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新疆于田发生Ms7.3级地震

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零度星系 发表于 2014-2-12 22:37 | 显示全部楼层 |阅读模式 来自: 中国–四川–南充 电信

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国家地震科学数据共享中心信息
发震日期
发震时刻
纬度(°)
经度(°)
深度(km)
震级
事件类型
参考地点
2014-02-1221:14:57.2
36.1
82.3
8
Ms3.2
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1220:26:41.5
36.2
82.9
6
Ms4.2
天然地震新疆维吾尔自治区和田地区民丰县
2014-02-1220:12:44.1
35.9
82.5
9
Ms3.2
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1219:31:01.8
36.0
82.5
6
Ms3.7
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1219:19:40.1
36.1
82.5
6
Ms3.0
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1219:14:20.6
36.2
82.5
8
Ms4.6
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1218:10:17.5
36.0
82.5
9
Ms3.4
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1218:04:58.3
36.1
82.5
6
Ms3.2
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1218:00:59.3
37.2
82.2
9
Ms3.1
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1218:00:07.6
36.0
82.5
6
Ms4.9
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:55:06.3
36.0
82.5
7
Ms3.4
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:41:49.8
36.1
82.5
6
Ms3.8
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:36:08.0
36.0
82.5
9
Ms4.2
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:33:04.9
37.0
82.2
12
Ms3.0
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:30:28.8
36.0
82.5
11
Ms3.4
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:29:44.6
35.9
82.4
8
Ms3.3
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:27:46.4
36.1
82.5
6
Ms3.7
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:26:43.6
36.1
82.5
4
Ms3.6
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:26:43.4
36.1
82.6
14
Ms4.2
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:26:03.0
36.1
82.5
9
Ms3.4
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:25:55.4
36.1
82.5
6
Ms3.6
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:24:43.4
36.0
82.5
5
Ms5.7
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:23:27.5
36.1
82.5
5
Ms4.1
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:22:20.7
36.1
82.5
5
Ms4.3
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1217:19:50.3
36.1
82.5
12
Ms7.3
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1122:28:40.9
33.6
89.4
5
Ms3.6
天然地震西藏自治区那曲地区尼玛县
2014-02-1120:33:47.9
36.1
82.5
7
Ms3.1
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1110:17:30.8
36.0
82.5
9
Ms3.7
天然地震新疆维吾尔自治区和田地区于田县
2014-02-1110:14:57.2
36.1
82.4
11
Ms5.4
天然地震新疆维吾尔自治区和田地区于田县


当前Kp指数估计值(三小时平均),当Kp指数达到6或以上时,我国境内有可能观察到极光;当前极光活动水平,极光为9时漠河可能见极光,
预计未来24小时地磁暴最强可达级,当地磁暴级别达到G2或以上时,我国境内有可能见极光
 楼主| 零度星系 发表于 2014-2-12 22:38 | 显示全部楼层 来自: 中国–四川–南充 电信

                               
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新疆维吾尔自治区和田地区于田县M7.3地震

地震参数时间: 2014-02-12 17:19:50.3
纬度: 36.1
经度: 82.5
深度: 12
震级: M7.3
震中位置: 新疆维吾尔自治区和田地区于田县
震中分布图
历史地震

3级以上历史地震
(10°×10°,据中国地震目录)

5级以上历史地震
(10°×10°,据中国地震目录)
M-T图

3级以上历史地震M-T图(10°×10°,据中国地震目录)

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 楼主| 零度星系 发表于 2014-2-12 22:55 | 显示全部楼层 来自: 中国–四川–南充 电信
ShakeMap:什么是ShakeMap?请参看http://en.wikipedia.org/wiki/ShakeMap


                               
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 楼主| 零度星系 发表于 2014-2-12 22:55 | 显示全部楼层 来自: 中国–四川–南充 电信
地震强地面运动的特征描述http://wenku.baidu.com/link?url=XWnRZVxHPf8ryFaS8ZAReDuIiJ_p7Kp7DDK5FOrHJHFO-3bwKRr_yo-efXNo0oFFQqv7i-z6ynhfcIKw04E-57wUIe19eMPpvH9Yep8TDDO

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法拉利ss 发表于 2014-2-12 23:03 | 显示全部楼层 来自: 中国–重庆–重庆 电信
太远了,我们不可能感受到震感。
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 楼主| 零度星系 发表于 2014-2-12 23:08 | 显示全部楼层 来自: 中国–四川–南充 电信
和田地区:麦加利地震烈度为4,人口数约114k。
4(IV)度
连室外的人也感觉到震动;家中较小的饰物开始摇晃,但不造成破坏。

