130 131 117 86 67 75 193 63 60 17 <d.l. 154 79 241 188 79 5 33
W INAA (1) <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. <d.l. 2 <d.l. <d.l. <d.l. <d.l. 3 <d.l. <d.l. <d.l. <d.l. 2 <d.l. <d.l. <d.l.
Y Fusion-ICP
(1)
19 16 17 16 19 17 17 10 12 23 13 22 36 36 22 13 29 19 16 11 12
Zn MULT INAA/
TD-ICP-
MS (1)
32 283211648 34282529576324 15 10621952 37 21 14 20
Zr Fusion-ICP-
MS (1)
125 113 100 148 121 149 152 104 119 127 112 265 381 131 127 106 113 110 132 112 111
La Fusion-ICP-
MS (0.05)
27.1 20.3 21.7 20.1 27.7 25.2 26.4 21.7 22.7 18.4 26.5 40.8 65.6 79.3 16.3 23.7 19.6 25.7 28.4 30.5 32.5
Ce Fusion-ICP-
MS (0.1)
53.2 39.9 41.5 35.6 46.9 43.7 45.8 37.1 39 39.9 47.7 79.5 123 152 32.6 43.1 42 45.5 49 47.3 55.8
Pr Fusion-ICP-
MS (0.02)
5.94 4.51 4.59 4.1 5.29 4.92 5.19 3.72 4.07 4.91 4.91 8.42 11.8 13.4 3.76 4.47 5.28 4.7 4.61 4.52 5.2
Nd Fusion-ICP-
MS (0.05)
22.2 17.4 17.9 13.6 17.2 15.8 16.6 12.7 15.1 20.2 17.4 29.8 38.8 40.2 15 16 21.8 17.1 14.7 11.8 15.2
Sm Fusion-ICP-
MS (0.01)
4.21 3.54 3.48 2.82 3.59 3.26 3.31 2.14 2.85 4.43 3.1 5.37 6.63 7.06 3.45 2.96 4.99 3.79 2.98 1.83 2.73
Eu Fusion-ICP-
MS (0.005)
1.24 1.01 1.06 0.856 1.05 0.979 0.93 0.733 0.974 1.32 0.903 1.22 1.24 0.476 1.31 0.887 1.41 1.17 0.833 0.232 0.694
Miner Deposita
Table 1 (continued)
Location Çöpler–KabataşDivriği YamadağÇaltıBizmişen Çöpler–
Kabataş
Doğanşehir KaramadazıHoroz
Sample no. C-014 C-104 C-163 C-164 C-166 C-169 C-173 CR-01 CR-02 CR-03 CR-05 CR-07 CR-08 CR-09 CR-10 CR-11 CR-12 CR-14 CR-24 CR-28 CR-31
Lithology
a
Hbl
Diorite
Porphyry
Grd.
Porphyry
Grd.
Porphyry
Grd.
Porphyry
Hbl
Diorite
Porphyry
Grd.
Porphyry
Grd.
Porphyry
Quartz
Diorite
Quartz
Diorite
Diorite
Porphyry
Quartz
Diorite
Quartz
Monzonite
Quartz
Monzonite
Alk.
Feld.
Granite
Basaltic
Andesite
Tonalite Diorite Hbl
Diorite
Porphyry
Tonalite Granite Granite
Alteration Least-alt. Least-alt. Alt.
(prop)
Alt.
(prop)
Alt.
(prop)
Alt. (K) Least-alt. Least-
alt.
Least-
alt.
Least-alt. Alt.
(phyl)
Least-alt. Least-alt. Least-
alt.
Least-alt. Least-
alt.
Least-alt. Alt.
(prop)
Least-alt. Least-alt. Least-
alt.
Gd Fusion-ICP-
MS (0.02)
3.5 2.92 2.93 2.88 3.5 3.04 3.05 1.76 2.33 4.05 2.56 4.25 5.11 5.23 3.59 2.31 4.75 3.68 2.67 1.36 2.08
Tb Fusion-ICP-
MS (0.01)
0.59 0.49 0.51 0.49 0.57 0.51 0.52 0.3 0.39 0.71 0.42 0.74 0.98 1.12 0.67 0.41 0.86 0.57 0.45 0.24 0.32
Dy Fusion-ICP-
MS (0.02)
3.45 2.92 3.08 2.63 3.1 2.83 2.86 1.78 2.26 4.39 2.45 4.09 6.08 6.78 4.2 2.46 5.41 3.37 2.76 1.62 1.87
Ho Fusion-ICP-
MS (0.01)
0.69 0.58 0.61 0.53 0.61 0.57 0.57 0.37 0.47 0.88 0.5 0.8 1.23 1.31 0.84 0.49 1.09 0.69 0.58 0.39 0.39
Er Fusion-ICP-
MS (0.01)
2.03 1.79 1.79 1.6 1.83 1.75 1.74 1.18 1.4 2.61 1.54 2.42 4 4.23 2.46 1.48 3.25 2.09 1.8 1.48 1.27
Tl Fusion-ICP-
MS (0.05)
0.25 0.45 0.5 1 0.63 0.63 0.63 0.28 0.86 0.17 0.26 0.64 0.49 0.68 0.29 0.23 0.14 0.48 0.15 1.25 0.28
Tm Fusion-ICP-
MS (0.005)
0.31 0.283 0.27 0.244 0.279 0.261 0.266 0.188 0.224 0.39 0.237 0.373 0.659 0.697 0.364 0.238 0.489 0.31 0.277 0.293 0.203
Yb Fusion-ICP-
MS (0.01)
2.08 1.91 1.8 1.67 1.87 1.74 1.79 1.31 1.54 2.46 1.58 2.4 4.43 4.42 2.33 1.6 3.11 2.02 1.85 2.25 1.43
Lu Fusion-ICP-
MS (0.002)
0.32 0.285 0.282 0.289 0.305 0.29 0.302 0.219 0.24 0.363 0.247 0.367 0.641 0.614 0.355 0.249 0.46 0.32 0.306 0.38 0.241
Element concentrations below the detection limits are indicated as <d.l.
