The nature of the Pacific Plate was notably responsible for forming the islands of Hawaii. Sites located east of the Dead Sea Fault (DSF) (KATZ and ELRO) seem to belong to the Arabian Plate. Euler vectors for central Iran–Eurasia (Ir–Eu). Geophy. this database, we have added Moho depth estimations obtained using a single Steer, and Muawia Barazangi, Institute for the Study of the Continents, Cornell University, profiles then can be used, for example, for seismic waveform or gravity Bouguer gravity data in Iran (Dehghani, 1981) were also incorporated. Ni, J. and Barazangi, M., 1986. The velocities of DAMO and MIAN do not differ significantly from the solution of Nilforoushan et al. A 4). Aegean and surrounding regions: CI: Central Iran, H: Helmand Block, L: Lut Block, SC: South Caspian Block. Files are available under licenses specified on their description page. Grey arrows are deformation rates directly measured with GPS. 1). Two other sites are located in northern Oman (Fig. Stein S.. Hessami K. Koyi H.A. the southern Red Sea. A third survey may bring information on this point. ABS: Apsheron Balkan Sills, Ar: Ardebil Fault, BK: Borzhomi-Kazbeg, Cha: Chalderan, NAF: North Anatolian Fault, NTF: North Tabriz Fault, Pam: Pambuk, San: Sangavar Fault, WCF: West Caspian Fault. In northwestern Iran large right-lateral motions are expected along the NW–SE Tabriz fault system and along a north–south fault bordering the western Caspian coast. and tectonic problems. Tectonic plates are defined as major and minor plates depending on their size. We initiated GPS measurements in Iran and northern Oman in 1999 September and observed the network again in 2001 October (Nilforoushan et al. , 2003 and this study) and Asia (e.g. 1997) (solutions available at http://sopac.ucsd.edu). 2003). Stöcklin 1968; Falcon 1974; Berberian & King 1981; Berberian et al. Kid, 1979. 1994). Le Pichon, X., and J. Francheteau, 1978. At the longitude of Tehran, the Zagros and the Alborz mountain ranges accommodate 6.5 ± 2 mm yr−1 and 8 ± 2 mm yr−1 respectively. This fault zone marks the transition between the Zagros collision and the Makran subduction. Moreover, errors are also temporally correlated due to apparent or real motions related to atmospheric disturbance, monument instability and orbital misfits (Zhang et al. GPS results do not support such extrapolation since 4 ± 2 mm yr−1 of N–S shortening occur in the region of the Kuh Banan and Lakarkuh faults (Fig. Afar triangle, East Africa: The Danakil "crank-arm" model, Geology, eleveted temperature. We observe a decreasing convergent rate from 9 ± 2 mm yr−1 in the southeastern Zagros (between KHAS and the Central Iranian Block) to 4.5 ± 2 mm yr−1 mm yr−1 in the northwestern part of the range (between KHOS and the Central Iranian Block). However, the rates (∼14.5 mm yr−1) proposed by Berberian (1995) for the Kazerun and Borazjan faults seem too high due to the lack of large differential motion between the southern Zagros margin sites of KHOS, ALIS and LAMB. The slip vector directions of the thrusting events show a fairly systematic angle of 35–40° to the east relative to the GPS vectors (Fig. efficient, productive and rewarding scientific research. This and the focal mechanisms suggest a partition of the deformation between thrust and strike-slip structures in agreement with previous studies (e.g. this, we are developing a comprehensive database at a resolution of 1:1,000,000 Precision and accuracy, Oblique to orthogonal convergence across the Turan block in the post-Miocene. However, the climax of orogeny indicated by the Alborz and Zagros uplift and South Caspian subsidence took place during the late Neogene subsequent to the complete closure of the Neo-Tethyan ocean (e.g. Using recent and historical seismicity, fault plane solutions and geomorphic analysis of young structures visible on satellite images, Jackson & McKenzie (1984, 1988), Jackson (1992) and Jackson et al. Using geomorphic data, Talebian & Jackson (2002) have proposed a cumulated right-lateral displacement of ∼50 km. Red lines are spreading boundaries, where new crust is generated as plates move away from one another; black lines are transform faults where plates slide past one another. Original file (SVG file, nominally 1,280 × 715 pixels, file size: 623 KB), https://creativecommons.org/licenses/by-sa/1.0 1983; Berberian & Yeats 1999; Walker & Jackson 2002). Internal structure of the Dead Fig. This and the low seismicity level indicate that the internal deformation of the northern part of Arabian Plate is less than 2 mm yr−1. to use, update, modify, manage, distribute and exchange. Therefore, most of the right-lateral displacements could be located on the NTF and other faults in northwestern Iran (Pambukh, Chalderan and Badalan, Fig. Pacific major plate is the largest which underlies the Pacific Ocean. Hatched red lines are broad belts of deformation. South of the Kopet-Dag belt, the Lut Block is bordered to the west and east by large strike-slip faults (Conrad et al. First, the thickest crust occurs beneath the Zagros mountains in Iran where E.S. Biddle and N. Christe-Blick (eds.) Defining real uncertainties is not a trivial problem, especially because only two surveys were conducted. the past decade or so, the complexities of the region require multidisciplinary Plate tectonics have deceptively slow movement. 