background image


The Savcôlô Thrust Fault (Kôrþehir, Central Anatolia):

a backthrust fault, a suture zone or a secondary fracture in

an extensional regime?


Hacettepe University, Department of Geological Engineering, 06532 Beytepe, Ankara, Turkey;

(Manuscript received November 30, 2004; accepted in revised form June 16, 2005)

Abstract:  Large exposures of granitic and metamorphic rocks characterize the geology of Central Anatolia, in Turkey.
These basement rocks crop out mainly between the Tuz Gölü and Ecemi  fault zones, two major fractures of strike-slip fault
character. During the Neogene, detachment faulting along the Tuz Gölü Fault (TGF) zone caused the deposition of several
thousand meters of sediments in the large intracontinental Tuz Gölü Basin. In the western parts of Central Anatolia and near
Kôr ehir town, another fracture zone runs almost parallel to the SE-trending TGF zone, separated from the TGF by a narrow

~ 30 km) and rectangular granitic belt. Along this fracture known as the Savcôlô Thrust Fault (STF), metamorphic and

plutonic rocks overthrust middle Eocene detrital rocks of the sedimentary cover along a relatively narrow (

~ 100 m)

crushing zone. In some previous works, this structure is presented as a backthrust of the Anatolian block, or a suture zone
along which two continental Central Anatolian blocks were amalgamated. Recent detailed mineral exploration studies reveal
that the area at the north of the STF comprises several low-angle normal faults along the surfaces of which the Eocene and
the underlying metamorphic rocks moved southwards until they were juxtaposed to southern granitic rocks along steeply
or moderately dipping contacts. The fault surfaces are several km long, slips of a few kilometers are clear and ductile
deformation is observed in the Eocene clastic rocks. Immediately to the north of the STF, Eocene rocks are asymmetrically
folded with a southern vergence, a displacement sense not compatible with the northerly movement observed at the STF
zone and suggesting a causal relationship between thrusting and normal faulting. A possible explanation of this extension
may be the southwards tilting of the foreland due to the northwards overthrusting and the following gravitational move-
ments. The folding style in the foreland and the very narrow width of the thrust zone, however, preclude such a crustal
loading to induce extension in the foreland. In the Savcili area where the thrust fault is observed, we do not see any evidence
to account for crustal shortening, as it should be observed in the vicinity of a major compressional structure as previously
advanced. How this thrust formed in an extensional regime and how this post-middle Eocene crustal extension is associated
with the southern Neogene Tuz Gölü Fault zone remain to be explored.

Key words: Turkey, Central Anatolia, Kôr ehir metamorphites, Savcôlô Thrust Fault, Tuz Gölü Fault, normal faulting.


The structural features of the Anatolian block are the re-
sults of geodynamic processes that opened and closed the
Tethys Ocean in the Eastern Mediterranean. Ketin (1966)
reviewed the previous proposals of the orogenic divisions
of this part of the Tethysides.  engör & Yôlmaz (1981) and

engör and co-workers ( engör et al. 1985) explained var-

ious points of the Anatolian geology. After several de-
cades of geological research that resulted in a large
number of papers (regional scale: (Ketin 1966; Brinkmann
1976; Görür et al. 1998); local scale: (Ketin 1955; Ataman
1972; Erkan 1976; Erkan & Ataman 1981; Oktay 1981;
Seymen 1981, 1982, 1984, 2000; Göncüoûlu et al. 1991;
Aydôn & Önen 1999; Whitney & Dilek 1998; Boztuû
2000; Dirik 2001; Whitney et al. 2001; Gautier et al.
2002; Güleç et al. 2002; Piper et al. 2002; Ku çu et al.
2002; Genç 2003)), the internal parts of the Anatolian
block known as Central Anatolia (Fig. 1) still remain the
structurally most poorly understood sector of Anatolian
block. Large outcrops of metamorphic and granitic rocks
characterize the geology of Central Anatolia, in particular