alk feld alkali feldspar, alt altered, grd granodiorite, hbl hornblende, ICP-MS inductively coupled plasma mass spectrometry, INAA instrumental neutron activation analysis, Kpotassic, LOI loss-on-
ignition, MULT multiple analytical methods, phyl phyllic, prop propylitic, TD total dis
a
Based on field names
Miner Deposita
Laboratories in Ontario, Canada. Major and trace element
compositions were obtained by a combination of inductively
coupled plasma (ICP), inductively coupled plasma emission
mass spectrometry (ICP-MS), and instrumental neutron ac-
tivation analysis (INAA) methods. Replicate analyses of
international standards indicate accuracy to within five rel-
ative percent for major and minor elements and to within ten
relative percent of the standard values for trace elements.
Results are listed in Table 1, and major oxide compositions
were recalculated to a volatile-free basis totalling 100 wt%
for plotting and classification purposes.
40
Ar/
39
Ar geochronology
Mineral separates of biotite, hornblende, and sericite were
prepared at the University of Alberta using crushing/sieving
and standard heavy liquid and magnetic separation techni-
ques. Individual grains were then hand-picked under a bin-
ocular microscope and sent to the Noble Gas Laboratory,
Pacific Centre for Isotopic and Geochemical Research,
University of British Columbia, Canada, for analysis by T.
Ullrich. Samples and flux monitors were wrapped in alumi-
num foil and sent for irradiation at the McMaster University
reactor in Canada. After irradiation, the samples were heated
in incremental steps under the defocused beam of a 10 W
CO
2
laser (New Wave Research MIR10) until fused. The Ar
isotopic composition of the gas emitted from each step was
analyzed using a VG5400 mass spectrometer. Isotopic ratios
were corrected for total system blank, mass spectrometer
sensitivity, mass discrimination, radioactive decay of
37
Ar
and
39
Ar during and subsequent to irradiation, and interfer-
ing argon from atmospheric contamination and the irradia-
tion of Ca, Cl, and K.
Re–Os geochronology
Selected quartz–magnetite–sulfide vein samples were pul-
verized in a porcelain disk mill, and molybdenite was then
separated from other sulfide and gangue phases using heavy
liquid techniques, magnetic separation, and by flotation
using high-purity water. Finally, molybdenite grains were
handpicked under a binocular microscope.
The
187
Re and
187
Os concentrations in molybdenite were
determined by isotope dilution mass spectrometry at the
University of Alberta Radiogenic Isotope Facility.
Dissolution of molybdenite separates and equilibration of
sample and tracer Re and Os were done using the Carius
tube method (Shirey and Walker 1995).
Samples were dissolved and equilibrated with a “mixed
double”spike containing a known amount of
185
Re +
188
Os
+
190
Os in 8 ml of reverse aqua regia (3:1, 16 N HNO
3
:12N
HCl) at 220 °C for 48 h. Os and Re were separated by
solvent extraction, microdistillation, and anion
chromatography techniques (Selby and Creaser 2004). The
purified Os and Re fractions were loaded onto Ba-coated Pt
or Ni filaments and measured with Faraday collectors using
negative thermal ionization mass spectrometry (Creaser et
al. 1991; Völkening et al. 1991) on a Micromass Sector 54
mass spectrometer. Total procedure blanks are on the order
of <5 pg for Re, and <2 pg for Os.
Errors (2σ) include uncertainties in Re and Os isotopic
measurements, Re and Os isotope composition reproducibil-
ity of standards, calibration and gravimetric uncertainties of
187
Re and
187
Os, and uncertainties in the
187
Re decay con-
stant. Uncertainties in weights of sample and tracer solution
do not affect the calculated age and are not considered.
Whole-rock geochemistry of the Çöpler–Kabataş
magmatic complex
The results of whole-rock geochemical analyses are listed in
Table 1.
Major elements
Least-altered and altered intrusive and hypabyssal igneous
rocks from the Çöpler–Kabataşmagmatic complex are plot-
ted on a total alkali versus silica diagram in Fig. 9(after
Middlemost 1994). All least-altered samples from the
Çöpler–Kabataşmagmatic complex display subalkaline
character (medium- to high-K calc-alkaline) and most plot
within the granodiorite field, with silica contents ranging
from 63.7 to 68.1 wt%. Three samples have lower silica
contents (between 56.4 and 58.1 wt% SiO
2
), with one least-
altered sample (CR-03) and one propylitically altered sam-
ple (C-166) plotting within the diorite field, and another
propylitically altered sample (CR-14) lying in the monzonite
field. The slightly elevated alkali contents of the two pro-
pylitically altered samples might be due to sericitization of
feldspars and are not thought to reflect primary magma
compositions. A compositional gap (between 58 and
64 wt% SiO
2
) exists between the fresh diorite porphyry
(CR-03) and the rest of the least-altered igneous lithologies
from the magmatic complex.
Major and minor oxide compositions of the least-altered
magmatic rocks from the Çöpler–Kabataşmagmatic com-
plex define roughly linear trends when plotted against SiO
2
on Harker-type diagrams (Fig. 10), suggesting a similar
parentage for these rocks. Most major oxides display weak
to moderate negative trends with increasing silica content,
consistent with fractional crystallization of minerals such as
pyroxene, amphibole, and plagioclase, which occur as phe-
nocryst phases. Na
2
O, on the other hand, shows a nearly flat
trend, whereas K
2
O abundance increases slightly with
Miner Deposita
increasing silica content until late stages of fractionation
(∼67 wt% SiO
2
).
