N a X c I v a n ( a z e r. )
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S N A X C I V A N ( A Z E R . ) G u l f o f S u e z G u l f o f A q a b a S t r a i t o f H o r m u z G u l f o f K u t c h T h e S w a t c h Cy cla de s DO DE CA NE SE Rhodes R U S S I A S u l a i m a n R a n g e Hi nd u Ku sh Z a g r o s M o u n t a i n s K ope t Da g Da sht -e-L ut Ba sin Alb orz Mount ains T ia n S h an P am ir G r e a t e r C a u c a s u s Delhi
Cairo Tehran
Bombay Karachi
Istanbul Pune
Giza Baku
Kabul Jeddah
Riyadh Jaipur
Kuwait Lahore
Aleppo Ankara
Almaty Baghdad
Mashhad Smyrana
Yerevan Tashkent
T'Bilisi Ahmadabad Alexandria Faisalabad Mecca Ahvaz
Amman Konya
Bursa Shiraz
Seyhan Aintab
Tabriz Esfahan
Bishkek Amritsar
Peshawar Srinagar
Dushanbe Al Basrah Al Mawsil Rawalpindi Kermanshah
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T U R K E Y S Y R I A G E O R G I A A R M E N I A A Z E R B A I J A N I R A Q J O R D A N E G Y P T S U D A N S A U D I A R A B I A U . A . E . K U W A I T Q A T A R B A H R A I N O M A N I R A N A F G H A N I S T A N T U R K M E N I S T A N U Z B E K I S T A N K A Z A K H S T A N C H I N A K Y R G Y Z S T A N T A J I K I S T A N I N D I A P A K I S T A N L E B A N O N I S R A E L C Y P R U S A N A T O L I A B L O C K A R A B I A P L A T E A F R I C A P L A T E E U R A S I A P L A T E I N D I A P L A T E B l a c k S e a a e S n a e g e A S ea o f C rete Sea of Mar mara M e d i t e r r a n e a n S e a Red Sea P e r s i a n G u l f Ca spi an S e a Aarabogazkol Basin Aral Sea Ysk Köl Lake G u lf o f O ma n I N D I A N O C E A N Gulf of Kumbhat RED SEA RIFT DEAD SEA TRANSFO RM N O R TH A N A TO L I A N FA UL T E A S T A N A T O L I A N F A U L T CYPRIAN ARC M A KRAN TRENCH C H AM AN FAUL T ALTYN TAGH FAULT KA RAK OR AM FAUL T TALA S FERGHANA FAUL T M AI N PA MI R T HRUS T e g n a R r a ht ri K Hyderabad 4 4 4 2 °
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Kuwait Riyadh
Jeddah Giza
Alexandria Damascus
Aleppo Smyrana
Ankara Baghdad
T’Bilisi Baku
Yerevan Tehran
Mashhad Kabul
Tashkent Faisalabad Lahore Ahmadabad Karachi Delhi
Jaipur Bombay
Pune Istanbul
ANATOLIA BLOCK ARABIA PLATE AFRICA PLATE EURASIA PLATE INDIA PLATE Damascus
GREECE Arabian Sea Quetta
U.S. Department of the Interior U.S. Geological Survey Seismicity of the Earth 1900–2010 Middle East and Vicinity Compiled by Jennifer Jenkins, 1 Bethan Turner, 1 Rebecca Turner, 1 Gavin P. Hayes, 2 Alison Sinclair, 1 Sian Davies, 1 Amy Parker, 1 Richard L. Dart, 2 Arthur C. Tarr, 2 Antonio Villaseñor, 3 and Harley M. Benz 2 2013 1 Department of Earth and Ocean Sciences, University of Liverpool, Liverpool, United Kingdom 2 U.S. Geological Survey 3 Institute of Earth Sciences, CSIC, Barcelona, Spain Open-File Report 2010–1083–K Version 1.1, revised January 28, 2014 TECTONIC SUMMARY No fewer than four major tectonic plates (Arabia, Eurasia, India, and Africa) and one smaller tectonic block (Anatolia) are responsible for seismicity and tectonics in the Middle East and surrounding region. Geologic development of the region is a consequence of a number of first-order plate tectonic processes that include subduction, large-scale transform faulting, compressional mountain building, and crustal extension. Mountain building in northern Pakistan and Afghanistan is the result of compressional tectonics, associated with