喀什地区:麦加利地震烈度为3
3(III)度
大部分室内的人感觉到震动,很多人意识不到是地震。



                               
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file:///d:/360安~1/360se6/USERDA~1/Temp/exposure.png
file:///d:/360安~1/360se6/USERDA~1/Temp/exposure.png
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 楼主| 零度星系 发表于 2014-2-12 23:17 | 显示全部楼层 来自: 中国–四川–南充 电信
汶川地震ShakeMap

                               
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北极之星 发表于 2014-2-13 10:06 | 显示全部楼层 来自: 中国–山东–济宁 电信
12日7.3级地震算是余震吧?11日已经有震感了

点评

那不叫余震。这是前震——主震——余震型的序列。1975年辽宁海城M7.3、2003年新疆伽师M6.8地震都是这样的形态。  详情 回复 发表于 2014-2-13 15:13
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旅行者2号 发表于 2014-2-13 15:13 | 显示全部楼层 来自: 中国–辽宁–大连 联通
北极之星 发表于 2014-2-13 10:06
12日7.3级地震算是余震吧?11日已经有震感了

那不叫余震。这是前震——主震——余震型的序列。1975年辽宁海城M7.3、2003年新疆伽师M6.8地震都是这样的形态。

点评

多谢指点,这样的地震一般造成的危害相对小一点吧,如果有前震的话一般都采取避灾措施了……记得汶川地震就没有前震吧。  详情 回复 发表于 2014-2-13 18:17
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旅行者2号 发表于 2014-2-13 15:19 | 显示全部楼层 来自: 中国–辽宁–大连 联通
这个地震依然在维持近20年来国内7级大震的统计规律。大约自1995年以来,国内全部的7级以上浅源地震全部分布在松潘——甘孜块体的边界上,这里是最近国内强震最活跃的地区。丽江地震(记不清年份和震级了)、96年西藏尼玛M7.5、01年昆仑山M8.1、08年新疆于田M7.1、08年四川汶川M8.0、10年青海玉树M7.1、13年四川雅安M7.0以及这次于田M7.3,全部都在这里分布。甚至上推到1937年,青海花石峡M7.5也在这个块体的边界上分布。问题在于这个块体太大了,绵延上千公里的边界,下一次具体在哪一个点呢?
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BlackEyeGalaxy 发表于 2014-2-13 15:49 | 显示全部楼层 来自: 中国–上海–上海–徐汇区 电信
Tectonic Summary


The February 12, 2014 M 6.9 earthquake south of Hotan, China, occurred as a result of shallow strike-slip faulting in the tectonically complex region of the northern Tibetan Plateau. Preliminary mechanisms for the event indicate slip occurred on a steeply dipping fault, either a left-lateral structure oriented northeast-southwest, or a right-lateral structure oriented northwest-southeast. This earthquake occurred several hundred kilometers north of the convergent India-Eurasia plate boundary, where the India Plate is moving northwards with respect to Eurasia at a rate of approximately 46 mm/yr. This convergence drives the uplift of the Himalaya Mountains, at a rate of approximately 10 mm/yr, and the Tibetan Plateau, which is an extremely broad region of thickened and uplifted crust sitting 4.5-5.0 km above sea level.

The uplifted Tibetan Plateau is spreading to the east and, as a result, is an area of east-west extension and eastward crustal motion within a larger region of generally north-south convergence. This earthquake likely reflects the interplay amongst these major tectonic forces. The eastward motion of Tibet, with respect to Eurasia further north, is accommodated in part by the large intra-continental Altyn Tagh and Kunlun strike-slip fault systems. The February 12, 2014 earthquake most likely resulted from movement along the Altyn Tagh fault system or an adjacent structure. In 2008, a M 7.2 earthquake occurred approximately 120 km further west-southwest of the February 12, 2014 event. The 2008 earthquake resulted in moderate damage to buildings in the region.

Seismotectonics of the Himalaya and Vicinity

Seismicity in the Himalaya dominantly results from the continental collision of the India and Eurasia plates, which are converging at a relative rate of 40-50 mm/yr. Northward underthrusting of India beneath Eurasia generates numerous earthquakes and consequently makes this area one of the most seismically hazardous regions on Earth. The surface expression of the plate boundary is marked by the foothills of the north-south trending Sulaiman Range in the west, the Indo-Burmese Arc in the east and the east-west trending Himalaya Front in the north of India.