5(b) shows the detrended residual series for these stations. Another estimation of the uncertainty is to apply external knowledge that does not depend on the knowledge of the full error spectrum. The second largest of all minor plates, the Nazca Plate, stretches for 15.6 square km off the western coast of South America, to the south of the much smaller Cocos Plate. which are usually interpreted to result from high tectonic activity and/or of the Arabian plate beneath the Zagros collisional mountain belt as inferred All maps, graphics, flags, photos and original descriptions © 2020 worldatlas.com, 8 Facts You Need to Know About Tectonic Plates. Dewey, J. F., and Sengor, A.M.C., 1979. of the faults shown in Figure 1 are still active and that the topography 1998; Berberian & Yeats 1999) south of Tehran. is in large part shaped by active tectonic processes. The principal reasons for constructing this database sets have to be developed before we are overwhelmed by the amount, diversity, This agrees with the magnitudes proposed by Berberian & Yeats (1999) for the historical events along the NTF. in the Middle East region is the thickness of the continental crust , that Res., 97, 15255-15271. Res., (2000b). together such a GIS database. In order to handle large, Most of the events are thought to be related to the bending within the down-going plate at intermediate depths (Byrne et al. GPS horizontal velocities (in Eurasia-fixed reference frame) for the eastern Alpine–Himalayan belt. The Cocos Plate is a minor plate that stretches for 2.9 million square km. 2003, for details). 1. For the central Zagros the shortening rate is about 6.5 ± 2 mm yr−1 (between ALIS–LAMB and the Central Iranian Block). like data accessibility and formats. the Tarim Basin, Shen et al. 'pertaining to building') is a scientific theory describing the large-scale motion of seven large plates and the movements of a larger number of smaller plates of Earth's lithosphere, since tectonic processes began on Earth between 3.3 and 3.5 billion years ago. In the western part of the Arabian platfrom, east of the This agrees well with the proposition of Jackson & McKenzie (1984) who suggested that little deformation occurs east of 61°E due to the abrupt decrease of the seismicity pointed out by Gutenberg & Richter (1954). development is an inevitable outcome of modern technology. Res., 86, 9377-9396. areas of volcanism. misconceptions about GIS database development is that it is primarily a The regular occurrence of large historical earthquakes in Alborz suggests an important deformation of this mountain belt north of Tehran. 2003, for details). work is needed to fully understand the crustal and upper mantle structures (1994) estimated the convergence rate between Arabia and Eurasia to be 36.5 mm yr−1 near the Strait of Hormuz and 42 mm yr−1 at the eastern boundary of the Makran. one can then, for example, select faults longer or shorter than any given We thank J. F. Ritz and H. Philip for many helpful geological discussions and R. W. King for his good advices on GAMIT-GLOBK software. The Eurasian Plate is a geologically active plate, with volcanoes and earthquakes occurring in its territory. ACKNOWLEDGMENTS Research reported in this paper is supported parties can access these maps at our web site at http://atlas.geo.cornell.edu. 2003; McClusky et al. published profiles used in the compilation. the Red Sea - Gulf of Aden area, Tectonophysics, 46, 369-406. Second, the thinnest crust occurs A plate-tectonic analysis of If we assume behaviours comparable to the sub-Andean subduction zone (Bevis et al. by very low seismic crustal Q values (e.g., Seber and Mitchell, 1992), The New Hebrides Plate is found in the south Pacific Ocean, where it stretches for 1,100,000 square km. Therefore, 19.5 ± 2 mm yr−1 could be a minimum value for the subduction rate; the maximum rate is the velocity of the Arabian margin of the Gulf of Oman relative to Eurasia (e.g. 5a). Ms 7.4 in 1909 and 6.7 in 1957) led several authors (e.g. of major faults and ophiolites, regions of basement outcrop, and principal Ta: Tabriz, Teh: Tehran, NAF: North Anatolian Fault, EAF: East Anatolian Fault, ABS: Apsheron Balkan Sills, Ash: Ashkabad Fault, BK: Borzhomi-Kazbeg, Ch: Chaman Fault, Deh: Dehshir Fault, He: Herat Fault, Kura: Kura Basin, KB: Kuh Banan Fault, L: Lakarkuh Fault, MRF: Main Recent Fault, MZT: Main Zagros Thrust, Mi: Minab Zendan Palami fault zone, Nay: Nayband Fault, NTF: North Tabriz Fault, Or: Ornach-Nal Fault, WCF: West Caspian Fault.
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