collision of the India plate moving northwards at a rate of 40 mm/yr with respect to the Eurasia plate. Continental thickening of the northern and western edge of the India subcontinent has produced the highest mountains in the world, including the Himalaya, Karakorum, Pamir and Hindu Kush ranges. Earthquake activity and faulting found in this region, as well as adjacent parts of Afghanistan and India, are due to collisional plate tectonics. Beneath the Pamir‒Hindu Kush Mountains of northern Afghanistan, earthquakes occur to depths as great as 200 km as a result of remnant lithospheric subduction. Shallower crustal earthquakes in the Pamir‒Hindu Kush Mountains occur primarily along the Main Pamir Thrust and other active Quaternary faults, which accommodate much of the region’s crustal shortening. The western and eastern margins of the Main Pamir Thrust display a combination of thrust and strike-slip mechanisms. Along the western margin of the Tibetan Plateau, in the vicinity of southeastern Afghanistan and western Pakistan, the India plate translates obliquely relative to the Eurasia plate, resulting in a complex fold-and-thrust belt known as the Sulaiman Range. Faulting in this region includes strike-slip, reverse-slip and oblique-slip motion and often results in shallow, destructive earthquakes. The relatively fast moving left-lateral, strike-slip Chaman Fault system in southeastern Afghanistan accommodates translational motion between the India and Eurasia plates. In 1505, a segment of the Chaman Fault system near Kabul, Afghanistan, ruptured causing widespread destruction of Kabul and surrounding villages. In the same region, the more recent May 30, 1935, M7.6 Quetta, Pakistan, earthquake occurred within the Kirthar range, killing between 30,000 and 60,000 people. Off the south coast of Pakistan and southeast coast of Iran, the Makran trench is the present- day surface expression of active subduction of the Arabia plate beneath the continental Eurasia plate, which converge at a rate of approximately 20 mm/yr. Although the Makran subduction zone has a relatively slow convergence rate, it has produced large devastating earthquakes and tsunamis. For example, the November 27, 1945, M8.0 mega-thrust earthquake produced a tsunami within the Gulf of Oman and Arabian Sea, killing over 4,000 people. Northwest of this active subduction zone, collision of the Arabia and Eurasia plates forms the approximately 1,500-km-long fold and thrust belts of the Zagros Mountains, which crosses the whole of western Iran and extends into northeast- ern Iraq. Collision of the Arabia and Eurasia plates also causes crustal shortening in the Alborz Mountains and Kopet Dag in Northern Iran. Eastern Iran undergoes destructive earthquakes that originate on both strike-slip and reverse faults. For example, the September 16, 1978, M7.4 earthquake, along the northwest edge of the Dasht-e-Lut Basin, killed at least 15,000 people. Though smaller, the M6.5 December 26, 2008, Bam earthquake, near the southwestern edge of the Dasht-e-Lut Basin, resulted in over 25,000 deaths. Along the eastern margin of the Mediterranean region there is complex interaction among Africa, Arabia, and Eurasia plates. The Red Sea Rift is a spreading center between the Africa and Arabia plates, with a spreading rate of approximately 10 mm/yr near its northern