The India-Eurasia plate boundary is a diffuse boundary, which in the region near the north of India, lies within the limits of the Indus-Tsangpo (also called the Yarlung-Zangbo) Suture to the north and the Main Frontal Thrust to the south. The Indus-Tsangpo Suture Zone is located roughly 200 km north of the Himalaya Front and is defined by an exposed ophiolite chain along its southern margin. The narrow (<200km) Himalaya Front includes numerous east-west trending, parallel structures. This region has the highest rates of seismicity and largest earthquakes in the Himalaya region, caused mainly by movement on thrust faults. Examples of significant earthquakes, in this densely populated region, caused by reverse slip movement include the 1934 M8.1 Bihar, the 1905 M7.5 Kangra and the 2005 M7.6 Kashmir earthquakes. The latter two resulted in the highest death tolls for Himalaya earthquakes seen to date, together killing over 100,000 people and leaving millions homeless. The largest instrumentally recorded Himalaya earthquake occurred on 15th August 1950 in Assam, eastern India. This M8.6 right-lateral, strike-slip, earthquake was widely felt over a broad area of central Asia, causing extensive damage to villages in the epicentral region.

The Tibetan Plateau is situated north of the Himalaya, stretching approximately 1000km north-south and 2500km east-west, and is geologically and tectonically complex with several sutures which are hundreds of kilometer-long and generally trend east-west. The Tibetan Plateau is cut by a number of large (>1000km) east-west trending, left-lateral, strike-slip faults, including the long Kunlun, Haiyuan, and the Altyn Tagh. Right-lateral, strike-slip faults (comparable in size to the left-lateral faults), in this region include the Karakorum, Red River, and Sagaing. Secondary north-south trending normal faults also cut the Tibetan Plateau. Thrust faults are found towards the north and south of the Tibetan Plateau. Collectively, these faults accommodate crustal shortening associated with the ongoing collision of the India and Eurasia plates, with thrust faults accommodating north south compression, and normal and strike-slip accommodating east-west extension.

Along the western margin of the Tibetan Plateau, in the vicinity of south-eastern 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 active, left-lateral, strike-slip Chaman fault is the fastest moving fault in the region. In 1505, a segment of the Chaman fault near Kabul, Afghanistan, ruptured causing widespread destruction. In the same region the more recent 30 May 1935, M7.6 Quetta earthquake, which occurred in the Sulaiman Range in Pakistan, killed between 30,000 and 60,000 people.

On the north-western side of the Tibetan Plateau, beneath the Pamir-Hindu Kush Mountains of northern Afghanistan, earthquakes occur at depths as great as 200 km as a result of remnant lithospheric subduction. The curved arc of deep earthquakes found in the Hindu Kush Pamir region indicates the presence of a lithospheric body at depth, thought to be remnants of a subducting slab. Cross-sections through the Hindu Kush region suggest a near vertical northerly-dipping subducting slab, whereas cross-sections through the nearby Pamir region to the east indicate a much shallower dipping, southerly subducting slab. Some models suggest the presence of two subduction zones; with the Indian plate being subducted beneath the Hindu Kush region and the Eurasian plate being subducted beneath the Pamir region. However, other models suggest that just one of the two plates is being subducted and that the slab has become contorted and overturned in places.

Shallow crustal earthquakes also occur in this region near the Main Pamir Thrust and other active Quaternary faults. The Main Pamir Thrust, north of the Pamir Mountains, is an active shortening structure. The northern portion of the Main Pamir Thrust produces many shallow earthquakes, whereas its western and eastern borders display a combination of thrust and strike-slip mechanisms. On the 18 February 1911, the M7.4 Sarez earthquake ruptured in the Central Pamir Mountains, killing numerous people and triggering a landside, which blocked the Murghab River.

Further north, the Tian Shan is a seismically active intra-continental mountain belt, which extends 2500 km in an ENE-WNW orientation north of the Tarim Basin. This belt is defined by numerous east-west trending thrust faults, creating a compressional basin and range landscape. It is generally thought that regional stresses associated with the collision of the India and Eurasia plates are responsible for faulting in the region. The region has had three major earthquakes (>M7.6) at the start of the 20th Century, including the 1902 Atushi earthquake, which killed an estimated 5,000 people. The range is cut through in the west by the 700-km-long, northwest-southeast striking, Talas-Ferghana active right-lateral, strike-slip fault system. Though the system has produced no major earthquakes in the last 250 years, paleo-seismic studies indicate that it has the potential to produce M7.0+ earthquakes and it is thought to represent a significant hazard.