Trace elements
All samples from the Çöpler–Kabataşmagmatic complex
have similar trace element compositions, as illustrated on a
primitive mantle-normalized trace element diagram
(Fig. 11). The samples are enriched in incompatible ele-
ments, particularly large ion lithophile elements (LILE)
when compared to high field strength elements (HFSE).
Positive peaks for Pb and Sb and negative anomalies for
Nb, Ta, and Ti are typical of magmas related to subduction
(Brenan et al. 1994; Stolz et al. 1996).
Rare earth elements (REE) in Çöpler–Kabataşsamples
show distinctive listric-shaped patterns on a chondrite-
normalized diagram (Fig. 12), with moderate enrichments
in light rare earth elements (LREE) relative to middle
(MREE) and heavy rare earth elements (HREE), and flat
to upward-trending (listric) slopes between MREE and
HREE (Fig. 12). This pattern is commonly ascribed to
hornblende fractionation or residual hornblende in the
source region because hornblende preferentially partitions
MREE (Frey et al. 1978; Hanson 1980). The lack of signif-
icant europium anomalies is indicative of either oxidizing
conditions (Eu
3+
cannot be incorporated into plagioclase)
and/or hydrous conditions (early plagioclase crystallization
being suppressed) during evolution of the Çöpler–Kabataş
magmas (Hanson 1980; Carmichael and Ghiorso 1990;
Moore and Carmichael 1998). The oxidized and hydrous
nature of these magmas is further supported by the abun-
dance of hornblende as a phenocryst phase and the wide-
spread presence of magnetite.
40
Ar/
39
Ar geochronology
A summary of the of
40
Ar/
39
Ar dating results is presented in
Table 2, and apparent age spectra are illustrated in Fig. 13;
full analytical data are listed in the Electronic
Supplementary Material (ESM 2). Plateau ages are defined
using the criteria of Fleck et al. (1977). All samples yielded
moderately to well-defined plateaus and calculated plateau
ages that are within error of the inverse isochron ages.
Igneous biotite from granodiorite porphyry (C-164), ig-
neous hornblende from hornblende diorite porphyry (C-
166), and igneous biotite from quartz diorite (CR-02) from
the Çöpler intrusive complex yielded plateau ages of 43.75±
0.26 Ma (MSWD00.20), 44.13±0.38 Ma (MSWD01.4),
and44.19±0.23Ma(MSWD00.49), respectively
(Figs. 13a–c). These dates overlap within error and are
interpreted to represent cooling ages for these samples.
40
Ar/
39
Ar analysis of hydrothermal alteration minerals
associated with mineralization at Çöpler yielded plateau
ages close to or overlapping the ages of igneous minerals.
Hydrothermal biotite from porphyry-style potassic alteration
Foidolite
Granite
Granodiorite
DioriteGabbro
Foid
Monzodiorite
Foid
Syenite
Quartz
Monzonite
Syenite
Monzonite
Monzodiorite
Foid
Gabbro
Monzogabbro
Foid
Monzosyenite
Alkalic
Subalkalic
Taurides
(Eocene)
Pontides
(Eocene)
Baskil
(Late Cretaceous)
Pontides
(Late Cretaceous)
Horoz
Karamadazı
}
+
Eocene
+
+
+
4
6
8
12
14
10
40 50 60 70 80
Na2O + K2O (wt.%)
SiO2 (wt.%)
+
+
2
Gabbroic
Diorite
Fig. 9 Total-alkali versus silica diagram (after Middlemost 1994) for
least altered and altered intrusive rocks from the Çöpler–Kabataş
magmatic complex (data recalculated 100 % volatile-free) plotted
together with a suite of regional samples obtained from various Late
Cretaceous–Eocene intrusive systems across the central eastern Taur-
ides, and one extrusive rock sample from the Yamadağvolcanic center.
Also plotted are the ranges of compositions from the same localities as
well as felsic to intermediate compositions from the Eocene Pontide
magmatic belt as compiled from previously published data. Data
sources: Eocene Tauride intrusions, Gençalioğlu-Kuşcu et al. (2001),
Önal et al. (2005), Kadıoğlu and Dilek (2010); Divriği, Boztuğet al.
(2007); Yamadağvolcanic center, Kürüm et al. (2008); Baskil intrusive
complex, Rızaoğlu et al. (2009); Pontides, Karslıet al. (2007,2010a,
b). Alkaline–subalkaline boundary from Irvine and Baragar (1971)
Miner Deposita
in sample C-169 yielded a plateau age of 43.84 ±0.26 Ma
(MSWD00.63; Fig. 13d). Sericite from phyllic alteration in
sample C-138 yielded a downward stepping spectrum, sug-
gesting the presence of minor excess
40
Ar in early steps
(Fig. 13e), but the second half of the spectrum includes an
acceptable six-step plateau containing more than 50 % of
total
39
Ar released, with an age of 44.44±0.28 Ma
(MSWD01.05), which should be considered a maximum
age. An alternative estimate in samples containing excess
40
Ar is provided by the inverse isochron age, which in this
case was almost within error of the plateau age at 45.22±
0.74 Ma (MSWD00.23).
Two samples from the Çaltı(CR-11) and Bizmişen (CR-
12) intrusions yielded well-defined plateau ages of 44.16 ±
0.23 Ma (MSWD00.71) and 43.51±0.51 Ma (MSWD 0
0.76), respectively (Fig. 13f, g), which are similar to the
ages from Çöpler. A granite sample (CR-09) from the
Divriği area also yielded a well-constrained plateau age of
74.24±0.41 Ma (MSWD00.18; Fig. 13h), about 30 my
older than the Çöpler magmatic system, and consistent with
the data previously published by Boztuğet al. (2007) and
Kuşcu et al. (2007).
