地电阻率观测在地震预测中的应用

doi:10.3969/j.issn.0253-4967.20240168

摘要/Abstract

摘要：

基于岩土介质电阻率变化开展地震预测, 是野外观测、科学研究和预测实践相互结合与促进的系统性工作。中国应用于地震监测预报的地电阻率观测, 采用直流电法连续测量地下固定探测体积内介质电阻率随时间的变化。通过计算直流稳恒电流场的电位分布, 实现了地电阻率地表和井下观测的解析计算和数值分析。在垂直方向, 一维影响系数分布揭示了不同深度地层电阻率变化对观测的影响程度; 更为细致的三维影响系数分布, 则揭示了测区不同区域地层电阻率变化对观测影响的差异性, 明确了地电阻率观测的局域性特点。岩石物理实验和电阻率理论模型揭示出压应力加载过程中, 含水岩土介质电阻率具有各向异性特征的下降变化与微裂隙定向扩展之间的关系。通过断层虚位错模式分析地震前震中周围相对的变形积累特征, 以区域变形为中间桥梁, 电磁学科建立了观测站的异常变化与远距离地震晚期孕育过程之间的联系过程, 得到了与孕震过程有关的地电阻率异常的预期形态, 在此基础上开展“以源观场”的地震中短期预测, 对近年来发生的2022年泸定 M_S6.8、2023年积石山 M_S6.2 和2024年乌什 M_S7.1 等地震做出了较好的预测。以上研究内容散见于时间跨度超过60年的国内外文献之中。文中对基于地电阻率观测开展地震预测的主要基础理论进行回顾总结, 以便地电分析人员能较为便捷地了解并应用于地震预测实践。

关键词: 地电阻率, 地震, 异常变化, 地震预测, 理论基础, 区域变形

Abstract:

Earthquake prediction based on changes in the resistivity of rock and soil media is a systematic endeavor that integrates field observation, scientific research, and forecasting practice. Apparent resistivity observation, which is widely used in earthquake monitoring and prediction in China, employs the direct-current method to continuously measure temporal changes in resistivity within a fixed subsurface investigation volume. Analytical calculations and numerical analyses of apparent resistivity observations conducted at the surface and underground have been developed by computing the potential distribution of the DC steady-current field. During the establishment of observation stations, electrical sounding should be carried out to invert the electrical structure of subsurface formations, and analytical calculations should be performed to determine the theoretical range of observational values, thereby verifying the correctness of the actual observation array configuration. Both analytical computation and numerical analysis can also be used to investigate the influence of resistivity variations in different parts of the medium on the observations. These methods provide reasonable explanations for three types of annual variation and for the characteristics of diurnal variation in apparent resistivity observations. In anomaly verification, they also enable quantitative evaluation of the interference amplitudes caused by leakage currents and electrically anomalous bodies. In the vertical direction, the one-dimensional sensitivity coefficient distribution reveals the extent to which resistivity changes at different depths affect the observations. The more detailed three-dimensional sensitivity coefficient distribution further reveals the differences in the effects of resistivity changes in different regions of the monitoring area on the observations. Therefore, the sensitivity coefficient distribution characterizes the local features of apparent resistivity observations and allows the influence of resistivity changes in different regions on the observations to be rapidly determined qualitatively. Petrophysical experiments and theoretical resistivity models have revealed the relationship between anisotropic resistivity decreases in water-bearing rock-soil media and the directional propagation of microcracks during compressive stress loading. In shallow subsurface layers, microcrack systems are predominantly aligned with the direction of the maximum horizontal principal compressive stress. During stress loading, the apparent resistivity measured in the direction perpendicular to the maximum principal compressive stress shows the largest variation amplitude, whereas that measured in the parallel direction shows the smallest variation, and that in an oblique direction exhibits an intermediate response. Through analysis of geoelectrical resistivity anisotropy, the orientation of the regional horizontal stress field can be inferred. The relative deformation accumulation around the epicenter before earthquakes has been analyzed using a virtual fault dislocation model. By using regional deformation as an intermediate bridge, a preliminary link has been established between anomalous changes at observation stations and the late-stage seismogenic process of distant earthquakes, and the expected patterns of apparent resistivity anomalies related to seismogenic processes have thus been obtained.