near Kôr ehir city (Fig. 2). The non-metamorphic cover be-
gins with the Upper Cretaceous rocks near Kôr ehir (Ketin
1955), overlain by Tertiary sediments comprising middle
Eocene sedimentary clastic rocks and carbonates, and
Neogene detrital rocks (Oktay 1981; Seymen 1982). To
the west of Kôr ehir and near Savcôlô town, the metamor-
phites tectonically overlie the Eocene rocks along a frac-
ture zone (Oktay 1981), namely the Savcôlô Thrust Fault
(STF). According to Seymen (1982, 2000), the STF is one
of the major fractures of Central Anatolia and extends for
about 150 km in a SE—NW direction. Noting that the com-
pression in Anatolia is absorbed by south-verging thrust
faults,  engör & Yôlmaz (1981) interpreted the STF as a
back-thrust fault of the Anatolian interior. For Görür et al.
(1998), two crustal blocks of Central Anatolia were su-
tured along this structure.

Recent detailed mapping and field observations under-

taken for mineral exploration studies (Genç 2004; Genç &
Yürür 2004) near this structure indicate, however, a struc-
tural setting of extensional character that is highly incom-
patible with the compressional tectonic interpretations
advanced by previous workers for the area considered. In

background image



Fig. 1. A – Place of the study area in a generalized tectonic map of Turkey:  AR – Aegean Region, CA – Central Anatolia, EF – Ece-
mi  Fault, TGF – Tuz Gölü Fault. The trace of the Savcôlô Thrust Fault is drawn from Dirik & Göncüoûlu (1996). B – Map showing the
study area, the Ecemi  and Tuz Gölü faults and the Savcôlô Thrust Fault.

this paper, we present our observations on the Savcôlô
Thrust Fault and field evidence of the extensional tectonics
that are observed near this structure. We use digital eleva-
tion models to present the topographic and morphological
features of this area, and geological map and cross-sections

of some key areas, the study of which effectively explains
the structural characteristics of the area near Savcôlô city
where this fracture zone is best observed. We then discuss
on the spatial relationships between the contractional
Savcôlô structure and the surrounding extensional tectonic

Fig. 2. Geological map of the region surrounding the study area (from the 1:500,000 scale geology map of Turkey, Ankara sheet,
MTA, 2002). Ka – Kaman, KI – Kôr ehir, Sa – Savcôlô.

background image



domain to check if both regimes could be parts of the same
tectonic phase. We think that deciphering this structural
contrast is of great importance to better understand the geo-
logical past of this part of the Anatolian Tethysides for
which the previous tectonic models are not satisfactorily
supported by field observations.

Geological setting

The Fig. 2 illustrates the geology of the area on a re-

gional scale. Near Kôr ehir, low- to high-grade metamor-
phites comprise gneissic rocks, migmatites and various
metamorphic rocks (such as mica-schists, calc-schists, mar-
bles, quartzites, etc). The depositional age of these meta-
morphites is Paleozoic (Genç 2003) whereas controversial
ages are proposed for their metamorphism. According to
Pollak (1958) and Brinkmann (1971, 1976), metamorphic
rocks are the products of a polyphased deformational his-
tory. Some workers, however, do not find any trace of pre-
Alpine movements in Central Anatolia (Ketin 1966; Erkan
1976; Seymen 1984; Whitney et al. 2001). New petrogen-
ic and radiometric data obtained from metamorphic and
plutonic rocks of Central Anatolia indicate a single-phase,
Late Cretaceous regional metamorphism related to crustal
thickening, and a later high-temperature overprint associ-

ated with magmatism, uplift and exhumation (Erkan &
Ataman 1981; Seymen 1982; Whitney & Dilek 1998;
Whitney et al. 2001). Granitic rock exposures are distrib-
uted over a large area in Central Anatolia but the largest
outcrop is located to the NE of the Tuz Gölü Fault (see
Fig. 2). In the area investigated, granites intrude the meta-
morphites as shown by the baking of these latter in con-
tact with the plutonic rocks. In the study area, the earliest
units of the sedimentary cover are nummulitic middle
Eocene clastic rocks with pebbles derived from the meta-
morphic and granitic rocks, overlain by Eocene lime-
stones. Generally poorly cemented detrital rocks of
Neogene age cover the oldest units. Metamorphic folia-
tions generally trend NW—SE, and the Eocene beds usual-
ly have gentle dips towards the south. Foliation and
bedding surfaces locally become almost vertical near the
Savcôlô Thrust Fault where the Eocene rocks are folded
and also in places where tilting occurred due to detach-
ment faulting. The Neogene strata remain subhorizontal
almost in the whole area.


