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Source rupture process, directivity and and Coulomb stress change of the 12 January 2010 (Port-au-Prince Haiti, Mw7.0) earthquake

机译：2010年1月12日（太子港海地，Mw7.0）地震的震源破裂过程，方向性和库仑应力变化

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摘要

The Haiti earthquake occurred on Tuesday, January 12, 2010 at 21:53:10 UTC. Its epi- center was at 18.46 degrees North, 72.53 degrees West, about 25 km WSW of Haiti’s capital, Port-au-Prince, along the tectonic boundary between Caribbean and North America plate dominated by left-lateral stri- ke slip motion and compression with 2 cm/yr of slip velocity eastward with respect to the North America plate. The earthquake was relatively shallow (about 13 km depth) with Mw 7.0 and CMT mechanism solution indica- ting left-lateral strike slip movement with a fault plane oriented toward the WNW-ESE. More than 10 aftershocks ranging from 5.0 to 5.9 in magnitude struck the area in hours following the main shock. Most of these af- tershocks have occurred to the west of the mainshock in the Mirogoane Lakes region and its distribution suggests that the length of the rupture was around 70 km. Rupture velocity and direction was constrained by using the directivity effect determined from broad-band waveforms recorded at regio- nal and teleseismic distances using DIRDOP computational code (DIRectivity DOPpler effect) [1]. The Results show that the rup- ture spread mainly from WNW to ESE with a velocity of 2.5 km/s. In order to obtain the spatiotemporal slip distribution of a fi- nite rupture model we have used teleseismic body wave and the Kikuchi and Kanamori’s method [2]. The inversion show complex source time function with a total scalar seismic moment of 2.2 x 1019Nm (Mw=6.9) a source duration of about 18 sec with a main energy relesea in the first 13 sec. Finally, we compared a map of aftershocks with the Coulomb stress changes caused by the main shock in the region [3]. [1] Kikuchi, M., and Kanamori, H., 1982, Inversion of com- plex body waves: Bull. Seismol. Soc. Am., v. 72, p. 491-506. [2] Caldeira B., Bezzeghoud M, Borges JF, 2009; DIRDOP: a directivity ap- proach to determining the seismic rupture velocity vector. J Seismology, DOI 10.1007/ s10950-009-9183-x [3] King, G. C. P., Stein, R. S. y Lin, J, 1994, Static stress changes and the triggering of earthquakes. Bull. Seismol. Soc. Am. 84,935-953. More than 10 aftershocks ranging from 5.0 to 5.9 in magnitude struck the area in hours following the main shock. Most of these aftershocks have occurred to the west of the mainshock in the Mirogoane Lakes region and its distribution suggests that the length of the rupture was around 70 km.In order to obtain the spatiotemporal slip distribution of a finite rupture model we have used teleseismic body wave and the Kikuchi and Kanamori's method [1]. Rupture velocity was constrained by using the directivity effect determined from waveforms recorded at regional and teleseismic distances [2]. The spatiotemporal slip estimated points to a unilateral rupture that propagates from WNW to ESE with a rupture velocity of 2.5 km/s. Finally, we compared a map of aftershocks with the Coulomb stress changes caused by the event in the region [3]. [1]- Kikuchi, M., and Kanamori, H., 1982, Inversion of complex body waves: Bull. Seismol. Soc. Am., v. 72, p. 491-506.[2] Caldeira B., Bezzeghoud M, Borges JF, 2009; DIRDOP: a directivity approach to determining the seismic rupture velocity vector. J Seismology, DOI 10.1007/s10950-009-9183-x[3] -King, G. C. P., Stein, R. S. y Lin, J, 1994, Static stress changes and the triggering of earthquakes. Bull. Seismol. Soc. Am. 84,935-953.
机译：海地地震发生在2010年1月12日星期二世界标准时间（UTC）。其震中点位于海地首府太子港西南约25公里的北纬18.46度，西经72.53度，沿加勒比海和北美板块之间的构造边界，其左旋走向滑动和挤压作用占主导地位相对于北美板块向东滑动速度为2 cm / yr。地震相对较浅（约13 km深），Mw 7.0级地震和CMT机制解表明左走向走滑运动，断层面向WNW-ESE。在主震发生后数小时内，发生了10次余震，震级范围从5.0到5.9。大多数的震后都发生在Mirogoane Lakes地区主震的西侧，其分布表明破裂的长度约为70 km。使用DIRDOP计算代码从方向和远震距离记录的宽带波形确定的方向性效应来限制破裂速度和方向[1]。结果表明，破裂主要从西北欧向ESE传播，速度为2.5 km / s。为了获得有限破裂模型的时空滑动分布，我们使用了远震体波以及菊池和金森的方法[2]。反演显示了复杂的源时间函数，总标量地震矩为2.2 x 1019Nm（Mw = 6.9），源持续时间约为18秒，前13秒主要能量释放。最后，我们将余震图与该地区主震引起的库仑应力变化进行了比较[3]。 [1] Kikuchi，M.和Kanamori，H.，1982，复杂体波反演：Bull。地震Soc。诉72页，第72页。 491-506。 [2] Caldeira B.，Bezzeghoud M，博尔赫斯·JF，2009年； DIRDOP：一种确定地震破裂速度矢量的方向性方法。 J地震学，DOI 10.1007 / s10950-009-9183-x [3] King，G. C. P.，Stein，R. S. y Lin，J，1994，静应力变化和地震触发。公牛。地震Soc。上午。 84,935-953。在主震发生后数小时内，发生了10次余震，震级范围从5.0到5.9。这些余震大多发生在米罗戈恩湖地区主震的西部，其分布表明破裂的长度约为70 km。为了获得有限破裂模型的时空滑动分布，我们使用了远震体波和菊池和金森的方法[1]。通过使用在区域和远震距离记录的波形确定的方向性效应来限制破裂速度[2]。估计的时空滑移指向从WNW传播到ESE的单侧破裂，破裂速度为2.5 km / s。最后，我们将余震图与该地区事件引起的库仑应力变化进行了比较[3]。 [1]-Kikuchi，M。和Kanamori，H.，1982，复杂体波反演：Bull。地震Soc。诉72页，第72页。 491-506。[2] Caldeira B.，Bezzeghoud M，Borges JF，2009； DIRDOP：一种确定地震破裂速度矢量的方向性方法。 J地震学，DOI 10.1007 / s10950-009-9183-x [3]-King，G. C. P.，Stein，R.S. y Lin，J，1994，静应力变化和地震触发。公牛。地震Soc。上午。 84,935-953。

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