Application of high-density resistivity method and audio-frequency magnetotelluric method in the detection of landslide structure in Houchang town
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摘要: 文章采用高密度电阻率法和音频大地电磁法对贵州省威宁县猴场滑坡区进行探测，探究从浅部到深部岩溶及裂缝发育情况、岩溶滑坡体底界面形态及滑坡体结构特征。通过音频大地电磁法划分了滑坡区地层结构，发现滑坡区发育浅部和深部两层岩溶，尤其在灰岩与泥页岩界面处的深部岩溶，加之煤层开采形成的采空区，是触发滑坡的背景条件；通过高密度电阻率法探测出的裂缝及岩溶发育区域，是滑坡体进一步位移拉裂的脆弱区。分析认为，岩溶发育破坏了滑坡体原来的整体性，使岩溶山体劣化成零散块体，是导致滑坡的关键因素之一。Abstract:
The frequent occurrence of landslides in China has done great harm to people's lives and property. In the stability analysis of landslides and the design of treatment scheme, the application of geophysical technologies has become a frontier research field in engineering and environment in terms of interdisciplinary development and application. The Houchang landslide in Weining county, Bijie City, Guizhou Province is a typical karst landslide. The landslide area is dominated by karst peak-cluster depressions or gullies, in which limestone strata are widely distributed, and karst is strongly developed. Since the collapse and landslide in 2006, the scale of tensile cracks in rock mass has gradually increased. In order to explore the causes of collapse, scholars have deduced the collapse process, established the conceptual model of landslide and studied the karst hydrogeological conditions. However, due to the lack of detection data, the structural characteristics of landslides have not been fully understood. In this study, the high-density resistivity method and audio-frequency magnetotelluric method were used to detect the landslide area, and the structural characteristics of landslides were revealed from the development of shallow karst and cracks, and the bottom interface of karst landslide. The stratigraphic structure of landslide area was divided by audio-frequency magnetotelluric method, and the lithologic interface between Qixia–Maokou Formation and Liangshan Formation was defined according to the electrical characteristics of different lithologic strata. Furthermore, the clastic rocks of Liangshan Formation in some areas were divided into shale, carbonaceous shale and coal seam. It is found that there are two layers of karst development: one is the karst fracture zone in the shallow part of the karst mountain, which is filled with mud and other low-resistivity substances, and the development depth of the karst layer gradually increases from northeast to southwest; the other is the deep karst fracture zone at the bottom interface of limestone in Qixia–Maokou Formation, which is mainly developed in the southern part of the landslide mountain, showing low-resistance characteristics. These two layers of karst structures provide a weak layer for landslide regeneration. Cracks and karst development areas have been detected by high-density resistivity method. There are three mountain cracks in the landslide mountain, including one with a large front edge and two secondary cracks at the rear edge. The cracks show the characteristics of "local high-resistance zone in the low-resistance layer on the surface and vertical low-resistance zone in the underground high-resistance rock mass". In addition, some shallow vertical karst fracture zones were detected, which destroyed the integrity of karst mountain. With the development of karst, karst mountain deteriorated into scattered fragments, which may gradually collapse or landslide under some extreme conditions. It is considered that the development of karst, especially the deep karst at the interface between limestone and shale, is one of the key factors leading to landslides. Together with the goaf formed by coal seam mining, karst development is the background condition that may trigger landslides, which in turn can deteriorate karst mountains into scattered blocks and gradually into collapses and landslides. The combination of audio-frequency magnetotelluric method and high-density electrical method can effectively detect the structural characteristics of karst landslides, and can comprehensively obtain the characteristics of karst spatial development, crack location and distribution of landslide bottom interface, which can provide an important basis for in-depth and comprehensive analysis of landslide stability. -
图 4 音频大地电磁法测量装置示意图
Figure 4. Schematic diagram of audio-frequency magnetotelluric method
图 6 音频大地电磁数据重复性检查曲线对比图
Figure 6. Contrast of repetitive check curves of audio-frequency magnetotelluric data
图 8 L1线高密度电阻率法数据反演及解译结果图
Figure 8. Results of inversion and interpretation of high-density resistivity data of Line 1
图 9 L2线高密度电阻率法数据反演及解译结果图
Figure 9. Results of inversion and interpretation of high-density resistivity data of Line 2
图 10 L11线高密度电阻率法数据反演及解译结果图
Figure 10. Results of inversion and interpretation of high-density resistivity data of Line 11
图 11 L12线高密度电阻率法数据反演及解译结果图
Figure 11. Results of inversion and interpretation of high-density resistivity data of Line 12
表 1 猴场滑坡区地层岩性表
Table 1. List of strata and lithology in Houchang landslide area
地层划分 主要岩性特征 厚度/m 栖霞茅口组（P2q+m） 灰至深灰色厚层至块状灰岩夹燧石灰岩、白云质灰岩 约200 梁山组（P2l） 细砂岩、石英砂岩、石英粉砂岩夹灰色页岩、炭质页岩及煤层。层煤多以煤线及透镜体产出，
目前发现可采稳定煤层只有1层，位于灰岩与梁山组接触面以下35~50 m深度，可采厚度0.5~0.8 m110~130 
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表 2 测线布置信息表
Table 2. Information of line survey arrangement
测线编号 测线长度/m 测线方位/° 点距/m L1 690 110 10 L2 590 139 10 L11 1 700 33 10~200 L12 649 21.2 11
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表 3 高密度电阻率法测量情况表
Table 3. Information of high-density resistivity method
测线 测线长度/m 测点数/个 点距/m 测点起始编号 装置类型 L1 590 60 10 1310~1900 对称四极和三极测深 L2 649 60 11 991~1640 对称四极和三极测深 L11 590 60 10 1080~1670 对称四极和三极测深 L12 590 60 10 1080~1670 对称四极和三极测深
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表 4 音频大地电磁法测量情况表
Table 4. Information of audio-frequency magnetotelluric method
测线 测线长度/m 测点数/个 点距/m 测点起始编号 装置类型 L1 690 39 10~20 1270~1960 张量 L11 1 700 36 10~200 920~2620 张量
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表 5 高密度电阻率法开工前后数据对照表
Table 5. Contrast of data before and after the use of high-density resistivity method
高密度电阻率法开工/收工测量数据 均方根误差 点号 1400 1410 1420 1430 1440 1450 1460 1470 1480 1490 1500 2.05% 开工前数据 702.2 413.7 610.5 575 603.8 655.4 592.4 697 870 692 770.2 收工后数据 701.3 410.9 613.6 575.1 604 655.6 591 696.5 869.5 691.5 769.7
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