As seen in the digital elevation model (DEM) (Fig. 3),

the study area is located in a region characterized general-

Fig. 3. A – Digital elevation model (DEM) of the region showing the topography of Central Anatolia, prepared using 1:250,000 topo-
graphic maps. Artificial lighting from West with a 45

° zenith angle. The rectangle denotes the location of Fig. 4. Vertical exaggeration

is 2. EF – Ecemi  Fault, KA – Kayseri, KI – Kôr ehir, NE – Nev ehir. B – Block diagram of the DEM with the same lighting and
vertical exaggeration parameters.

background image



ly by a low, gentle rolling topography, with well-pro-
nounced, subparallel alignments of moderate heights
trending more or less parallel to the direction of the two
major fracture zones, the Tuz Gölü and Ecemi  Faults.
Near Kayseri, the well-marked relief is due to the Quater-
nary Erciyes stratovolcano that developed along the Ece-
mi  Fault. Although covered in several places by Neogene
deposits, these alignments of older rocks, in particular the
metamorphic and plutonic rocks of Central Anatolia, ap-
pear to create a large curvilinear structure with a south-
ward convexity.

In our study region, this low-relief landscape comprises

several large Quaternary depositional areas (such Tuz Gölü
Basin, Seyfe Basin). These areas represent basins bounded
by strike-slip faults ( engör 1980;  engör et al. 1985).

Fig. 4 is a high-resolution DEM of the region around the

study area, prepared on the basis of 1:25,000 scale topo-
graphic maps. The DEM is displayed with a vertical exag-
geration of 2 and artificial lighting from the west, the best
direction to emphasize the structural morphology due to
shadowing. The DEM shows a generally mild topography
disturbed by the NW-SE alignment of numerous hills, like
the Aliöflez Mount. To the NE of this alignment, a terrain
much subdued in grey tones corresponds to relatively low
relief topography. This topographic texture is again ex-

Fig. 4. Digital elevation model (DEM) of the region in the vicinity of the Savcôlô Thrust Fault, shown by white line (STF), and the
Savcôlô Detachment Fault (SDF) drawn by black line. (DEM is prepared based on the digitization of 1:25,000 scale topographic maps.)
Vertical exaggeration is 2 and the artificial illumination is from West with a 45

° zenith angle. Rectangles and numbers in them represent

the locations of Figs. 5, 6, 9 and 10.

pressed far from the hilly terrain and towards the Hirfanlô
dam lake to the SW. We will see in the next sections that
this hilly alignment delineates the starting line of slices
that moved more or less southwards along detachment
faults whilst another southern lineament, sub-parallel to
this line, corresponds to the trace of the Savcôlô Thrust
Fault. Almost no topographic signature could be associat-
ed to the fault trace in the DEM.

The Savcôlô Thrust zone

The Savcôlô Thrust Fault (STF) is observed typically

near Sôddôkdede (Fig. 4) along a contact between the
northern Eocene detrital rocks and the southern metamor-
phic and magmatic rocks (Fig. 5). Along the faulted con-
tact that dips about 45°, the Eocene strata are reversed and
folded. A few hundreds of meters northerly, the Eocene de-
trital rocks are exposed in a south-vergent asymmetric
fold, a folding geometry in contradiction to the northerly
thrusting movement. The thrust zone does not affect a
zone larger than a few hundreds of meters north of which
the Eocene beddings have gentle dips. To the south of the
STF, a large area is composed of granitic rocks most of
which remain under the Hirfanlô dam lake. Further south,

background image



Fig. 5. A – Mosaic of photographs showing the Savcôlô Thrust Fault near Sôddôkdede locality (see Fig. 4 for its location). B – Geologi-
cal map of the area. C – A—B cross-section.

