01. 2013年4月10日 13:12:00
: xEBOc6ttRg
付近と言っても大分離れているし、M6.3では。ほぼノーダメージなのも当然https://maps.google.co.jp/maps?hl=ja&q=iran+bushehr+nuclear+power+plant&bav=on.2,or.r_qf.&bvm=bv.44990110,d.dGI&biw=2133&bih=1203&um=1&ie=UTF-8&sa=N&tab=wl
https://maps.google.co.jp/maps?q=28.500%C2%B0N+51.591%C2%B0E http://earthquake.usgs.gov/earthquakes/world/index.php?regionID=13 http://earthquake.usgs.gov/earthquakes/eventpage/usb000g2y5#summary
Location 28.500°N 51.591°E depth=10.0km (6.2mi) Nearby Cities 89km (55mi) SE of Bandar Bushehr, Iran
92km (57mi) SSE of Borazjan, Iran
103km (64mi) WSW of Firuzabad, Iran
124km (77mi) S of Kazerun, Iran
272km (169mi) NNE of Manama, Bahrain
Related Links Additional earthquake information for Iran
Earthquake Summary Poster
View location in Google Maps Tectonic Summary The April 9, 2013 M6.3 earthquake in southern Iran occurred as result of northeast-southwest oriented thrust-type motion in the shallow crust of the Arabian plate. The depth and style of faulting in this event are consistent with shortening of the shallow Arabian crust within the Zagros Mountains in response to active convergence between the Arabian and Eurasian plates. Because this event is an intraplate event, occurring almost 300 km south of the main plate boundary, and since the event likely did not break the surface, precise identification of the causative fault is difficult at this time. On a broad scale, the seismotectonics of southern Iran are controlled by active convergence between the Arabian and Eurasian tectonic plates. This motion manifests in two ways: subduction in the Makran which stretches from the mouth of the Persian Gulf eastward into Pakistan, and continental collision in the Zagros Mountains, which stretch from the Makran northward into Iraq and Turkey. The April 9 event occurred within the Zagros fold-and-thrust belt - the portion of the Zagros Mountains that border the north shore of the Persian Gulf. At the latitude of the event, convergence rates between Arabia and Eurasia are approximately 30 mm/yr. The Zagros Mountains experience high rates of seismicity, with thrust-type events similar to the April 9 earthquake and right-lateral strike slip events common. Recent thrust-type events as large as M6 have occurred south of the April 9 epicentral area in the Bandar-e-Abbas region. Highly damaging events such as the 2003 M6.6 Bam earthquake occurred outside of the Zagros Mountains, north of the Makran subduction zone, 660 km to the east of the April 9 event. While the Zagros region experiences high rates of seismicity, large (>M7) surface rupturing earthquakes here are rare. Over the past 40 years, 5 events of M6 or greater have occurred with 300 km of the April 9 earthquake. The closest was an M6.1 right-lateral strike slip event on March 1, 1994, which killed approximately 50 people. Seismotectonics of the Middle East and Vicinity 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 Himalayan, Karakoram, 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 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 30 May 1935, M7.6 Quetta, Pakistan earthquake, occurred within the Sulaiman 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 Arabia 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 belt of the Zagros Mountains, which crosses the whole of western Iran and extends into northeastern Iraq. Collision of the Arabia and Eurasia plates also causes crustal shortening in the Alborz Mountains and Kopet Dag in northern Iran. Eastern Iran experiences destructive earthquakes that originate on both strike-slip and reverse faults. For example, the 16 September 1978 M7.8 earthquake, along the southwest edge of the Dasht-e-Lut Basin killed at least 15,000 people. Along the eastern margin of the Mediterranean region there is complex interaction between the 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 10mm/yr near its northern end, and 16mm/yr near its southern end (Chu, D. and Gordon, R. G., 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 25mm/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 westwards along the North Anatolia Fault system. The westernmost of these earthquakes was the 17th August 1999, M7.6 Izmit earthquake, near the Sea of Marmara, 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. |
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