Comparison of the offsets in dreinage network with some tectonic data between Karlıova-Türkoğlu in the East Anatolian fault zone, East Anatolia/Turkey

Doğu Anadolu Fay Zonu Türkiye'nin doğusunda Güneydoğu Torosları ve bu dağlar arasındaki çöküntü ovalarını yaklaşık KD-GB doğrultusunda kesen, sol yanal, doğrultu atımlı, aktif bir fay zonudur. Fay sistemi farklı doğrultularda, yer yer kademeli yön değiştiren çok sayıda bölümden (segment) oluşmakta ve genç morfolojisi ile arazide açık olarak izlenmektedir. Türkiye’nin önemli neotektonik yapılarından biri olan Doğu Anadolu Fay Zonu Alt Pliyosen’de ortaya çıkmıştır. Pliyosen’den önce kurulan büyük akarsular fay tarafından ötelenmiştir. Pliyosen ve geç dönemlerde kurulan akarsular fay zonuna yerleşmiştir. Fayın gençleşmesi akarsu ağında ötelenmelere, keskin dirseklerin oluşumuna neden olmuştur. Drenaj sistemindeki değişikliklerden fayın yanal atımı, fayın gençleşme dönemleri ve faya bağlı jeomorfolojik birimler konusunda bilgiler elde edilmiştir. Doğu Anadolu Fay Zonu boyunca Karlıova’dan Türkoğlu’na doğru Palu çevresinde Irgat (Caru) Çayı 10 km, Doğanyol ile Hazar Gölü arasında Fırat Nehri 13 km, Gölbaşı ile Erkenek Ovası arasında Fırat Nehri’nin kolu olan Göksu Çayı’na ait Kapı Deresi ve vadisi 14 km, Göksu Çayı ve vadisi 32 km, Aksu Çayı’nın kolları olan Kısık ve Koca dereleri 5 km sol yanal ötelenmiştir. Fay zonu boyunca tespit edilen en büyük akarsu ötelenmesi olan Göksu Çayı vadisindeki 32 km’lik ötelenmenin yörede yapılacak yapısal ve morfolojik araştırmalarla teyit edilmesi gerekir. Doğu Anadolu Fay Zonu’ndaki akarsularda ortaya çıkan ötelenmeler akarsuların kuruluş dönemlerine bağlı olarak değişmekte ve belirli değerlerde sıkça görülmektedir. Yapı ve morfoloji ilişkisine göre bu değerler 0-250 m’ye kadar Holosen, 250-1500 m ve 4-5 km; Pleyistosen, 5-32 km arasında ise Pliyosen dönemlerine ait olmalıdır. Fırat Nehri ve kolu olan Göksu Çayı ile Ceyhan Nehri’nin kolu olan Aksu Çayı’nın kuruluşu faydan eskidir. Dolayısıyla bu akarsulardaki ötelenme değerleri fayın toplam yanal atımına daha yakın değerler olarak yorumlanabilir. Akarsu ötelenmelerinin değeri Karlıova'dan Türkoğlu’na doğru artmaktadır. Akarsu ağma göre fayın öncelikle Antakya-Maraş arasında ortaya çıktığı, daha geç zamanlarda segmentler halinde kırılarak Karlıova'ya ulaştığı ileri sürülebilir. Akarsuların kuruluşu, drenajdaki ötelenmeler, fayın genç morfolojisi, faya bağlı oluşan havzalar, fayın Kuvaterner dönemine ait yer şekillerini kesmesi, deforme etmesi, zon boyunca görülen şiddetli depremler Doğu Anadolu Fay Zonu’nun Alt Pliyosen tektonik hareketleri ile ortaya çıktığını, Pliyosen, Pleyistosen, Holosen ve tarihi dönemlerde zaman zaman gençleştiğini ve fayın aktif olduğunu göstermektedir.The East Anatolian Fault Zone which cuts depression betvveen the Southeast Taurus and these mountains in Eastern Turkey in the direction of NE-SW, approximately is a left lateral, strike-slip, active fault zone. The East Anatolian fault system consists of lots of segments in different directions have step-like change in its directions. In addition, this fault with its young morphology can be clearly seen in the field. The East Anatolian fault zone, which is one of the important Neo-tectonic structures of Turkey, has appeared in the Lower Pliocene Period. The river drainage which was formed Pre-Pliocene time offset by the fault. The rivers which were formed in the Pliocene and later periods settled to the fault zone. Reactivation of the fault caused offsets in the river drainage and the formation of the sharp tums of the rivers. The strike slip of the fault is obtained from these changes in the drainage system. Throughout the East Anatolian Fault Zone the following rivers, streams, and valleys have been taken from following left lateral offsets: Irgat (Caru) stream around Palu 10 km; Euphrates betvveen Doğanyol and Hazar lake 13 km; Kapı stream of Göksu river, which is a tributary of Euphrates, is betvveen Gölbaşı and Erkenek plain 14 km; Göksu river and its valley 32 km; Kısık and Koca streams and their valleys vvhich are the tributaries of Aksu river 5 km. These values of Göksu are the biggest river displacement that have been observed along the fault zone. New researches must be for the straightness in terms of structural and morphological of that value. Offsets which appear in the rivers of East Anatolian Zone, change depend on the period of their establishment and also are seen in certain values, frequently. According to the relations of structure and morphology, these values in 0-250 m accepted as the Holocene, 250- 1500 m and 4-5 km described as the Pleistocene, betvveen 5-32 km accepted as Pliocene periods. Establishment Euphrates river and its Göksu tributary, Aksu stream, which is a tributary of the Ceyhan river, are older than the fault. So the offset values of these rivers can be said to be closer values to the total lateral. The value of river offset increases from Karlıova to Antakya. By taking into consideration this can be clearly said that, at the beginning of the fault appears betvveen Antakya and Maraş, and reached Karlıova by being broken as segments in following times. The formation of the rivers, drainage displacements, young morphology of the fault, basins formed by the fault, the cutting of the Quaternary landforms by the fault and observed destructive earthquakes along the zone show that East Anatolian fault has appeared with lovver Pliocene tectonic movements. Moreover', above mentioned these characteristics indicate that the fault reactivated in Pliocene, Pleistocene, Holocene and historical periods and it is an active fault