Fig. 6.  A – Geological map of the area at the south of the Aliöflez Mount, showing the Savcôlô Detachment Fault and Savcôlô Thrust
Fault (see Fig. 4 for its location). B – A—B cross-section. Dashed heavy line below the topographic detachment surface denotes the de-
tachment fault that initiates at the northern vicinity of the Aliöflez Mount. C – Detail of the thrust fault zone.

background image



plutonic rocks crop out again along the granitic belt that
extends up to the Tuz Gölü Fault zone (Fig. 2).

The thrust fault can also be observed on the southern

flanks of the SE-trending hills (Figs. 3, 4). One of these
topographic highs is the Aliöflez Mount, comprising at
the lowest parts wollastonite-bearing calc-silicatic
gneisses overlain by Eocene rocks that crop out in the
highest parts (Fig. 6). The surface of the southern flank of
this mount is an extensional fault that will be described
in the next section. The flank ends at a small stream
where the sedimentary and metamorphic rocks are juxta-
posed to granitic rocks along a subvertical contact. Dips
of the beddings/foliations of the sedimentary/metamor-
phic rocks gradually increase when approaching the con-
tact that appears to be an almost vertical reverse fault
along which the southern plutonic rocks overthrusted the
northern cover units. The granitic rocks of the contact
are highly fractured and have an arenitic appearance.
Near the contact and within the granites, subhorizontal
tensional fractures filled with few centimeters thick cal-
cite suggest subvertical stretching of the material associ-
ated with subhorizontal shortening.

Evidence of extensional tectonics

In the vicinity of the Savcôlô Thrust Fault (STF), exten-

sional tectonics are shown by the presence of low-angle
normal faults cropping out between the SE—NW trending
alignment of hills, such the Aliöflez Mount, at the north,
and the thrust zone, at the south. There, metamorphic rock
slices capped by Eocene rocks moved downslope and
southwards along normal faults from the highest points of
these hills, for about 2 km to end up on the thrust zone
along and south of which granitic rocks crop out (for geo-
logical map and cross-section, see Fig. 6). The Fig. 7 illus-
trates a general view of the study area in which normal and
thrust faulting are shown. In many places, varied mesoscop-
ic structures (Fig. 8) attest to the low-angle normal faulting.
Amongst them, there are faulted contacts between Eocene
limestones and Eocene clastic rocks (Fig. 8a and b), fault
surfaces traced with shear fractures bisected by groove
marks, slickenlines and elongated pebbles of the Eocene
basal conglomerates due to shearing, found in both the
Eocene and metamorphic rocks (locally calc-silicate gneiss-

es) (Fig. 8a,b,c,d,e,f and g).  In the topographically highest
parts, at the ùnlidaû Mount for instance, the movements be-
tween gliding slices are accommodated by several N-trend-
ing strike-slip faults (Fig. 8d). There, the southern faces of
the Eocene rocks are extensively fractured (marked as
“stretched rocks” in Fig. 8d), possibly as a result of splitting
due to extensional forces that existed between the hanging-
wall rocks that slid and those that remained in place. On the
gently dipping detachment fault surfaces, slickenlines are
clear within Eocene rocks (Fig. 8e). At Lele Hill, normal
faulting is obvious at the summit of the hill within meta-
morphic rocks (Fig. 8i). Downwards and in metamorphic
rocks, the fault surfaces display an almost flat geometry
when viewed from afar, and in detail, the surfaces are fre-
quently cut by crescent-shaped extensional fractures with
downslope concavity, most of them dipping with high an-
gles in the same sense as the surface dips (Fig. 8h). Along
these structures, metamorphic rocks are offset for several
centimeters downslope so as to generate a step-like mor-
phology on the surface. Again in metamorphic rocks, the
transport direction is suggested by groove marks, but also
by quartzite fragments embedded in the foot-wall block sur-
face (Fig. 8g). Some elongate-shaped of these accreted ob-
jects have their long axes aligned parallel to the groove
marks but they are not associated with a channel-shaped tail
often observed along fault surfaces, an observation that is
used to better determine the shear sense. Near the STF where
the hanging-wall blocks can be observed, mylonitization
affects the Eocene strata at the bottom parts of these blocks
(see the sheared and elongated pebbles of the middle
Eocene basal conglomerates in Fig. 8b and f). Further field
observations are necessary to establish a detailed rock
stratigraphy (undeformed, mylonitic, brecciated mylonitic
zones etc.) associated with detachment faulting.

