GNSS/Pseudolites������λ�е�α�����Ż�ģ���о�

???GNSS/Pseudolites???????α????????????????????????????????μ?GNSS????α????????????,??????????λ??????????????????????????????????????????????????????????????????α??????????????????????????????????????仯????Ч????????????????????????λ????????????μ?PDOP????????????????????仯?????????????PDOP?????????????????????????????????ЧЭ?????????????????????????????????????????Ч????α???????GNSS?????Ч??????     

GPS��̬���β����еĶ�·��ЧӦ�����о�

?????????Χ??????????????GPS??·??Ч????к??????????????????β????е?GPS??·??Ч?????????????????????????????顣???????????????μ???е??·??Ч?????????г??????????????????????????????????????????????????????????????????????????????????????????t????????????????????·??Ч??????????????GPS???????????????30%?????     

���μ�����ݵ�С��������Ԥ�ⷽ��

??????μ?????????????????????????С??????????????????????С???????????????μ??????????????????????????????????ó????????б????ó?????:С??????????????μ??????????????????????Ч????     

����ǰ��Դ����λ�����о�

????С??????????????α??????????????ε??????????????????????????????μ?????????????????????????λ?????????1995???????????????????7??6????6????????????????????У????????Ч????     

��С������������ͨKriging���ıȽ�

?????????????????????????????????С???????ú????Kriging????????????????????????÷??????Kriging??????????????????????????μ??????????????????1??????????????????￡?????????????Kriging???????????????÷??????????????￡?????????????÷??????????????Kriging????????2????:???????????????У????Kriging??????????Ч?????????     

��ͬ�����¼����˲������ıȽ��о����Ľ�

????о???GPS???μ???????????????????????????С???????????????????????????????????????Ч?????ó?????????????????????÷?Χ????????????????????????????????????????????????????????????С???????????????????????????????????????????????????????????????Ч??????????????     

���ڸ߽�̩�ռ���չ��ʽ�Ķ������ӳ����ڲ��о�

???????μ???巽??????????????????????????ZTD?????÷????????????????????????????????????????????幫?????????????????????????????????????????Ч????ZTD????徫???????SCIGN?????GPS?????????????????????????Χ?????????????????????????????????????ZTD???????????????????????????????????????????????????????????????????????????????????????????????????????????????????     

Mohr-Coulomb�����Բ����׼���ڱ����ȶ������е�Ӧ��

?????????????????????????????ж???????????Mohr-Coulomb?????????????????????????????????????Ч????????????????μ?????????????????????????????????????k????0.8?????????????????????????????????????????????????????????????????С??Mohr-Coulomb??Ч????????????????????????k???????????Mohr-Coulomb??Ч?????????????????????????????????????????????k???0.8~0.9??????     

GPS���μ������ȡ��������ĵ���Ԫ���㷽���о�

????????????????????????L₁???????????????????GPS????????μ???????????????μ??????????????????????????????????ARCE??????????????????????????????????±1??????????????????п????????????????????????????????L₁?????????????????????????????????????????Ч???????????????????????????ú???Ч????     

���ڸĽ�С����ֵȥ�뷨�ı���Ԥ���о�

?????С?????????????????????μ???????????????С???任????????????????????μ??????????????????????????????????????????ι????????????н??????????????????????????Ч???????????????????淽????     

����������3��7�����ϵ��������챳��

?????????????????????????????????????????????????????????????????????????????????1969????1976???????????????????3??7?????????????????????????Щ????????: ??????????????????????????????????28 km;?????????????????????????????α??????????????????;?????????????????????????????λ???????;??????????????3??????????????????????????????????????????????????????????????????????????????й??     

沂沭断裂带及邻区双差层析成像

利用双差层析成像方法,选取2008-10～2017-12山东及周边区域182个地震台站记录的1190个近震观测资料,对沂沭断裂带及邻区的震源位置和三维速度结构进行联合反演.结果表明,沂沭断裂带内部介质速度结构具有明显的不均匀性,并呈现分段特性;在郯城和莒县中上地壳内存在明显的低速结构;胶南地块总体速度低于鲁西地块;鲁西...     

2017-06巴东MS4.3地震序列视应力变化

采用固定台站的宽频带数字地震波形资料，计算2017-06-16巴东MS4.3地震序列16个ML1.8以上地震的视应力、拐角频率及震源破裂半径等震源参数，并系统分析地震视应力值与各参数之间的关系。结果表明,地震序列视应力值与震级正相关，地震震源谱的高频成分不丰富，拐角频率和视应力值均远小于非水库区的构造地震，震源区地下结构较为复杂。     

