2017年四川九寨沟M_s7.0地震的地震学特征
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摘要
2017年九寨沟M_s7.0地震位于巴颜喀喇地块东边界带附近的虎牙断裂NNW方向的延长线上,震源深度20km,震源机制解为左旋走滑型,矩震级为M_w6.5.震后6 d内共记录到3000多次余震,最大震级为M4.8,余震活动强度偏低但衰减正常.主震位于余震区中部,为双侧破裂.余震区呈NNW向线性分布,断层面近乎直立,长度超过30 km,破裂宽度约15 km.余震区中部、东南部余震的震源机制大多与主震震源机制一致,而西北部余震的震源机制均为逆冲型,可能与岷江断裂有关.余震区中部、东南部的应力也较西北部释放充分.九寨沟地震最大烈度为9度,记录的峰值加速度值NS向最大,EW向次之,垂直向最小,最近的强震台是九寨百河台,其加速度反应谱低于九寨沟地区的8度设防烈度.静态库仑应力研究表明,汶川地震对九寨沟地震具有较明显的触发作用.沿虎牙断裂发生的1973年松潘东北M_s6.5地震,1976年松潘M_s7.2地震和本次九寨沟地震的余震区沿NNW方向相连.结合主震破裂位移分布、余震的震源机制及应力降分析认为,九寨沟地震余震区中部、东南部发生强余震的危险性不大,但需注意余震区西北部及岷江断裂地震活动的发展.
The M_s7.0 Jiuzhaigou earthquake with the hypocenter depth of 20 km occurred at the NNW extension line of the Huya fault located next to the eastern boundary of the Bayan Har block. The focal mechanism solution of the mainshock based on the W-phase source inversion showed a sinistral slip and the moment magnitude was M_w6.5. Over 3000 aftershocks were recorded within six days, among which the largest was M4.8 and three others were larger than M4.0. The value of the aftershock frequency attenuation coefficient P was 1.03, and the b value of the magnitude-frequency relationship was 0.68. The aftershock activities were relatively inactive but the attenuation was normal. Relocation results of 603 aftershocks were obtained by using the double-difference earthquake location algorithm and the location errors of the EW, NS and the vertical directions were 0.81, 0.84 and 1.59 km respectively. The mainshock occurred in the center of the aftershock region and ruptured on both sides along the strike direction. The aftershocks were distributed linearly along a NNW direction, and the fault plane was nearly vertical with a length over 30 km and a width of about 15 km. Aftershocks were more concentrated in the southeast than in the northwest. The focal mechanism solutions of most aftershocks in the central and southeastern regions were consistent with the mainshock, while those in the northwest were thrust-types, which might be related to the Minjiang fault. Meanwhile, the regional stress was released more in the central and southeastern regions than in the northwest. The maximum intensity investigated in the damage zone was up to IX. The maximum intensity region was located in scenic areas, therefore few people were present when the earthquake occurred at night. The peak acceleration was highest in the NS records, followed by the EW and vertical records. The design spectra of intensity for Jiuzhaigou was Ⅷ, which is higher than the acceleration response spectra obtained from the Jiuzhaibaihe station, the nearest station which had strong motion recordings. These aforementioned factors may have contributed to the minor casualties resulting from this earthquake. The aftershock regions of the Jiuzhaigou earthquake, the 1973 M_s6.5 Songpan northeast earthquake, and the 1976 M_s7.2 Songpan earthquake are connected along the Huya fault which may extend to the northwest in the deep earth. Considering the rupture displacement distribution of the mainshock, the focal mechanism of aftershocks, and the stress drop, strong aftershocks are unlikely to occur in the central and southeastern Jiuzhaigou aftershock regions; however, the development of seismicity in the northwest and the Minjiang River fault should be noted. Static Coulomb stress triggering of other 4 earthquakes larger than M6.5 occurred near the Ganqingchuan border were calculated using the Coulomb 3.3 software. The results indicated that the Jiuzhaigou earthquake was triggered by the Wenchuan earthquake and related to the stress adjustment in the study area.
The M_s7.0 Jiuzhaigou earthquake with the hypocenter depth of 20 km occurred at the NNW extension line of the Huya fault located next to the eastern boundary of the Bayan Har block. The focal mechanism solution of the mainshock based on the W-phase source inversion showed a sinistral slip and the moment magnitude was M_w6.5. Over 3000 aftershocks were recorded within six days, among which the largest was M4.8 and three others were larger than M4.0. The value of the aftershock frequency attenuation coefficient P was 1.03, and the b value of the magnitude-frequency relationship was 0.68. The aftershock activities were relatively inactive but the attenuation was normal. Relocation results of 603 aftershocks were obtained by using the double-difference earthquake location algorithm and the location errors of the EW, NS and the vertical directions were 0.81, 0.84 and 1.59 km respectively. The mainshock occurred in the center of the aftershock region and ruptured on both sides along the strike direction. The aftershocks were distributed linearly along a NNW direction, and the fault plane was nearly vertical with a length over 30 km and a width of about 15 km. Aftershocks were more concentrated in the southeast than in the northwest. The focal mechanism solutions of most aftershocks in the central and southeastern regions were consistent with the mainshock, while those in the northwest were thrust-types, which might be related to the Minjiang fault. Meanwhile, the regional stress was released more in the central and southeastern regions than in the northwest. The maximum intensity investigated in the damage zone was up to IX. The maximum intensity region was located in scenic areas, therefore few people were present when the earthquake occurred at night. The peak acceleration was highest in the NS records, followed by the EW and vertical records. The design spectra of intensity for Jiuzhaigou was Ⅷ, which is higher than the acceleration response spectra obtained from the Jiuzhaibaihe station, the nearest station which had strong motion recordings. These aforementioned factors may have contributed to the minor casualties resulting from this earthquake. The aftershock regions of the Jiuzhaigou earthquake, the 1973 M_s6.5 Songpan northeast earthquake, and the 1976 M_s7.2 Songpan earthquake are connected along the Huya fault which may extend to the northwest in the deep earth. Considering the rupture displacement distribution of the mainshock, the focal mechanism of aftershocks, and the stress drop, strong aftershocks are unlikely to occur in the central and southeastern Jiuzhaigou aftershock regions; however, the development of seismicity in the northwest and the Minjiang River fault should be noted. Static Coulomb stress triggering of other 4 earthquakes larger than M6.5 occurred near the Ganqingchuan border were calculated using the Coulomb 3.3 software. The results indicated that the Jiuzhaigou earthquake was triggered by the Wenchuan earthquake and related to the stress adjustment in the study area.