The geometry of the cross-section and kinematic mark-

ers observed suggest a general downslope tectonic trans-
port in an approximately N-S direction and towards the
south (Fig. 9).The transport is accommodated by normal
faults with steeply to moderately dipping surfaces while
the dip of the fault becomes almost horizontal in some
parts of the flank between the northern heights and the
southern STF (see Fig. 6). This geometry of this kilometric
low-angle normal fault, where the dip angle of the fault
surface decreases away from its topographically high sec-
tor, is similar to detachment faults already recognized

Fig. 7. Mosaic of photographs taken to show the Savcôlô Detachment Fault and Savcôlô Thrust Fault, in a N-S section at the western vi-
cinity of the Aliöflez Mount.

background image



Fig. 8. Several structural aspects of the detachment faulting observed along the section shown in Fig. 7. In each picture, the view direction
is given next to the inset letter as well as the lithological and structural elements are written. In (F), the length of the pen scale is 12 centi-
meters. In (H), the arrows indicate the trace of one of the several crescent-shaped structures observed along the fault surface and in meta-
morphic rocks.

background image



Fig. 9. Lower hemisphere Schmidt projection of structural data col-
lected on and near the Savcôlô Detachment Fault surfaces. Normal
and strike-slip faults and associated lineations together with kine-
matic indicators like groove marks, extensional fractures and veins,
and southward concave crescent structures suggest a NNE—SSW ex-
tension, accommodated by the displacements of hanging-wall units
from NNE towards SSW.

Fig. 10. Geological cross-section around the Karaabalô village (see Fig. 4 for its location). Vertical exaggeration is 2.

from previous studies (e.g. Harris et al. 2002). We therefore
call this structure the Savcôlô Detachment Fault.

These gravitational movements have generated a gently

rolling landscape characterized by the repetition of whit-
ish Eocene outcrops in particular near the hill alignment.
A good example can be observed near Karaabalô village
where several low-angle normal faults have generated this
morphological feature along several kilometers (Fig. 10).
Another aspect of these tectonics is the tilting of the
Eocene strata to almost vertical (Fig. 11) in the vicinity of
Ebri im village. This is likely the result of block rotations
about horizontal axes due to movements along normal
fault surfaces.

Significance and cause of thrusting

As seen in digital elevation models, the Savcôlô Thrust

Fault (STF) is associated with almost no topographic sig-
nature, and in the field, its width of not more than a hun-
dred of meters does not suggest the presence of an
important crustal structure, as it would be when consider-
ing the geotectonic role previously ascribed to this struc-
ture (e.g. Görür et al. 1998). Morphologically, the STF is
much less pronounced compared to the elements of the
surrounding extensional structures.

The field data do not allow us to propose a chronology

for the thrust and detachment faulting events in the study
area, and these events may well have occurred in different
periods. Nevertheless, the folding vergence of the foreland
units suggests that the crustal portions that moved by de-
tachment faulting were stopped against the granitic mass-
es to the south. A structural scenario in which the Eocene
rocks and their metamorphic basement rocks have moved
along detachment faults and were blocked by a southern

background image



Fig. 11. Geological cross-section around the Ebri im village (see Fig. 4 for its location).