end, and 16 mm/yr near its southern end (Chu and Gordon, 1998). Seismicity rate and size of earthquakes has been relatively small along the spreading center, but the rifting process has produced a series of volcanic systems across western Saudi Arabia. Further north, the Red Sea Rift terminates at the southern boundary of the Dead Sea Transform Fault. The Dead Sea Transform is a strike-slip fault that accommodates differential motion between the Africa and Arabia plates. Though both the Africa plate, to the west, and the Arabia plate, to the east, are moving in a NNE direction, the Arabia plate is moving slightly faster, resulting in the left-lateral, strike-slip motion along this segment of the plate boundary. Historically, earthquake activity along the Dead Sea Transform has been a significant hazard in the densely populated Levant region (eastern Mediterranean). For example, the November 1759 Near East earthquake is thought to have killed somewhere between 2,000‒20,000 people. The northern termination of the Dead Sea Transform occurs within a complex tectonic region of southeast Turkey, where interaction of the Africa and Arabia plates and the Anatolia block occurs. This involves translational motion of the Anatolia block westwards, with a speed of approximately 25 mm/yr with respect to Eurasia, in order to accommodate closure of the Mediterranean Basin. The right-lateral, strike-slip North Anatolia Fault, in northern Turkey, accommodates much of the westwards motion between the Anatolia block and Eurasia plate. Between 1939 and 1999, a series of devastating M7.0+ strike-slip earthquakes propagated westward along the North Anatolia Fault system. The westernmost of these earthquakes was the August 17, 1999, M7.6 Izmit earthquake, near the Sea of Marmara, which killed approximately 17,000 people. At the southern edge of the Anatolia block lies the east-west trending Cyprian Arc with associated levels of moderate seismicity. The Cyprian Arc represents the convergent boundary between the Anatolia block to the north and the Africa plate to the south. The boundary is thought to join the East Anatolia Fault zone in eastern Turkey; however, no certain geometry or sense of relative motion along the entire boundary is widely accepted. DATA SOURCES The earthquake locations shown on the main map (left) are taken from the global 1900‒2007 Centennial Catalog (Engdahl and Villaseñor, 2002), a catalog of high-quality depth determinations for the period 1964‒2002 (Engdahl, personal commun., 2003), and U. S. Geological Survey- Preliminary Determination of Epicenters (USGS-PDE, http://earthquake.usgs.gov/research/data/pde.php) for the years 2008‒2010. Major earthquakes (7.5≤M≤8.2) are labeled with the year of occurrence, while earthquakes (8.0≤M≤8.2) are labeled with the year of occurrence and also denoted by a white outline (Tarr and others, 2010). The Seismic Hazard and Relative Plate Motion figure (lower left) shows the generalized seismic hazard (Giardini and others, 1999) and relative plate motion vectors (open arrows with labels) using the Morvel model (DeMets and others, 1994). Base map data sources include GEBCO 2008 shaded relief, Volcanoes of the World dataset (Siebert and Simkin, 2002); plate boundaries (Bird, 2003); and geographic information from Digital Chart of the World (1992), and ESRI (2002).
