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Numerical Simulation of Crustal Strain in Turkey from Continuous GNSS

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Numerical Simulation of Crustal Strain in Turkey from Continuous GNSS J. Geod. Sci. 2017; 7:113–129 Research Article Open Access Kutubuddin Ansari*, Ozsen Corumluoglu, and Sunil Kumar Sharma Numerical Simulation of Crustal Strain in Turkey from Continuous GNSS Measurements in the Interval 2009-2017 https://doi.org/10.1515/jogs-2017-0013 Keywords: Anatolian Fault, Crustal Strain, TPGN Received April 15, 2017; accepted September 18, 2017 Abstract: The present study investigates the crustal strain in Turkey by using data from the Turkish permanent GNSS 1 Introduction network (TPGN) and international GNSS services (IGS) ob- servations for a period of 9 years, 2009 t0 2017. The posi- Turkey is a seismically active area within the complex tional variation of GNSS sites is studied to understand the zone of collision between the Eurasian Plate and both coordinate reliability, interseismic and coseismic eects the African and Arabian Plates. The large part of the coun- and linear velocities as well as three dimensional princi- try lies on the Anatolian Plate which is a small plate pal strains across the country. The study of coordinate re- bounded by two major strike-slip fault zones, the right- liability shows that the horizontal and vertical residuals lateral North Anatolian Fault (NAF) and left-lateral East in 2013 and 2015 are of the order of 100 mm per coordi- Anatolian Fault (EAF) (Fig. 1). The Anatolian block is being nate or higher than those of 2009 and 2011 and 10 times pulled by the Hellenic trench rather than being pushed by higher than those of 2017. The changes in baseline length the Arabian plate, as a result the Arabian plate has been in relative to an arbitrary zero-oset for the selected period rapid collision with the Eurasian plates in Eastern Turkey shows that the most of the sites have displacement in the since 23.03 to 5.332 Ma (Miocene period) (Tatar et al., 2012). interval −10 to 10 mm but some sites have larger varia- The easternmost part of Turkey lies on the western end tions. These displacements are mostly related to motion of the Zagros folds and thrust belt, which is dominated of the Turkish tectonic plate, regional crustal deformation by thrust tectonics. The GNSS derived velocities relative to and small amounts of errors in GNSS positioning. The most Eurasia in Eastern Turkey is ~10 mm/yr with the regional GNSS site velocities located all over Turkey give signi- tectonics (Walters, 2012; McClusky et al., 2000). The west- cant information for the study. The GNSS data shows that ern part of the country is also aected by the zone of ex- the Anatolian plate relative to the Eurasia is moving in a tensional tectonics in the Aegean Sea caused by the south- western direction in the central part of Turkey and starts ward migration of the Hellenic arc. Western Turkey is ex- to move in a south-westerly direction in the west part of tending in N-S direction with an upper bound rate of 20 the country. The westward motion of Anatolia increases mm/yr south of 39.5oN (Ayhan et al., 2003). This region gradually from 20 mm/yr in central Anatolia to 30 mm/yr is also undertaking about 3.6 mm/yr extension in E-W di- in south-west Turkey. The numerical simulation of the rection (Eyidogan, 1988). The western Turkish border is a crustal strain in the Aegean region shows a maximum region of roughly 700×700 km2 showing small deforma- −6 1.0446×10 compressional principal strain rate while the tions (Jackson, 1994). The region has apparently experi- second principal strain rate is zero. The strain in Central enced collisional shortening probably due to the westward Anatolia is evidently dominated by extensional deforma- motion of the plate along continental Greece into a sta- tions and the principal strain rate reaches to 0.9589×10−6 with maximum extension. The Marmara Region network is subject to an extensional principal strain (0.6608×10−6) which is also revealed in the Mediterranean Region with a *Corresponding Author: Kutubuddin Ansari: Department of Geomatics Engineering, Izmir Katip Celebi University, Izmir-Turkey, 0.5682×10−6 extension. The present analysis of GNSS data E-mail: [email protected] over the region may complement towards the understand- Ozsen Corumluoglu: Department of Geomatics Engineering, Izmir ing of the stability of regional tectonics and long term Katip Celebi University, Izmir-Turkey aseismic strain inside the country. Sunil Kumar Sharma: College of computer and information Sci- ences, Majmaah University, Majmaah-Saudi Arabia Open Access. © 2017 Kutubuddin Ansari et al., published by De Gruyter Open. This work is licensed under the Creative Commons Attribution-NonCommercial-NoDerivs 4.0 License. 