Comparison of the offsets in dreinage network with some tectonic data between Karlıova-Türkoğlu in the East Anatolian fault zone, East Anatolia/Turkey

Doğu Anadolu Fay Zonu Türkiye'nin doğusunda Güneydoğu Torosları ve bu dağlar arasındaki çöküntü ovalarını yaklaşık KD-GB doğrultusunda kesen, sol yanal, doğrultu atımlı, aktif bir fay zonudur. Fay sistemi farklı doğrultularda, yer yer kademeli yön değiştiren çok sayıda bölümden (segment) oluşmakta ve genç morfolojisi ile arazide açık olarak izlenmektedir. Türkiye’nin önemli neotektonik yapılarından biri olan Doğu Anadolu Fay Zonu Alt Pliyosen’de ortaya çıkmıştır. Pliyosen’den önce kurulan büyük akarsular fay tarafından ötelenmiştir. Pliyosen ve geç dönemlerde kurulan akarsular fay zonuna yerleşmiştir. Fayın gençleşmesi akarsu ağında ötelenmelere, keskin dirseklerin oluşumuna neden olmuştur. Drenaj sistemindeki değişikliklerden fayın yanal atımı, fayın gençleşme dönemleri ve faya bağlı jeomorfolojik birimler konusunda bilgiler elde edilmiştir. Doğu Anadolu Fay Zonu boyunca Karlıova’dan Türkoğlu’na doğru Palu çevresinde Irgat (Caru) Çayı 10 km, Doğanyol ile Hazar Gölü arasında Fırat Nehri 13 km, Gölbaşı ile Erkenek Ovası arasında Fırat Nehri’nin kolu olan Göksu Çayı’na ait Kapı Deresi ve vadisi 14 km, Göksu Çayı ve vadisi 32 km, Aksu Çayı’nın kolları olan Kısık ve Koca dereleri 5 km sol yanal ötelenmiştir. Fay zonu boyunca tespit edilen en büyük akarsu ötelenmesi olan Göksu Çayı vadisindeki 32 km’lik ötelenmenin yörede yapılacak yapısal ve morfolojik araştırmalarla teyit edilmesi gerekir. Doğu Anadolu Fay Zonu’ndaki akarsularda ortaya çıkan ötelenmeler akarsuların kuruluş dönemlerine bağlı olarak değişmekte ve belirli değerlerde sıkça görülmektedir. Yapı ve morfoloji ilişkisine göre bu değerler 0-250 m’ye kadar Holosen, 250-1500 m ve 4-5 km; Pleyistosen, 5-32 km arasında ise Pliyosen dönemlerine ait olmalıdır. Fırat Nehri ve kolu olan Göksu Çayı ile Ceyhan Nehri’nin kolu olan Aksu Çayı’nın kuruluşu faydan eskidir. Dolayısıyla bu akarsulardaki ötelenme değerleri fayın toplam yanal atımına daha yakın değerler olarak yorumlanabilir. Akarsu ötelenmelerinin değeri Karlıova'dan Türkoğlu’na doğru artmaktadır. Akarsu ağma göre fayın öncelikle Antakya-Maraş arasında ortaya çıktığı, daha geç zamanlarda segmentler halinde kırılarak Karlıova'ya ulaştığı ileri sürülebilir. Akarsuların kuruluşu, drenajdaki ötelenmeler, fayın genç morfolojisi, faya bağlı oluşan havzalar, fayın Kuvaterner dönemine ait yer şekillerini kesmesi, deforme etmesi, zon boyunca görülen şiddetli depremler Doğu Anadolu Fay Zonu’nun Alt Pliyosen tektonik hareketleri ile ortaya çıktığını, Pliyosen, Pleyistosen, Holosen ve tarihi dönemlerde zaman zaman gençleştiğini ve fayın aktif olduğunu göstermektedir.The East Anatolian Fault Zone which cuts depression betvveen the Southeast Taurus and these mountains in Eastern Turkey in the direction