Bird, Peter, 2003, An updated digital model of plate boundaries: Geochemistry Geophysics Geosystems, v. 4, no. 3, 52 p. Chu, D., Gordon, R.G., 1998, Current plate motions across the Red Sea: Geophysical Journal International, v. 135, is. 2, p. 313‒328. Daëron, M., Klinger, Y., Tapponnier, P., Elias, A., Jacques, E., and Sursock, A., 2005, Sources of the large A.D. 1202 and 1759 Near East earthquakes: Geology, v. 35, p. 755‒758, doi:10.1130/G23631A.1. DeMets, Charles, Gordon, R.G., Argus, D.F., and Stein, Seth, 1994, Effect of recent revisions to the geomagnetic time scale on estimates of current plate motions: Geophysical Research letters, v. 21, p. 2191‒2194. Digital Chart of the World, 1992: Accessed on Mar. 9, 1996 at
Engdahl, E.R., and Villaseñor, Antonio, 2002, Global seismicity 1900‒1999, in Lee, . W.H.K., Kanamori, Hiroo, Jennings, P.C., and Kisslinger, Carl, eds., International Handbook of Earthquake and Engineering Seismology, v. 81(A), chap. 41, p. 1‒26. ESRI, 2002, ESRI data and maps: Redlands, Calif., ESRI. Available at
GEBCO, 2008, The GEBCO_08_Grid, ver. 20091120: GEBCO. Accessed Jan. 8, 2010 at http://www.gebco.net. Giardini, D., Grunthal, G., Shedlock, K., Zhang. P., and Global Seismic Hazards Program, 1999, Global seismic hazards map: Accessed on Jan. 9, 2007 at http://www.seismo.ethz.ch/GSHAP. National Oceanic and Atmospheric Administration (NOAA), 2010: National Geophysical data Center (NGDC): National Oceanic and Atmospheric Administration, Accessed on Mar. 31, 2010 at
Siebert, Lee, and Simkin, Thomas, 2002, Volcanoes of the world—An illustrated catalog of Holocene volcanoes and their eruptions: Smithsonian Institution, Global Volcanism Program Digital Information Series, GVP-3. Accessed on Jan. 9, 2007 at http://www.volcano.si.edu/world. Tarr, A.C., Villaseñor, Antonio, Furlong, K.P., Rhea, Susan, and Benz, H.M., 2010, Seismicity of the Earth 1900‒2007: U.S. Geological Survey Scientific Investigations Map 3064, scale 1:25,000,000. Available at http://pubs.usgs.gov/sim/3064. 8.2
4–5.9 6–6.4
6.5–6.9 7–7.4
7.5 7.6
7.7 7.8
7.9 8.0
8.1 Active volcanoes Country Boundary
0–69 km 70–299 km 300–700 km Others
Subduction Transform Divergent Large Active Fault
0 200 400 600
800 100
KILOMETERS Scale 1: 7 000 000 0 300
600 900
1200 Scale 1: 28 300 000 KILOMETERS Country
Boundary Large Active Fault Subduction Transform Divergent Others 0– 0.2 m/s² 0.2– 0.4 0.4– 0.8
0.8– 1.6 1.6– 3.2
3.2– 6.4 6.4– 9.8
Relative plate motion in mm/yr 4 3 FIGURE EXPLANATION Peak ground acceleration Plate boundaries This and other USGS information products are available at http://store.usgs.gov/. U.S. Geological Survey Box 25286, Denver Federal Center Denver, CO 80225 To learn about the USGS and its information products visit
1-888-ASK-USGS This report is available at:
For more information concerning this publication, contact: Center Director, USGS Geologic Hazards Science Center Box 25046, Mail Stop 966 Denver, CO 80225 (303) 273-8579 Or visit Geologic Hazards Science Center Web site at:
Publishing support provided by: Denver Publishing Service Center Manuscript approved for publication January 4, 2013 Any use of trade, product or firm names is for descriptive purposes only and does not imply endorsement by the U.S. Government. Although this information product, for the most part, is in the public domain, it also contains copyrighted materials as noted in the text. Permission to reproduce copyrighted items for other than personal use must be secured from the copyright owner. Suggested citation: Jenkins, Jennifer, Turner, Bethan, Turner, Rebecca, Hayes, G.P., Sinclair, Alison, Davies, Sian, Parker, Amy, Dart, R.L., Tarr, A.C., Villaseñor, Antonio, and Benz, H.M., compilers, 2013, Seismicity of the Earth 1900–2010 Middle East and vicinity (ver. 1.1, Jan. 28, 2014): U.S. Geological Survey Open-File Report 2010–1083–K, scale 1:7,000,000, http://pubs.usgs.gov/of/2010/1083/k/. Albers Equal Area Conic Projection Digital Map database and cartography by Arthur C.Tarr and Susan Rhea Seismic Hazard and Relative Plate Motion Download 126.81 Kb. Do'stlaringiz bilan baham: 
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