The northern portion of the Tibetan Plateau itself is largely dominated by the motion on three large left-lateral, strike-slip fault systems; the Altyn Tagh, Kunlun and Haiyuan. The Altyn Tagh fault is the longest of these strike slip faults and it is thought to accommodate a significant portion of plate convergence. However, this system has not experienced significant historical earthquakes, though paleoseismic studies show evidence of prehistoric M7.0-8.0 events. Thrust faults link with the Altyn Tagh at its eastern and western termini. The Kunlun Fault, south of the Altyn Tagh, is seismically active, producing large earthquakes such as the 8th November 1997, M7.6 Manyi earthquake and the 14th November 2001, M7.8 Kokoxili earthquake. The Haiyuan Fault, in the far north-east, generated the 16 December 1920, M7.8 earthquake that killed approximately 200,000 people and the 22 May 1927 M7.6 earthquake that killed 40,912.

The Longmen Shan thrust belt, along the eastern margin of the Tibetan Plateau, is an important structural feature and forms a transitional zone between the complexly deformed Songpan-Garze Fold Belt and the relatively undeformed Sichuan Basin. On 12 May 2008, the thrust belt produced the reverse slip, M7.9 Wenchuan earthquake, killing over 87,000 people and causing billions of US dollars in damages and landslides which dammed several rivers and lakes.

Southeast of the Tibetan Plateau are the right-lateral, strike-slip Red River and the left-lateral, strike-slip Xiangshuihe-Xiaojiang fault systems. The Red River Fault experienced large scale, left-lateral ductile shear during the Tertiary period before changing to its present day right-lateral slip rate of approximately 5 mm/yr. This fault has produced several earthquakes >M6.0 including the 4 January 1970, M7.5 earthquake in Tonghai which killed over 10,000 people. Since the start of the 20th century, the Xiangshuihe-Xiaojiang Fault system has generated several M7.0+ earthquakes including the M7.5 Luhuo earthquake which ruptured on the 22 April 1973. Some studies suggest that due to the high slip rate on this fault, future large earthquakes are highly possible along the 65km stretch between Daofu and Qianning and the 135km stretch that runs through Kangding.

Shallow earthquakes within the Indo-Burmese Arc, predominantly occur on a combination of strike-slip and reverse faults, including the Sagaing, Kabaw and Dauki faults. Between 1930 and 1956, six M7.0+ earthquakes occurred near the right-lateral Sagaing Fault, resulting in severe damage in Myanmar including the generation of landslides, liquefaction and the loss of 610 lives. Deep earthquakes (200km) have also been known to occur in this region, these are thought to be due to the subduction of the eastwards dipping, India plate, though whether subduction is currently active is debated. Within the pre-instrumental period, the large Shillong earthquake occurred on the 12 June 1897, causing widespread destruction.
我贴下美国地址勘探局的分析,他们测定矩震级是6.9级。
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旅行者2号 发表于 2014-2-13 16:35 | 显示全部楼层 来自: 中国–辽宁–大连 联通
USGS最初给定的震级时6.8,后来修正到6.9。不过貌似国内的台站测定的单台结果都是7+。这也正常,彼此的起算函数、台网形态、震中距都会影响计算结果。这次地震也结束了全球近3个月的7级平静,而全年平均全球会有18次7+的地震。
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北极之星 发表于 2014-2-13 18:17 | 显示全部楼层 来自: 中国–山东–济宁 电信
旅行者2号 发表于 2014-2-13 15:13
那不叫余震。这是前震——主震——余震型的序列。1975年辽宁海城M7.3、2003年新疆伽师M6.8地震都是这样的 ...

多谢指点,这样的地震一般造成的危害相对小一点吧,如果有前震的话一般都采取避灾措施了……记得汶川地震就没有前震吧。
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旅行者2号 发表于 2014-2-13 19:03 | 显示全部楼层 来自: 中国–辽宁–大连 联通
造成震害的因素有很多,例如房屋的质量、震中距、震源深度、震级大小、甚至震源破裂的方式也会影响震害的轻重。但如果有前震,也很难采取措施。问题在于,当刚刚发生一次地震的时候,如何判断这是前震还是主震?后续如何发展?如果有活动增强的趋势,主震会在什么具体时间发生?不用多,临震预报能精确到2、3天都极为难得了,而实际情况是,大众不可能天天住帐篷,工厂停产一天的损失同样惊人。
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BlackEyeGalaxy 发表于 2014-2-22 15:10 | 显示全部楼层 来自: 中国–上海–上海–徐汇区 电信
巴颜喀拉地块活动的活跃期有望结束。
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旅行者2号 发表于 2014-2-23 11:17 | 显示全部楼层 来自: 中国–辽宁–大连 联通
我的硕士论文就差点写关于巴颜喀拉地块的问题。
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