of NE-SW, approximately is a left lateral, strike-slip, active fault zone. The East Anatolian fault system consists of lots of segments in different directions have step-like change in its directions. In addition, this fault with its young morphology can be clearly seen in the field. The East Anatolian fault zone, which is one of the important Neo-tectonic structures of Turkey, has appeared in the Lower Pliocene Period. The river drainage which was formed Pre-Pliocene time offset by the fault. The rivers which were formed in the Pliocene and later periods settled to the fault zone. Reactivation of the fault caused offsets in the river drainage and the formation of the sharp tums of the rivers. The strike slip of the fault is obtained from these changes in the drainage system. Throughout the East Anatolian Fault Zone the following rivers, streams, and valleys have been taken from following left lateral offsets: Irgat (Caru) stream around Palu 10 km; Euphrates betvveen Doğanyol and Hazar lake 13 km; Kapı stream of Göksu river, which is a tributary of Euphrates, is betvveen Gölbaşı and Erkenek plain 14 km; Göksu river and its valley 32 km; Kısık and Koca streams and their valleys vvhich are the tributaries of Aksu river 5 km. These values of Göksu are the biggest river displacement that have been observed along the fault zone. New researches must be for the straightness in terms of structural and morphological of that value. Offsets which appear in the rivers of East Anatolian Zone, change depend on the period of their establishment and also are seen in certain values, frequently. According to the relations of structure and morphology, these values in 0-250 m accepted as the Holocene, 250- 1500 m and 4-5 km described as the Pleistocene, betvveen 5-32 km accepted as Pliocene periods. Establishment Euphrates river and its Göksu tributary, Aksu stream, which is a tributary of the Ceyhan river, are older than the fault. So the offset values of these rivers can be said to be closer values to the total lateral. The value of river offset increases from Karlıova to Antakya. By taking into consideration this can be clearly said that, at the beginning of the fault appears betvveen Antakya and Maraş, and reached Karlıova by being broken as segments in following times. The formation of the rivers, drainage displacements, young morphology of the fault, basins formed by the fault, the cutting of the Quaternary landforms by the fault and observed destructive earthquakes along the zone show that East Anatolian fault has appeared with lovver Pliocene tectonic movements. Moreover', above mentioned these characteristics indicate that the fault reactivated in Pliocene, Pleistocene, Holocene and historical periods and it is an active fault

3D-Architecture and Neogene Evolution of the Malatya Basin: Inferences for the Kinematics of the Malatya and Ovacık Fault Zones