granitic relief during a post-middle Eocene period is con-
ceivable since the middle Eocene clastic sedimentary
rocks comprise granitic pebbles indicating that during
Eocene deposition clastic rocks were supplied by material
from a subaerial source of granitic rocks. In the Eocene
conglomerates, the nature of the clastic material becomes
dominantly granitic when approaching the southern gra-
nitic exposures. Consequently, it may be proposed that a
regional crustal extension was accommodated by detach-
ment faults in the post-middle Eocene time, and that the
northern slices could not move further south than the gra-
nitic heights. At this point, the question is if the granitic
rocks were not affected by these extensional displace-
ments. Alternatively, thrusting may have a structural link
with the Neogene activity of the Tuz Gölü Fault (TGF), in
the SW of the study area. It may be induced due to the mi-
gration of the detachment faulting activity from the study
area towards the TGF, a phenomenon that is known from
earlier works (e.g. Lister & Davis 1989).

Crustal extension in the study area may have initiated

during the Neogene time as in the Neogene activity of the
TGF (Dhont et al. 1998; Çemen et al. 1999). On a larger
scale, this extension seems to be coeval with the Aegean
extension at the west of Turkey (Dhont et al. 1998; Koçy-
iûit et al. 1999; Bozkurt 2000; Seyitoûlu et al. 2002), a
geotectonic event generally attached to subductional pro-
cesses between the African and Eurasian plates in the East-
ern Mediterranean (e.g. Seyitoûlu & Scott 1996).


Field observations undertaken around the Kôr ehir city, in

Central Anatolia, suggest that the Savcôlô Thrust Fault
(STF) zone developed in an area that experienced exten-
sional tectonics accommodated by low-angle normal faults,
in the post-middle Eocene period. The vicinity and paral-
lelism of the compressional and extensional structures as

well as the geometry of the foreland folding suggest a struc-
tural causality between the gravitationally moving blocks
and the thrusting event. We interpret the STF as a secondary
structure developed on the northern flank of a granitic belt
due to the collision of this belt front with the southerly glid-
ing metamorphic and sedimentary slices. Further research
has to be concentrated to understand how this thrust formed
in the extensional regime and how this regime is associated
with the southern nearby detachment faulting event along
the Tuz Gölü Fault zone.

Acknowledgments:  We are thankful to Halil Türkmen, ge-
ologist at MTA, for his help and assistance during the
field work. We also wish to express our thanks to Dušan
Plašienka and Erdin Bozkurt whose subtle suggestions
were useful to improve the paper.


Ataman G. 1972: A preliminary study on the radiometric age of the

Cefalôk Daû, one of the granitic-granodioritic massifs at the SE
of Ankara. Hacettepe Fen ve Mühendislik Bilimleri Dergisi, 2,
44—49 (in Turkish with English abstract).

Aydôn N.S. & Önen P. 1999: Field, petrographic and geochemical

features of the Baranadaû Quartz Monzonite of the Central Ana-
tolian granitoids, Turkey. Turkish J. Earth Sci. 8, 113—124.

Bozkurt E. 2000: Timing of extension on the Büyük Menderes gra-

ben, Western Turkey and its tectonic implications. In: Bozkurt
E., Winchester J.A. & Piper J.D.A. (Eds.): Tectonics and mag-
matism in Turkey and the surrounding area. Geol. Soc. Lon-
don, Spec. Publ. 173, 385—403.

Boztuû D. 2000: S-I-A type intrusive associations: geodynamic sig-

nificance of synchronism between metamorphism and magma-
tism in Central Anatolia, Turkey. In: Bozkurt E., Winchester
J.A. & Piper J.D. (Eds.): Tectonics and magmatism in Turkey
and surrounding area. Geol. Soc. London, Spec. Publ. 173,

Brinkmann R. 1971: Das kristalline Grundgebirge von Anatolien.

Geol. Rdsch. 60, 886—899.

background image



Brinkmann R. 1976: Geology of Turkey. Elsevier, Amsterdam,


Çemen  ù., Göncüoûlu M.C. & Dirik K. 1999: Structural evolution

of the Tuzgölü Basin in Central Anatolia, Turkey. J. Geol.
107, 693—706.