Re–Os geochronology
Model Re–Os ages were calculated for molybdenite samples
C-161 and C-162 from Çöpler, based on the simplified
isotope equation: t0ln(
187
Os/
187
Re+1)/λ,wheretis the
model age, and λis the
187
Re decay constant (1.666×10
–
11
a
–1
; Smoliar et al. 1996). The samples yielded ages of
44.6±0.2 and 43.9± 0.2 Ma, respectively (Table 3), which
are similar to each other, and to the
40
Ar/
39
Ar ages of
igneous (44.2±0.3 Ma) and hydrothermal (44.4–43.8 Ma)
minerals.
Discussion
Interpretation of geochronological data
New geochronological data presented herein constrain the
temporal relationship between magmatic and hydrothermal
events at the Çöpler–Kabataşmagmatic complex. With the
exception of two samples, combined
40
Ar/
39
Ar and Re–Os
ages of igneous and hydrothermal minerals from Çöpler are
analytically indistinguishable from each other suggesting
rapid cooling conditions within a period of ≤1my
(Fig. 14). This is consistent with the simple intrusive history
and the relatively shallow level of emplacement directly
beneath the Munzur limestone, which has a maximum thick-
ness of 1,200 m (Özgül and Turşucu 1984;Tunçetal.
1991).
The plateau age of sericite sample obtained from phyllic-
altered granodiorite porphyry (44.44±0.28 Ma) and the Re–
Os age of one molybdenite-bearing quartz–sulfide vein
(44.6±0.2 Ma) are notably older than the
40
Ar/
39
Ar plateau
age of igneous biotite (43.75±0.26 Ma) obtained from the
host granodiorite porphyry (Fig. 14). This discrepancy be-
tween the igneous and hydrothermal dates likely suggests
thermal resetting of the igneous biotite and hornblende
during high temperature potassic alteration, and therefore,
at least the younger
40
Ar/
39
Ar dates probably represent
cooling ages rather than the crystallization age of the
Çöpler intrusion. If this is the case, then the older molybde-
nite age can be explained by the high closure temperature of
molybdenite (>700 °C; Bingen and Stein 2003) compared to
the Ar diffusion blocking temperature of biotite (250–400 °
55 60 65 70
0
5
10
15
20
25
Oxide (wt. %)
Al2O3
Fe2O3
MgO
CaO
Na2O
K2O
MnO
TiO2
P2O5
0
5
6
8
10
13
55 60 65 70
3
4
7
9
11
12
1
2
Oxide (wt. %)
0
0.1
0.3
0.5
0.7
0.9
55 60 65 70
0.2
0.4
0.6
0.8
Oxide (wt. %)
SiO2 (wt. %)
SiO2 (wt. %)
SiO2 (wt. %)
b
a
c
Fig. 10 Harker diagrams showing variation of major and minor oxide
abundances relative to SiO
2
for least altered intrusive rocks from the
Çöpler–Kabataşmagmatic complex
Miner Deposita
C; Richards and Noble 1998) and hornblende (∼500 °C).
However, based on the close agreement between these cool-
ing ages and the plateau age of igneous biotite (44.19±
0.23 Ma) from unaltered quartz diorite immediately to the
east of Çöpler, it can be inferred that the hydrothermal event
resetting the Ar isotopic system of igneous biotite and
hornblende from Çöpler is only slightly younger than
the age of pluton emplacement at the Çöpler–Kabataş
magmatic complex. This interpretation is further sup-
ported by the
40
Ar/
39
Ar dates of igneous biotite and
hornblende from the unaltered Çaltıand Bizmişen plutons,
which yielded plateau ages of 44.16±0.23 and 43.51±
0.51 Ma, respectively.
Molybdenite samples from two quartz–magnetite–sulfide
veins from the Çöpler Main Zone yielded Re–Os ages of
44.6±0.2 and 43.9 ± 0.2 Ma, which do not overlap within
error. These different ages may represent discrete pulses of
molybdenite mineralization, although there is no field or
petrographic evidence to confirm this hypothesis.
The timing of the paragenetically later epithermal-style
mineralization, on the other hand, could not be determined
due to its poor preservation. Minerals such as adularia or
sericite, which may have originally been present, have been
destroyed by intense weathering and oxidization of the
shallow epithermal levels of the system. However, there is
no evidence to suggest that this stage of mineralization was
++
++++
++
+
++
+
++
+
+
+++
+
+
+
+++++++
++
+
++
+
+
+
++
+
+
+
+
++
++
+++
+
+
+
++
+
++++++
Element
Primitive mantle normalized
Cs
Rb
Tl
Ba
Th
Nb
U
Ta
K
Ce
La
Pb
Pr
P
Sr
Nd
Zr
Sm
Hf
Eu
Sb
Gd
Ti
Tb
Dy
Ho
Y
Er
Tm
Lu
Yb
1
10
100
1000
CR-01
CR-02
CR-03
C-014
C-169
C-173
C-104
+
+
Altered
Fig. 11 Primitive mantle-
normalized trace element dia-
gram for least altered igneous
rocks from the Çöpler–Kabataş
magmatic complex. Gray area
represents altered samples from
the region, and the close over-
lap between least altered and
altered samples indicates that
hydrothermal alteration has had
minimal effect on most trace
element compositions in this
suite. Normalization values
from Sun and McDonough
(1989)
+
+
+++
+
+
+++++++
+
+
+
+
+
+
+
+
+
+
+
+
+
+
La Ce Pr Nd Sm Gd Dy ErEu Tb Ho Tm Yb Lu
1
10
100
1000
Element
C1 Chondrite Normalized
CR-01
CR-02
CR-03
C-014
C-169
C-173
C-104
+
+
Altered
Fig. 12 Chondrite-normalized
REE diagram for least altered
igneous rocks from the Çöpler–
Kabataşmagmatic complex.
Gray area represents altered
samples from the region,
showing that alteration has not
affected rare earth element
compositions in these rocks.
Normalization values from Sun
and McDonough (1989)
Miner Deposita
substantially later than the higher-temperature porphyry-
style mineralization.