The 3D-architecture of the Malatya Basin was studied using remote sensing, seismic interpretation, and palaeostress analysis in the context of the Malatya-Ovacık fault zone. The results indicate that the Ovacık and Malatya fault zones are not different segments of a single 'so called' Malatya-Ovacık fault zone; rather, they are two different fault zones that have operated independently. In addition, the Ovacık fault zone is delimited in the west by the Malatya fault zone, which extends farther north from the point of supposed junction. Maximum individual deflection of streams along the Ovacık fault zone is about 9.3 km, and summation of all stream deflections along different segments of the Ovacık fault zone indicates that sinistral displacement of the Ovacık fault zone has been not more than 20 km following development of the drainage system in the region. Evidence for three different deformation phases were recognized in the Malatya Basin. Deformation phase 1 was characterized by NW-SE-directed extension and operated in the Early to Middle Miocene interval. Deformation phase 2 was characterized by WNW-ESE-directed compression and a vertical s2 which indicates transcurrent tectonics. It operated in the Late Miocene to Middle Pliocene. Deformation phase 3 was characterized by NNE-SSW-directed compression, and vertical stress is interchanged with s2 and s3; this is interpreted as due to near equal magnitudes of these stresses, resulting in stress permutation and interchange of intermediate and minor stress. Deformation phase 3 commenced in the Late Pliocene and has been active since then. The infill of the Malatya Basin has wedge-like geometry in E-W and N-S directions and the basin fed detritus mainly from its eastern margin. During field studies in the basin, a number of inverted normal faults were encountered; these apparently developed as growth faults in the Early to Middle Miocene time interval and then were reactivated or inverted during post-Middle Miocene compressional phase

The Palu-Uluova Strike-Slip Basin in the East Anatolian Fault System, Turkey: Its Transition from the Palaeotectonic to Neotectonic Stage

The East Anatolian fault system (EAFS) is the 80-km-wide, 700-km-long, NE-trending sinistral strike-slip fault system forming a seismically very active intracontinental transfom fault boundary. It is located between Karhova County in the northeast and Karatas-Samandag counties in the southwest, and forms the southeastern boundary of the Anatolian platelet. The Palu-Uluova basin is one of several strike-slip basins located along the EAFS. It is surrounded by several push-ups such as the Karaomerdagi, Mastardagi and Askerdagi push-ups caused by the complexities peculiar to strike-slip faulting. The Palu-Uluova basin consists of three sub-sections: two are NE-trending strike-slip sub-basins, the Uluova and the Palu-Kumyazi sub-basins, while the third is a ramp basin, the E-W-trending Yolustu basin which links the earlier two sub-basins. The Palu-Uluova basin is characterized and shaped by a 130-m-thick neotectonic basin infill (Palu Formation) and a series of bounding strike-slip fault zones such as the Sivrice, Adiyaman, Uluova, Elazig, Pertek and Yolustu fault zones. The Palu Formation is an undeformed fluvio-lacustrine sedimentary sequence. The youngest palaeotectonic rock-stratigraphic unit is the Upper Miocene-Lower Pliocene caybagi Formation, deposited in a ramp type of intermontane basin bounded and controlled by the reverse faults. The caybagi Formation is intensely deformed (steeply tilted, folded and thrust to reverse-faulted) on a regional (mappable) scale. The compressional deformation pattern of the Caybagi Formation is truncated, sealed and overlain with angular unconformity by the nearly horizontal undeformed Plio-Quaternary Palu Formation. This regional angular unconformity reflects: (a) a series of pre-Late Pliocene regional tectonic inversions (e.g., type of the tectonic regime, style of deformation and nature of magmatic activity), and (b) the timing of the major transition from the folding and thrust to reverse faulting-dominated palaeotectonic period into the strike-slip faulting-dominated neotectonic period is Late Pliocene

Late Cretaceous to Recent kinematics of SE Anatolia (Turkey)

Five different deformation phases have been recognized in the SE Anatolian orogen and the Arabian Platform based on palaeostress inversion studies using fault-slip data sets. The timing and duration of these phases are determined using various criteria including the age of the affected strata, syndepositional structures, cross-cutting structures and overprinting slickensides. The oldest deformation phase is characterized generally by NE-SW-directed extension. The extension is thought to have resulted from slab-roll back processes during the Maastrichtian to Middle Eocene interval (c. 60 Ma to 40-35 Ma). The second deformation phase is characterized by east-west to NW-SE-directed compression and thought to result from cessation of roll-back processes possibly due to subduction of younger oceanic crust or increase in the convergence rate between Africa and Eurasia during the post-Middle Eocene to Late Oligocene interval (c. 40-35 Ma to 25 Ma). The third deformation phase is characterized by east-west to NW-SE-directed extension possibly due to slab detachment that initiated in Iran and migrated westwards during the latest Oligocene to Middle Miocene period (25-11 Ma). The fourth deformation phase is characterized by approximately north-south-directed compression due to collision and further northwards indentation of Arabian Plate by the end of Middle Miocene (11-3.5 Ma). The fifth and present deformation phase is characterized by NE-SW compression which might result from tectonic re-organization in the region since the Middle Pliocene (c. 3.5 Ma to recent)