Dhont D., Chorowicz J., Yürür T., Froger J.-L., Köse O. & Gün-

doûdu N. 1998: Emplacement of volcanic vents and geody-
namics of Central Anatolia, Turkey. J. Volcanol. Geothermal
Res. 85, 1998, 33—54.

Dirik K. 2001: Neotectonic evolution of the northwestward arched

segment of the Central Anatolian Fault Zone, Central Anatolia-
Turkey.  Geodinamica Acta 14, 147—158.

Dirik K. & Göncüoûlu M.C. 1996: Neotectonic characteristics of

the Central Anatolia. Int. Geol. Rev. 38, 807—817.

Erkan Y. 1976: Isogrades determined in the regional metamorphic

area surrounding Kôr ehir and their petrological interpretation.
Yerbilimleri 2, 1, 23—54 (in Turkish with English abstract).

Erkan Y. & Ataman G. 1981: A study on the age of metamorphism

of Central Anatolian Massif (Kôr ehir Region) by K-Ar meth-
od. Yerbilimleri 8, 27—30 (in Turkish with English abstract).

Gautier P., Bozkurt E., Hallot E. & Dirik K. 2002: Dating the exhu-

mation of a metamorphic dome: geological evidence for pre-
Eocene unroofing of the Niûde Massif (Central Anatolia,
Turkey).  Geol. Mag. 130, 05, 559—576.

Genç Y. 2003: New observations on the metamorphic stratigraphy

of the Kôr ehir Massif. Extended Abstract Book,  56



cal Congress of Turkey, Ankara 55—56.

Genç Y. 2004: Savcôlô migmatite-dome hosted gold-quartz veins in

Kôr ehir Metamorphic Core Complex (KMCC), Central Anato-
lia, Turkey. In: Chatzipetros A.A. & Pavlides S.B. (Eds.): Pro-
ceedings of the 5


 Int. Symposium on Eastern Mediterranean

Geology, Thessalloniki, Greece. April 2004. Vol. 3, 1394—
1397, 14—20.

Genç Y. & Yürür T. 2004: The Kôr ehir detachment faulting and a

new interpretation of the “Savcôlô Thrust Zone” in central Ana-
tolia, Turkey. In: Chatzipetros A.A. & Pavlides S.B. (Eds.):
Proceedings  5


 of the International Symposium on Eastern

Mediterranean Geology, Thessalloniki, Greece. April 2004.
Vol. 1,  73—76, 14—20.

Göncüoûlu M.C., Toprak V., Ku çu ù., Erler A. & Olgun E. 1991:

Geology of the western part of the central Anatolian Massif,
Part 1: Southern Sector. TPAO Report No. 2909, 1—140 (in
Turkish with English abstract).

Görür N., Tüysüz O. &  engör A.M.C. 1998: Tectonic evolution of

the Central Anatolian basins. Int. Geol. Rev. 40, 831—850.

Güleç N., Hilton D.R. & Mutlu H. 2002: Helium and heat distribu-

tion in Turkey: relations to tectonic provinces, volcanism and
recent seismic activities. Chem. Geol. 187, 129—142.

Harris L.B., Koyi H.A. & Fossen H. 2002: Mechanisms for folding

of high-grade rocks in extensional tectonic settings. Earth Sci.
Rev.  59, 163—210.

Ketin I. 1955: On the geology of Yozgat region and the tectonic

features of the Central Anatolian Massif (Kôr ehir Crystallines).
Bull. Geol. Soc. Turkey VI/1, 1—20 (in Turkish with English

Ketin I. 1966: Tectonic units of Anatolia. Bull. General Directorate

of Mineral Research and Exploration 66, 23—34.

Koçyiûit A., Yusufoûlu H. & Bozkurt E. 1999: Evidence from the

Gediz graben for episodic two-stage extension in western Tur-
key.  J. Geol. Soc. London Vol. 156, 1999, 605—616.

Ku çu I., Gencalioûlu-Ku çu G., Meinert L.D. & Floyd P.A. 2002:

Tectonic setting and petrogenesis of the Çelebi granitoid,
(Kôrôkkale-Turkey) and comparison with world skarn grani-
toids,  J. Geochem. Exploration 76, 3, 175—194.