Petrogenesis of middle Eocene granitoids in the central
eastern Taurides
The timing of cooling of the magmatic-hydrothermal system
at Çöpler and the inferred crystallization age of the Çöpler–
Kabataşmagmatic complex (∼44 Ma) overlaps with the
emplacement ages of the nearby Çaltı(44.16±0.23 Ma)
and Bizmişen intrusions (43.51±0.51 Ma) and is slightly
younger than the cooling ages of the Horoz, Karamadazı,
and Doğanşehir plutons (50–48 Ma; Kuşcu et al. 2007;
Karaoğlan et al. 2009) located farther to the southwest.
Together, these intrusive centers define a middle Eocene
calc-alkaline suite in the central and eastern Taurides, with
broadly similar trace element compositions (including
enrichments in LREE, negative anomalies of HFSE such
as Nb, Ta, Zr, and Ti, and listric-shaped REE patterns;
Figs. 15a and 16a). One sample of evolved granite (CR-
28) from Horoz shows stronger depletions in Ba, Sr, P, Eu,
and Ti, likely due to extensive fractionation of plagioclase,
apatite, and Ti-bearing phases (Figs 15a and 16a). In gener-
al, however, the geochemical signatures of the middle
Eocene granitoids of the central eastern Taurides are consis-
tent with typical arc-related magmatic rocks formed by
partial melting of metasomatized mantle wedge above a
subducting slab (Brenan et al. 1994; Stolz et al. 1996;
Kogiso et al. 1997).
The central eastern Tauride granitoids are currently locat-
ed approximately 140 km north of the Bitlis Suture, and
about 120 km north of the Maden and Helete volcanic belt
(Fig. 1), but these distances may have been larger prior to
Miocene collision. Thus, these granitoids may have formed
in a back-arc environment behind the main Maden and
Helete arc and Bitlis subduction zone.
Late Cretaceous–Eocene magmatism along the southeastern
TAB margin (Taurides)
The Late Cretaceous (88–70 Ma) Baskil intrusive complex
and several granitoid bodies exposed around Göksun–Afşin
area represent the earliest stage of arc magmatism along the
southern TAB margin. Geochemical data compiled for a
range of mafic to felsic subalkaline lithologies (Fig. 9)
Table 2 Summary of
40
Ar/
39
Ar dating results from the Çöpler–Kabataşmagmatic complex and Bizmişen, Çaltı, and Divriği intrusions
Sample number Lithology Mineral Integrated
age± 2σ(Ma)
Plateau
age± 2σ(Ma)
MSWD Number of
steps in plateau/
total steps
%
39
Ar
released
(plateau)
Inverse isochron
age± 2σ(Ma)
MSWD Initial
40
Ar/
36
Ar
a
Igneous minerals: Çöpler–Kabataşmagmatic complex
C-164 Granodiorite porphyry Biotite 43.29 ±0.21 43.75 ± 0.26 0.20 6/9 94 43.70± 0.28 0.19 289 ±24
C-166 Hornblende diorite porphyry Hornblende 44.43± 0.42 44.13±0.38 1.4 8/11 100 43.74± 0.49 0.69 307 ±12
CR-02 Quartz diorite Biotite 43.97± 0.11 44.19 ±0.23 0.49 11/18 89.5 44.17 ± 0.26 0.65 294±23
Hydrothermal minerals: Çöpler
C-169 Potassically altered porphyry Biotite 43.22 ±0.24 43.84± 0.26 0.63 11/17 90.5 43.86 ± 0.30 0.49 292.9 ±5.1
C-138 Sericitized porphyry Sericite 44.91 ± 0.16 44.44±0.28 1.05 6/13 53 45.22± 0.74 0.23 148 ±130
Igneous minerals: Çaltıand Bizmişen intrusions
CR-11 Tonalite Biotite 44.11± 0.11 44.16 ± 0.23 0.71 9/16 77.9 43.68 ± 0.26 1.4 476± 36
CR-12 Diorite Hornblende 42.36± 1.11 43.51 ±0.51 0.76 11/14 98.6 43.40±0.64 0.82 293±2.7
Igneous minerals: Divriği intrusion
CR-09 Alkali feldspar granite Biotite 72.89 ± 0.22 74.24± 0.41 0.18 7/11 81.3 74.24 ±0.56 0.21 288±45
a
Expected
40
Ar/
36
Ar composition of atmospheric argon0295.5
Fig. 13 Apparent
40
Ar/
39
Ar age spectra for igneous biotite and horn-
blende from the Çöpler–Kabataşmagmatic complex (a–c), hydrother-
mal biotite and sericite from the Çöpler porphyry deposit (d,e), and
igneous biotite from nearby central eastern Tauride intrusive centers (f–
h). See Table A1for sample locations and descriptions. Locations of
the samples from the Çöpler deposit are also shown in Fig. 5. Results
are summarized in Table 2, and full data are listed in Electronic
Supplementary Material (ESM 2)
b
Miner Deposita
0
20
40
60
0 20 40 60 80 100
Plateau age = 43.84±0.26 Ma
(2σ, including J-error of .5%)
MSWD = 0.63, probability=0.79
Includes 90.5% of the 39Ar
Cumulative
39
Ar Percent
Age (Ma)
20
30
40
50
020406080100
Plateau age = 43.75±0.26 Ma
(2σ, including J-error of .5%)
MSWD = 0.20, probability=0.96
Includes 94% of the 39Ar
Cumulative
39
Ar Percent
Age (Ma)
0
20
40
60
80
020406080100
Plateau age = 44.13±0.38 Ma
(2
σ
, including J-error of .5%)
MSWD = 1.4, probability=0.19
Includes 100% of the
39
Ar
Cumulative
39
Ar Percent
Age (Ma)
35
40
45
50
020406080100
Plateau age = 44.19±0.23 Ma
(2σ, including J-error of .5%)
MSWD = 0.49, probability=0.90
Includes 89.5% of the 39Ar
Cumulative
39
Ar Percent
Age (Ma)
ab
cd
Cumulative
39
Ar Percent
Age (Ma)
20
30
40
50
60
020406080100
Plateau age = 44.44±0.28 Ma
(2
σ
, including J-error of .5%)
MSWD = 1.05, probability=0.39
Includes 53% of the
39
Ar
e
Cumulative
39
Ar Percent
Age (Ma)
50
60
70
80
90
020406080100
Plateau age = 74.24±0.41 Ma
(2
σ
, including J-error of .5%)
MSWD = 0.18, probability=0.98
Includes 81.3% of the
39
Ar
h
Cumulative
39
Ar Percent
Age (Ma)
30
35
40
45
50
0 20 40 60 80 100
Plateau age = 44.16±0.23 Ma
(2
σ
, including J-error of .5%)
MSWD = 0.71, probability=0.69
Includes 77.9% of the
39
Ar
f
Cumulative
39
Ar Percent
Age (Ma)
0
20
40
60
80
020406080100
Plateau age = 43.51±0.51 Ma
(2
σ
, including J-error of .5%)
MSWD = 0.76, probability=0.67
Includes 98.6% of the
39
Ar
g
Miner Deposita
indicate relatively unenriched compositions compared to the
Çöpler–Kabataşsuite (Fig. 15b and 16b), consistent with a
continental arc origin for these granitoids (Yazgan and
Chessex 1991; Parlak 2006;Rızaoğlu et al. 2009).