When observation stations are located within compressional enhancement zones during the seismogenic process, apparent resistivity exhibits anomalous decreases, whereas stations located in dilatational domains show anomalous increases. Transitional zones between compression and dilatation typically display weak or negligible anomalous variations. Based on earthquake case studies, persistent apparent resistivity anomalies lasting from several months to approximately two years serve as magnitude indicators for earthquake prediction, providing important constraints on potential epicentral locations and earthquake magnitudes. By contrast, short-impending anomalies characterized by accelerated variations or high-frequency perturbations act as temporal indicators and provide predictive information on earthquake timing. In operational earthquake forecasting, the spatial location and magnitude should first be preliminarily estimated using magnitude indicators, followed by short-term time prediction through continuous monitoring of temporal indicators within the pre-identified risk zone. On this basis, medium- and short-term earthquake predictions have been carried out from the perspective of interpreting field anomalies in terms of their seismic source processes. In recent years, the 2022 M_S6.8 Luding, 2023 M_S6.2 Jishishan, and 2024 M_S7.1 Wushi earthquakes were successfully predicted using the apparent resistivity method. However, the relevant research is scattered across domestic and international literature spanning more than 60 years. This paper therefore reviews and summarizes the main theoretical foundations of earthquake prediction based on apparent resistivity observations, so as to facilitate their understanding and application in geoelectrical earthquake prediction practice.

Key words: apparent resistivity, earthquake, anomaly, earthquake prediction, basic theory, regional deformation

解滔, 李新艳, 韩盈, 于晨, 李晓帆. 地电阻率观测在地震预测中的应用[J]. 地震地质, 2026, 48(3): 597-650.

XIE Tao, LI Xin-yan, HAN Ying, YU Chen, LI Xiao-fan. APPLICATION OF APPARENT RESISTIVITY OBSERVATION IN EARTHQUAKE PREDICTION[J]. SEISMOLOGY AND GEOLOGY, 2026, 48(3): 597-650.

图/表 33

表1 部分岩土介质孔隙度

Table1 The porosity of some rock and soil

序号	岩石、土层	孔隙度/%	序号	岩石、土层	孔隙度/%	序号	岩石、土层	孔隙度/%
1	变质页岩	0.02~0.60	8	石英岩	0.00~8.70	15	古近-新近纪砂岩	2.20~42.00
2	花岗岩	0.05~2.80	9	黏土质砂岩	0.40~10.00	16	白垩纪砂岩	7.20~37.70
3	大理岩	0.10~6.00	10	砂质页岩	1.50~44.80	17	三叠纪砂岩	0.60~27.70
4	硅质页岩	0.80~1.50	11	砂岩	8.10~9.50	18	砾岩	20.20~37.70
5	黑色页岩	0.70~1.40	12	中生代石灰岩	1.20~26.50	19	黏土	10.10~62.90
6	片麻岩	0.30~2.40	13	板岩状页岩	1.10~20.00	20	土壤	20.00~69.40
7	硬石膏	0.03~6.26	14	侏罗纪砂岩	4.20~24.60