引文
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2 Earthquake Prevention and Defense Department of China Earthquake Administration.Catalogue of Chinese Earthquakes 1912-1990,Ms≥4.7(in Chinese).Beijing:China Science and Technology Press,1999[中国地震局震害防御司.中国近代地震目录:公元1912年~1990年,Ms≥4.7.北京:中国科学技术出版社,1999]
3 Xu X W,Wen X Z,Ye J Q,et al.The Ms8.0 Wenchuan earthquake surface ruptures and its seismogenic structure(in Chinese).Seismol Geol,2008,30:597-629[徐锡伟,闻学泽,叶建青,等.汶川Ms8.0地震地表破裂带及其发震构造.地震地质,2008,30:597-629]
4 Niu Z J,Wang M,Sunh R,et al.Contemporary velocity field of crustal movement of Chinese mainland from Global Positioning System measurements.Chin Sci Bull,2005,50:939-941
5 Zhang P Z,Xu X W,Wen X Z,et al.Slip rates and recurrence intervals of the Longmen Shan active fault zone,and tectonic implications for the mechanism of the May 12 Wenchuan earthquake,Sichuan,China(in Chinese).Chin J Geophys,2008,51:1066-1073[张培震,徐锡伟,闻学泽,等.2008年汶川8.0级地震发震断裂的滑动速率、复发周期和构造成因.地球物理学报,2008,51:1066-1073]
6 Chen L C,Ran Y K,Wang H,et al.The Lushan Ms7.0 earthquake and activity of the southern segment of the Longmenshan fault zone(in Chinese).Chin Sci Bull,2013,58:1925-1932[陈立春,冉勇康,王虎,等.芦山地震与龙门山断裂带南段活动性.科学通报,2013,58:1925-1932]
7 Chen G G,Ji F J,Zhou R J,et al.Primary research of activity segmentation of Longmenshan fault zone since Late Quaternary(in Chinese).Seismol Geol,2007,29:657-673[陈国光,计凤桔,周荣军,等.龙门山断裂带晚第四纪活动性分段的初步研究.地震地质,2007,29:657-673]
8 Zhang J L,Ren J W,Fu J D,et al.Earthquake rupture features and tectonics significance of the Tazang fault in the eastern part of the east Kunlun fault zones(in Chinese).Earthquake,2012,32:1-16[张军龙,任金卫,付俊东,等.东昆仑断裂带东部塔藏断裂地震地表破裂特征及其构造意义.地震,2012,32:1-16]
9 Qian H,Zhou R J,Ma S H,et al.South segment of Minjiang fault and Diexi earthquake in 1933(in Chinese).Earthq Res China,1999,15:333-338[钱洪,周荣军,马声浩,等.岷江断裂南段与1933年叠溪地震研究.中国地震,1999,15:333-338]
10 Zhao X L,Deng Q D,Chen S F.Tectonic geomorphology of the Minshan uplift in western Sichuan,Southwestern China(in Chinese).Seismol Geol,1994,16:429-439[赵小麟,邓起东,陈社发.岷山隆起的构造地貌学研究.地震地质,1994,16:429-439]
11 Deng Q D.Maps of Active Tetonics of China(in Chinese).Beijing:Seismological Press,2007[邓起东.中国活动构造图.北京:地震出版社,2007]
12 Cesca S,Heimann S,Stammler K,et al.Automated procedure for point and kinematic source inversion at regional distances.J Geophys Res,2010,115:1-24
13 Wan Y G.Introduction to Seismology(in Chinese).Beijing:Science Press,2016[万永革.地震学导论.北京:科学出版社,2016]
14 Guo L C,Pang M H.Surface-wave magnitude of earthquakes and its station correction(in Chinese).Acta Seismol Sin,1981,3:312-320[郭履灿,庞明虎.面波震级和它的台基校正值.地震学报,1981,3:312-320]
15 Han X J,Ma Y L,Liu R F.The measurement method research of the new IASPEI standard broadband surface wave magnitude(in Chinese).Seismol Geomag Obs Res,2011,32:9-12[韩雪君,马延路,刘瑞丰.IASPEI宽频带面波震级的测定方法研究.地震地磁观测与研究,2011,32:9-12]
16 Bormann P,Liu R,Xu Z,et al.First application of the new IASPEI teleseismic magnitude standards to data of the China National Seismographic Network.Bull Seism Soc Am,2009,99:1868-1891
17 The Working Group on Magnitudes of the International Association of Seismology and Physics of the Earth’s Interior(IASPEI)Commission on Seismological Observation and Interpretation.Summary of Magnitude Working Group recommendations on standard procedures for determining earthquake magnitudes from digital data.International Association of Seismology and Physics of the Earth’s Interior(IASPEI),2013
18 Duputel Z,Rivera L,Kanamori H,et al.W-phase fast source inversion for moderate to large earhquakes(1990-2010).J Geophys Res,2012,189:1125-1147
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