After a period of quiescence in the Paleocene, magma-
tism along the southern TAB margin resumed in the middle
Eocene with eruption of the Maden and Helete volcanic
rocks (Fig. 1). These basaltic to rhyolitic rocks have sub-
alkaline to mildly alkaline character, with enrichments in
LILE relative to HFSE, and negative Nb and Zr anomalies
(Aktaşand Robertson 1984;Yiğitbaşand Yılmaz 1996a;
Elmas and Yılmaz 2003; Robertson et al. 2007). The Helete
and Maden suites appear to represent the locus of middle
Eocene volcanism above the southern Neotethys subduction
zone (Yiğitbaşand Yılmaz 1996a; Robertson et al. 2007).
In comparison, as noted above, the broadly coeval Çöpler–
Kabataşmagmatic complex, located 120 km further north,
likely represents a back arc magmatic system. A similar
tectonomagmatic setting may also be invoked for Eocene
magmatism along the transtensional Göksu–Yazyurdu and
Malatya–Ovacık fault zones. Paleocene–Eocene slab roll-
back beneath southeast Anatolia (Robertson et al. 2007;
Kaymakçıet al. 2010) may have caused extension in the
overriding plate, and subsequent initiation of these back-arc
systems, and may also be responsible for the anomalous
curvatures of the Bitlis sector of the southern Neotethyan
subduction zone and the adjacent Cypriot arc to the southwest
(Fig. 2c; Schellart and Lister 2004; Wallace et al. 2009).
Similar middle Eocene back-arc magmatism occurred behind
the main axis of the Urumieh–Dokhtar arc in Iran (the eastern
continuation of the Maden–Helete arc), producing large vol-
umes of calc-alkaline volcanic and plutonic rocks with sub-
duction signatures (LILE-enriched, HFSE-depleted, and
LREE-enriched trace element patterns; Ahmadian et al.
2009;Allen2009; Verdel et al. 2011; Vincent et al. 2005).
On the other hand, Kuşcu et al. (2010) argued that the
middle Eocene volcanism at Maden and Helete, and the
Eocene central eastern Tauride granitoids were generated in
a postcollisional setting, following the termination of Late
Cretaceous subduction magmatism in southeast Anatolia.
According to this model, incipient rupturing of the steepened
slab led to invasion of hot asthenospheric material beneath the
southern TAB margin, which caused the delayed partial melt-
ing of subduction-modified mantle sources and subsequent
subalkaline to mildly alkaline magmatism in the eastern TAB.
However, a problem with this model is that it infers a pre-
Eocene timing for the Eurasia–Arabia collision, which is not
supported by recent tectonic reconstructions that suggest
Miocene collision (e.g., Dewey et al. 1986; McQuarrie et al.
2003;Hüsingetal.2009;Okayetal.2010).
Middle Miocene postcollisional magmatism in the TAB
Postcollisional magmatism along the southern TAB margin
began during the middle Miocene with eruption of large
volumes of subalkaline to mildly alkaline mafic to felsic
Table 3 Summary of Re–Os molybdenite data from the Çöpler deposit
Sample
number
Sample location Drill hole: depth Re
(ppm)
187
Re
(ppm)
187
Os
(ppb)
Model
age (Ma)
Age uncertainty
(±2σ) with
decay constant
uncertainty (Ma)
C-161 0458723E 4363842N –7,031 4,419 3,284 44.6 0.2
C-162 0458802E 4363880N CDD-140: 180.0–180.1 m 2,242 1,409 1,031 43.9 0.2
45.0 44.5 43.544.0 43.0
A
g
e (Ma)
43.75 ± 0.26
44.13 ± 0.38
44.19 ± 0.23
43.84 ± 0.26
44.44 ± 0.28
44.6 ± 0.20
43.9 ± 0.20
Granodiorite porphyry (C-164: igneous biotite)
Hornblende diorite porphyry (C-166: hornblende)
Quartz diorite (CR-2: igneous biotite)
Potassic alteration (C-169: hydrothermal biotite)
Phyllic alteration (C-138: sericite)
Molybdenite vein (C-161)
Molybdenite vein (C-162)
40
Ar/
39
Ar
Re-Os
Fig. 14 Summary of
40
Ar/
39
Ar
and Re–Os geochronology
results for the Çöpler–Kabataş
magmatic complex and the
Çöpler gold deposit.
