Tectonics and Aftershocks of the Mw=8.8 2010 Chile earthquake rupture area from Oceanbottom Seismometer data

小组提案的总体目标已在摘要文件中作了说明。破坏性俯冲带地震，如Mw=8.8 27。2010年2月智利地震，是由俯冲巨型逆冲断层突然滑动引起的。一旦局部成核，破裂就会在地震中传播和扩展。然而，在所谓的同震破裂上倾极限处，破裂一般会阻止海沟轴线向陆地方向数十公里的海前弧下。向海上升界限的位置对于确定地震引发的海啸的大小至关重要。余震可以用来确定上升极限的位置。然而，全球目录中报告的事件一般都有几十公里量级的很大不确定性。在这里，我们将使用密集的海底地震仪网络数据，这些数据记录了2010年2月智利8.8级大地震的三个月余震序列。数据将被用来定义控制上倾角极限的过程的地理位置和性质。此外，我们还将研究同震破裂带上倾角和下倾角俯冲推力和俯冲板块之间的应力变化和应力传递。

The overarching aims of the group proposal have been described in the summary document. Destructive subduction zone earthquakes, like the Mw=8.8 27. February 2010 Chile earthquake, are caused by sudden slippage of the subduction megathrust fault. Once nucleation occurs locally, rupture can propagate and expand in an earthquake. However, rupture generally stops several tens of kilometers landward of the trench axis below the marine fore-arc at the so called updip limit of coseismic rupture. The location of the seaward updip limit is critical for defining the size of a tsunami generated by the earthquake. Aftershocks can be used defining the location of the updip limit. However, events reported in global catalogues have generally large uncertainties in the order of several tens of kilometres. Here, we will use data from a dense network of ocean bottom seismometers data that recorded for three month the aftershock sequence of the Great Mw=8.8 Chile earthquake of February 2010. Data will be used to define the geographical location and nature of the processes controlling the updip limit. Further, we will study stress changes and stress transfer between the subduction thrust and the subducting plate both updip and down-dip of the co-seismic rupture zone.