114 Ë Kutubuddin Ansari, Ozsen Corumluoglu, and Sunil Kumar Sharma tionary Ionic margin (Cianetti et al., 2001). The eect of this shortening into Western Turkey and across the Aegean Sea is a set of thrust faults, a series of folds, and sutures in mainland Greece (Scott, 1981). The boundary of south- west is marked by the Hellenic Arc and the region dis- tinguished by gravity anomalies, seismicity, volcanic and oceanic arc inside the trench supports the explanation of this region as a subduction zone (Scott, 1981). The bulk of seismicity increases signicantly in the west of Turkey Figure 2: The historical earthquakes of Turkey (according to our and generates a ring in the southern Aegean Sea around literature search) with red circle and the earthquakes from 2009 to the relative to the seismic region. The bulk of this ring in 2017 with red rectangular the south is the Hellenic subduction trench (Giunchi et al. 1996). This subduction arc is a result of the African and Aegean plates converging at a rate of ~33 mm/yr (Delph of Anatolia. The largest geodetic and modeled strain rate of −15 −1 et al., 2015). The African plate is moving slowly relative to 80 nanostrain/yr (2.6 × 10 s ) is achieved in the western Eurasia in a northward direction along the Hellenic trench part of the NAF (Jimenez-Munt and Sabadini, 2002). The (Jackson 1994). The subduction of the African plate along implications of low strains are studied in the western and the Cyprian arc in the south of Turkey is not well dened central Marmara Sea block that accounts for recoverable but it occurs there rather than the Hellenic arc (Reilinge et growth of elastic strain (Meade et al. 2002). By integrating al., 1997). the GNSS data from all over Turkey with the IGS network, we tried to estimate the crustal strain in Turkey between the years 2009 and 2017. 2 The GNSS Observations The global navigation satellite system (GNSS) is a tool that has been used to measure surface displacements within the accuracy of a few millimeters in seismically active re- gions. Causative faults or dislocations that slip and simu- late the measured surface displacement and velocity eld Figure 1: Large-scale tectonic features of the Turkey, the yellow can then be modelled to better understand where strain is arrows show approximate plate motions relative to stable Eurasia. accumulating in a seismic area. The high-precision GNSS The three sites namely (BALK, BOYT and SURF) are TPGN sites and is used geodetically to constrain the motion of sites in the ANKR is an IGS site seismological areas and examine the deformation of the crust (Ansari 2014). The permanent GNSS reference site The strong and shocking earthquakes experienced in networks are being implemented throughout the world. Turkey and the surrounding area in the last centuries The establishment of the GNSS plays a precious role for shows a most seismotectonic regional feature (Fig. 2, Ta- the study of Earth sciences. These types of networks are ble 1). The new catalogue given by Duman (Duman et al, used to augment the regional geodetic framework. The 2016) also represents fault plane solution parameters for analyses of continuous time series, in cases where no the 1517 earthquakes with Mw ≥ 4.0 in Turkey and its near abrupt changes have occurred in time series due to earth- vicinity from 1906 to 2012 (Duman et al, 2016). The para- quakes and the principal strain accumulation from the in- metric information includes epicenter, seismic moment, terseismic velocities, are the most common elds of in- nodal planes and principal axes. Based on magnitude, the terest (Sagiya et al. 2000, Lenk et al., 2003). The infor- distributions of the selected solutions included in the cat- mation about the mechanism of earthquakes during co- alogue are: 13 of Mw >7.0, 118 of 6.0 <Mw >7.0, 501 of 5.0 seismic deformation and the information about rheology <Mw > 6.0, 784 of 4.0 <Mw>5.0 and 101 of Mw <4.0 (Duman of the fault zone and surrounding crust can also be ob- et al, 2016). The maximum values of seismic strain rate are tained easily from the continuous time series recorded by placed in the Aegean and in the eastern and western parts dense and permanent GNSS networks (Ayhan et al. 2001; Numerical Simulation of Crustal Strain in Turkey Ë 115 Table 1: The list of historical earthquakes of Turkey available in literature according to my search till 2017 Date Time (LT) Place Location Magnitude Reference 17 CE - Alaşehir 38.21◦N; 28.31◦E -- Internet Classics Archive 13-12-115 - Antioch 36.10◦N; 36.10◦E 7.5 Ms NGDC 141 or 142 - Lycia 36.70◦N; 28.00◦E VIII - NGDC 262 - Southwest Anatolia 36.50◦N; 27.80◦E IX - NGDC 19-05-526 - Antioch - VIII - Procopius 14-12-557 - Constantinople 40.90◦N; 28.70◦E X - Agathias et al.
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