40
Ar/
39
Ar
dates are plateau ages and
Re–Os dates are model ages.
Error bars are reported at 2σ
Miner Deposita
volcanic rocks, including the Yamadağvolcanic center.
Overall, the trace element and REE profiles of the erupted
magmas are broadly similar to those of middle Eocene
central eastern Tauride intrusions (Figs. 15c and 16c), sug-
gesting derivation from a remnant subduction-modified
mantle source beneath the TAB. Partial melting was possi-
bly triggered by slab break-off following early Miocene
collision (Keskin 2003;Şengör et al. 2003; Faccenna et al.
2006) or by delamination of the subcontinental lithospheric
mantle beneath eastern Anatolia (Pearce et al. 1990;Göğüş
and Pysklywec 2008).
Comparison with Eocene magmatism along the northern
TAB margin (Pontides)
Middle Eocene (52–41 Ma) plutonic and volcanic sequences
also occur along the northern TAB margin in the eastern
Pontides and are interpreted to represent postcollisional
magmatism following closure of the İzmir–Ankara–
Erzincan Ocean (Okay and Şahintürk 1997). These rocks
are geochemically quite similar to the Çöpler–Kabataşmag-
matic rocks (Figs. 9,15d, and 16d) but, in this case, are
indisputably postcollisional. This illustrates the problem of
using lithogeochemistry alone as an indicator of tectonic
setting because geochemically similar magmas can be gen-
erated in back-arc and postsubduction settings.
Metallogenic Implications
The calc-alkaline Çöpler–Kabataşmagmatic complex is ar-
gued above to have formed in a back-arc setting during the
final stages of regional transtension prior to collision, and its
location was controlled by a major ENE-trending sinistral
fault system.
Element
Primitive mantle normalized
Rb
Ba
Th
Nb
U
Ta
K
Ce
La
Pb
Pr
P
Sr
Nd
Zr
Sm
Hf
Eu
Gd
Ti
Tb
Dy
Ho
Y
Er
Tm
Lu
Yb
CR-10
0.1
10
100
1000
1
c
a
Primitive mantle normalized
Element
0.1
1
10
100
+
+
++
+++
1000
Rb
Ba
Th
Nb
U
Ta
K
Ce
La
Pb
Pr
P
Sr
Nd
Zr
Sm
Hf
Eu
Gd
Ti
Tb
Dy
Ho
Y
Er
Tm
Lu
Yb
CR-11
CR-12
CR-24
CR-28
CR-31 +
Eocene Central-Eastern Tauride intrusive rocks and
+
+
+++
+
+
+
+
++++
++
+
++
+++
Element
0.1
1
10
100
1000
Rb
Ba
Th
Nb
U
Ta
K
Ce
La
Pb
Pr
P
Sr
Nd
Zr
Sm
Hf
Eu
Gd
Ti
Tb
Dy
Ho
Y
Er
Tm
Lu
Yb
bLate Cretaceous Baskil Intrusive Complex (dark gray)
Element
Rb
Ba
Th
Nb
U
Ta
K
Ce
La
Pb
Pr
P
Sr
Nd
Zr
Sm
Hf
Eu
Gd
Ti
Tb
Dy
Ho
Y
Er
Tm
Lu
Yb
dEocene Eastern Pontide magmatic rocks (dark gray)
Yamada Volcanic Center (dark gray) and
Magmatic Complex (light gray)
Magmatic Complex (light gray) and öpler-Kabata Magmatic Complex (light gray)
Magmatic Complex (light gray)
Primitive mantle normalized
0.1
10
100
1000
1
Primitive mantle normalized
and öpler-Kabata
öpler-Kabata
öpler-Kabata
Fig. 15 Primitive mantle-normalized trace element diagrams, showing
compositions of aEocene central eastern Tauride plutonic rocks, bthe
Late Cretaceous Baskil intrusive complex, cthe Miocene Yamadağ
volcanic center, and dthe middle Eocene eastern Pontide plutonic and
volcanic rocks, compared with the range of compositions of igneous
rocks from the Çöpler–Kabataşmagmatic complex (light grey field).
Data sources: Baskil intrusive complex: Rızaoğlu et al. (2009); Yamadağ
volcanic center: Kürüm et al. (2008). Normalization values from Sun and
McDonough (1989)
Miner Deposita
Unlike many porphyry systems that occur as clusters
within orogen-parallel volcano-plutonic belts in convergent
margin settings, the Çöpler Au–(Cu) deposit is positioned
inland from the coeval Maden–Helete arc system. In this
respect, Çöpler may have formed in a manner comparable to
some other isolated Au-rich porphyry deposits such as the
Bajo de la Alumbrera porphyry Cu–Au deposit in northwest
Argentina and Bingham Canyon porphyry Cu–Au–Mo de-
posit in western USA.
The Miocene Farallòn Negro Complex and associated
Bajo de la Alumbrera porphyry Cu–Au deposit in
Argentina lies about 200 km inland from the main axis of
the Andean volcanic arc and is thought to have formed
during a period of flattening of subduction, with magmatism
being localized by extensional structural intersections in the
upper plate (Sasso and Clark 1998; Chernicoff et al. 2002;
Halter et al. 2004).
Similarly, the Bingham porphyry Cu–Au–Mo deposit is
located far inland with respect to the coeval subduction zone
and is proposed to have formed during a period of incipient
extension related to steepening/roll-back of the Farallon
Plate during the Paleocene (Ryskamp et al. 2008; Sillitoe
2008; Pettke et al. 2010). Pettke et al. (2010) further sug-
gested that the parental magma at Bingham and its ore
components were derived from a Proterozoic subduction-
modified lithospheric mantle source, which was remelted
during the Eocene tectonic activity.