2020-01-23四川石渠MS4.3地震震源机制及发震构造研究

基于数字地震台网波形数据,采用gCAP反演方法解算四川石渠M_S4.3地震的震源机制。结果表明,最佳双力偶解为节面Ⅰ走向134°、倾角82°、滑动角11°,节面Ⅱ走向42°、倾角79°、滑动角171°;最佳质心深度为9 km,矩震级为M_W4.53。为测试震源机制解的稳定性和可靠性,从地壳速度结构、定位误差和数据质量影响等方面进行分析,研究结果表明,这些因素对反演结果影响较小。余震序列展布方向为NW向,主要分布在主震偏北东侧附近,发震断层具有向NE倾的趋势。综合震源区地质构造特征、主震震源机制解和余震序列的空间分布特征,初步判断石渠地震的发震断层面为节面Ⅰ,即长沙贡玛断裂,是一次左旋走滑型地震事件。     

1932年麻城6.0级强震的蕴育环境条件探讨

本文在活断层研究和地震宏观调查的基础上,从现代地壳运动特征及活动断层几何学,运动特征等方面研究了1932年麻城Ms6.0级地震的蕴育环境条件,为预测该区强震的地点和强度提供依据。     

�Ͷ�Ms5.1����——һ���µ�ˮ���������

????2013????5.1?????????????????????????????????????????????仯??????????????????????????Ч???????????????????????????????й?????????з???????????????????????????淢????????????????????????????????????????й??????????????????????????????????Ms5.1?????????????????????????????????????????????????????????????????????????淢???????????γ?????????????????????????????????????????????????桢???????????????????μ???????????--????????????????     

�봨8.0������ǰ��ؿǴ�ֱ�α����

??????8.0?????????????????????????????????????Ms8.0?????????????α????????:???????????α???????????????????????????????????仯???????????????????????????????????????????????????????????????????????????????α???????     

Seismogenic structures of the 2006 M<Subscript>L</Subscript>4.0 Dangan Island earthquake offshore Hong Kong

The northern margin of the South China Sea, as a typical extensional continental margin, has relatively strong intraplate seismicity. Compared with the active zones of Nanao Island, Yangjiang, and Heyuan, seismicity in the Pearl River Estuary is relatively low. However, a M_L4.0 earthquake in 2006 occurred near Dangan Island (DI) offshore Hong Kong, and this site was adjacent to the source of the historical M5.8 earthquake in 1874. To reveal the seismogenic mechanism of intraplate earthquakes in DI, we systematically analyzed the structural characteristics in the source area of the 2006 DI earthquake using integrated 24-channel seismic profiles, onshore–offshore wide-angle seismic tomography, and natural earthquake parameters. We ascertained the locations of NW- and NE-trending faults in the DI sea and found that the NE-trending DI fault mainly dipped southeast at a high angle and cut through the crust with an obvious low-velocity anomaly. The NW-trending fault dipped southwest with a similar high angle. The 2006 DI earthquake was adjacent to the intersection of the NE- and NW-trending faults, which suggested that the intersection of the two faults with different strikes could provide a favorable condition for the generation and triggering of intraplate earthquakes. Crustal velocity model showed that the high-velocity anomaly was imaged in the west of DI, but a distinct entity with low-velocity anomaly in the upper crust and high-velocity anomaly in the lower crust was found in the south of DI. Both the 1874 and 2006 DI earthquakes occurred along the edge of the distinct entity. Two vertical cross-sections nearly perpendicular to the strikes of the intersecting faults revealed good spatial correlations between the 2006 DI earthquake and the low to high speed transition in the distinct entity. This result indicated that the transitional zone might be a weakly structural body that can store strain energy and release it as a brittle failure, resulting in an earthquake-prone area.     

��Ͽˮ��Ͷ������ĵ�������

????????μ??????????????????????????仯???????????????????????????????????????????????????????????????????????????????????????????????????к??????????????????????????????????????     

Effect of lithology and structure on seismic response of steep slope in a shaking table test

Studies on landslides by the 2008 Wenchuan earthquake showed that topography was of great importance in amplifying the seismic shaking, and among other factors, lithology and slope structure controlled the spatial occurrence of slope failures. The present study carried out experiments on four rock slopes with steep angle of 60° by means of a shaking table. The recorded Wenchuan earthquake waves were scaled to excite the model slopes. Measurements from accelerometers installed on free surface of the model slope were analyzed, with much effort on timedomain acceleration responses to horizontal components of seismic shaking. It was found that the amplification factor of peak horizontal acceleration, RPHA, was increasing with elevation of each model slope, though the upper and lower halves of the slope exhibited different increasing patterns. As excitation intensity was increased, the drastic deterioration of the inner structure of each slope caused the sudden increase of RPHA in the upper slope part. In addition, the model simulating the soft rock slope produced the larger RPHA than the model simulating the hard rock slope by a maximum factor of 2.6. The layered model slope also produced the larger RPHA than the homogeneous model slope by a maximum factor of 2.7. The upper half of a slope was influenced more seriously by the effect of lithology, while the lower half was influenced more seriously by the effect of slope structure.