Lister G.S. & Davis G.A. 1989: The origin of metamorphic core

complexes and detachment faults formed during Tertiary con-
tinental extension in the northern Colorado River region,
U.S.A. J. Struct. Geol. 11, 65—94.

MTA 2002: Geological maps of Turkey in 1:500,000 scale (Ankara

sheet). General Directorate of Mineral Research and Explora-
tion,  Ankara, Turkey.

Oktay F.Y. 1981: Geology and sedimentology of the sedimentary

cover of the central Anatolian Massif around Savcôlôbüyükoba
(Kaman).  ù.T.Ü. Maden Fakültesi (unpublished Thesis), ùstan-
bul, 1—175 (in Turkish with English abstract).

Piper J.D.A., Gürsoy H. & Tatar O. 2002: Palaeomagnetism and

magnetic properties of the Cappadocian ignimbrite succession,
central Turkey and Neogene tectonics of the Anatolian col-
lage.  J. Volcanol. Geothermal Res. 117, 3—4, 237—262.

Pollak A. 1958: Über einige geologische Beobachtungen im zen-

tral-anatolischen Massiv. Notizbl. Hess. Landesamt Bodenfors-
chung 87, 239—245.

Seyitoûlu G. & Scott B.C. 1996: The cause of N-S extensional tec-

tonics in western Turkey: Tectonic escape vs. back-arc spread-
ing vs. orogenic collapse. J. Geodynamics 22, 145—153.

Seyitoûlu G., Tekeli O., Çemen ù.,  en  . & I ôk V. 2002: The role

of the flexural rotation/rolling hinge model in the tectonic
evolution of the Ala ehir graben, western Turkey. Geol. Mag.
139, 1, 2002, 15—26.

Seymen I. 1981: Stratigraphy and metamorphism of the Kôr ehir

Massif around Kaman (Kôr ehir, Turkey). Bull. Geol. Soc.
Turkey 24, 101—108 (in Turkish with English abstract).

Seymen I. 1982: Geology of Kôr ehir Massif around Kaman. I.T.U.

Min. Fac. (unpublished Thesis), Istanbul, 1—164 (in Turkish
with English abstract).

Seymen I. 1984: Geological evolution of the metamorphic rocks in

the Kôr ehir Massif. Geol. Soc. Turkey, Ketin Symposium Book
133—148 (in Turkish with English abstract).

Seymen I. 2000: Geology of the Kôr ehir Massif between the

Savcôlôebeyit (Kaman) and Ye illi (Kôr ehir) villages. Congress
of Geosciences and Mining for the 75


 anniversary of the

Turkish Republic. Proceedings Book I,  MTA-Ankara 67—91
(in Turkish with English abstract).

engör A.M.C. 1980: Principles of neotectonism of Turkey. Geol.

Soc. Turkey, Conference Series, No. 2, 40 (in Turkish).

engör A.M.C. & Yôlmaz Y. 1981: Tethyan evolution of Turkey:

A plate tectonic approach. Tectonophysics 75, 181—241.

engör A.M.C., Görür N. &  aroûlu F. 1985: Strike-slip faulting

and related basin formation in zones of tectonic escape: Tur-
key a case study. In: Biddle K.T. & Christie-Blick N. (Eds.):
Strike-slip deformation, basin formation, and sedimentation.
Soc. Econ. Paleont. Mineral. Spec. Publ. 37, 227—264 (in
honor of J.C. Crowell).

Whitney D.L. & Dilek Y. 1998: Metamorphism during Alpine crustal

thickening and extension in Central Anatolia, Turkey: the Niûde
metamorphic core complex. J. Petrology 39, 70, 1385—1403.

Whitney D.L., Teyssier C., Dilek Y. & Fayon A.K. 2001: Metamor-

phism of the Central Anatolian Crystalline complex, Turkey:
influence of orogen-normal collision vs. wrench-dominated
tectonics on P-T-t paths. J. Metamorph. Geology 19, 411—432.