In comparison, collision-related deposits such as
Grasberg (Indonesia) and Ok Tedi (Papua New Guinea)
are thought to have formed by remelting of subduction-
modified lithospheric sources following delamination of
the subcontinental lithospheric mantle (McDowell et al.
1996; Cloos et al. 2005; van Dongen et al. 2010). The
similarity of magma compositions and deposit styles
+
+
+
+
+
+++++++++
La Ce Pr Nd Sm Gd Dy ErEu Tb Ho Tm Yb Lu
1
10
100
1000
Element
C1 Chondrite Normalized
a Eocene Central-Eastern Tauride intrusive rocks and
1000
b
La Ce Pr Nd Sm Gd Dy ErEu Tb Ho Tm Yb Lu
1
10
100
Element
C1 Chondrite Normalized
Element
d
La Ce Pr Nd Sm Gd Dy ErEu Tb Ho Tm Yb Lu
1
10
100
1000
C1 Chondrite Normalized
Late Cretaceous Baskil Intrusive Complex (dark gray)
Eocene Eastern Pontide magmatic rocks (dark gray)
La Ce Pr Nd Sm Gd Dy ErEu Tb Ho Tm Yb Lu
1
10
100
1000
Element
C1 Chondrite Normalized
c
CR-10
CR-11
CR-12
CR-24
CR-28
CR-31 +
Yamada Volcanic Center (dark gray) and
Magmatic Complex (light gray) Magmatic Complex (light gray)
Magmatic Complex (light gray)
öpler-Kabata and öpler-Kabata
and öpler-Kabata
öpler-Kabata Magmatic Complex (light gray)
Fig. 16 Chondrite-normalized rare earth element diagrams, showing
compositions of aEocene central eastern Tauride plutonic rocks, bthe
Late Cretaceous Baskil intrusive complex, cthe Miocene Yamadağ
volcanic center, dthe middle Eocene eastern Pontide plutonic and
volcanic rocks, compared with the range of compositions of igneous
rocks from the Çöpler–Kabataşmagmatic complex (light gray field).
Data sources: Baskil intrusive complex, Rızaoğlu et al. (2009); Yamadağ
volcanic center (light gray field), Kürüm et al. (2008). Normalization
values from Sun and McDonough (1989)
Miner Deposita
between these collision-related and back-arc deposits such
as Çöpler suggests that there may be a continuum in terms
of tectonomagmatic and metallogenic processes in these
broadly subduction-related settings (Richards 2009,2011).
Conclusions
The Çöpler porphyry-epithermal Au–(Cu) deposit is spatially
related to middle Eocene calc-alkaline diorite and granodiorite
porphyry stocks, which are interpreted to have formed in a
back-arc setting behind the southern Neotethys subduction
zone, shortly prior to continent–continent collision in the
Miocene. Emplacement of these and other middle Eocene
intrusions in the central eastern Taurides was controlled by
regionally extensive, ENE-striking, strike-slip fault systems.
40
Ar/
39
Ar ages of igneous minerals from intrusive rocks
in the Çöpler–Kabataşmagmatic complex range between
44.13± 0.38 and 43.75±0.26 Ma, whereas hydrothermal biotite
and sericite associated with porphyry-style hydrothermal alter-
ation at Çöpler yielded
40
Ar/
39
Ar ages of 43.84± 0.26 Ma and
44.44± 0.2, respectively. The ∼0.7 my range in these ages likely
reflects differential cooling in different parts of the magmatic-
hydrothermal system and the different closure temperatures to
argon diffusion of biotite and sericite. Nevertheless, these cool-
ing ages closely overlap with the age of porphyry-type miner-
alization obtained from two molybdenite samples (44.6±0.2
and 43.9±0.2 Ma), indicating a short life span for the
magmatic-hydrothermal system of ≤1my,whichisconsistent
with the relatively simple history and shallow emplacement of
the intrusive system and ore deposit.
These ages are also similar to the
40
Ar/
39
Ar plateau ages
of igneous biotite from an unaltered quartz diorite to the east
of Çöpler (44.19±0.26 Ma) and igneous biotite and horn-
blende from the unaltered Çaltı(44.16±0.23 Ma) and
Bizmişen (43.51±0.51 Ma) intrusions, indicating that the
hydrothermal system at Çöpler developed concurrently with
the ∼44 Ma back-arc magmatic activity that took place in
the eastern Taurides.
The back-arc setting of the Çöpler Au–(Cu) deposit can
be compared to other similar porphyry Cu–Au deposits in
back-arc or collisional settings, such as Bingham Canyon
(USA), Bajo de la Alumbrera (Argentina), and possibly Ok
Tedi (Papua New Guinea) and Grasberg (Indonesia).
Acknowledgments This work was funded by a Discovery Grant
from the Natural Sciences and Engineering Research Council of Can-
ada (NSERC) to JPR. Partial financial support was provided by the
Society of Economic Geologists through a Student Research Grant to
Aİ. Logistical support for fieldwork was provided by Anatolia Miner-
als Development Ltd. (AMDL), and special thanks are due to Firuz
Alizade and İlhan Poyraz of the Ankara office for access to the mine
site. Ali Ekber Özden, Aşkın Sarpay, and İbrahim Güney of AMDL are
thanked for their assistance during fieldwork in 2006, and Orhan
Karaman is thanked for his help during collection of regional samples
in 2008. We thank Tom Ullrich of the Pacific Centre for Isotopic and
Geochemical Research (PCIGR) Noble Gas Laboratory at the Univer-
sity of British Columbia for providing
40
Ar/
39
Ar isotopic data. We also
thank Sergei Matveev, Mark Labbe, Don Resultay, and everyone at the
Radiogenic Isotope Facility at the University of Alberta for their help
in sample preparation, and data collection. We thank Thomas Bissig,
Kalin Kouzmanov, and Aleksandar Miskovich for their constructive
reviews, which helped improve the manuscript.
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