表2 常见岩土介质电阻率

Table2 The resistivity of common rock and soil

序号	岩石、土层	电阻率//Ω·m	序号	岩石、土层	电阻率/Ω·m	序号	岩石、土层	电阻率/Ω·m
1	硬石膏	10⁴~10⁶	11	石英岩	10⁶~10⁸	21	石膏	10⁵~10⁷
2	石灰岩	10⁴~10⁸	12	片岩	10³~10⁸	22	裂隙石灰岩	10⁴~10⁶
3	砾岩	10¹~10⁸	13	页岩	10³~10⁵	23	结晶石灰岩	10⁴~10⁶
4	砂岩	10^-1~10⁸	14	泥质板岩	10³~10⁵	24	砂质石灰岩	10⁸
5	花岗岩	10⁶~10⁷	15	黏土质页岩	10³~10⁵	25	黄土层	0~200
6	辉长岩	10⁵~10⁶	16	粉砂岩	10⁴~10⁶	26	干砂卵石层	>600
7	石英斑岩	10⁴~10⁶	17	多孔砂岩	10⁵~10⁶	27	含水砂卵石层	50~500
8	橄榄岩	10⁴~10⁷	18	致密砂岩	10⁵~10⁶	28	隔水黏土层	5~30
9	千枚岩	10⁴~10⁵	19	泥灰岩	10⁴~10⁵	29	白垩纪黏土	5~10
10	大理岩	10⁵~10⁷	20	白云岩	10⁵~10⁶	30	黏土	1~200

图1 岩土介质电阻率影响因素 a 孔隙度的影响(Тархова, 1963); b 含水饱和度的影响(胡庆东等, 1993); c 温度的影响(Пархоменко, 1965)

Fig. 1 Factors affecting resistivity of rock and soil medium.

图2 地电阻率对称四级观测装置 a 地表观测; b 井下观测

Fig. 2 The Schlumberger array used in apparent resistivity monitoring.

图3 地电阻率解析计算与有限元数值计算结果对比 a 三层电性结构; b 解析方法与有限元数值计算结果

Fig. 3 Comparison of the apparent resistivity compulated from analytical and finite element method.

图4 地电阻率影响系数 a 甘孜站电测深曲线与电性结构; b 一维影响系数; c 三维影响系数在地表的平面分布; d 三维影响系数沿测道垂直剖面的分布

Fig. 4 The sensitivity coefficients of apparent resistivity.

图5 地电阻率影响系数随深度的变化 a 供电极距为2 000m; b 供电极距为1 000m; c 供电极距为500m

Fig. 5 The sensitivity changes of apparent resistivity with depth.

图6 单轴压缩试验中应力-应变曲线与不同阶段的裂隙变化(修改自Xue et al., 2014)

Fig. 6 Stress-strain diagram showing different stages of crack development during the uniaxial compression test(modified from Xue et al., 2014).

图7 地震前兆异常机理的2种物理模式 a 流体膨胀扩散模式(DD模式, 修改自Scholz et al., 1973); b 裂隙雪崩扩展模式(IPE模式, 修改自Mjachkin et al., 1975)

Fig. 7 Two physical models of earthquake precursor anomaly mechanism.

图8 含原生裂隙的介质在低围压条件下单轴压缩时的新生裂隙变化 a 岩石物理实验结果(张恒等, 2015); b 数值模拟结果(张志强等, 2020), α为岩桥角度

Fig. 8 Growth of new cracks in medium containing preexisting cracks under compressive stress loading with low confining pressure.

图9 压应力加卸载过程中介质电阻率变化 a 含水凝灰岩样品在单轴压缩应力作用下的电阻变化(修改自Morrow et al., 1981); b 野外原地压应力作用下的地电阻率变化(赵玉林等, 1983)

Fig. 9 Electrical resistivity changes under compressive stress.

图10 裂隙沿优势展布方向扩展时介质电阻率和地电阻率的变化 ρ1和ρ2为水平方向电性主轴, 其中ρ1平行于裂隙优势展布方向, ρ2与之垂直, ρ3为垂直方向的电性主轴; ρa1、ρa2、ρa3 分别为在地表观测时与优势展布方向平行、45° 夹角、垂直方向观测的地电阻率。 a 裂隙沿优势展布方向扩展示意图; b、c 无水介质无水补给; d、e 含水介质无水补给; f、g 含水介质有水补给, 含水饱和度保持不变

Fig. 10 Variations in medium and ground resistivity during fracture growth along the dominant orientation.

图11 断层虚位错模式示意图 a 2022年泸定 MS6.8 地震同震位移(修改自单新建等, 2023); b走滑断层的虚位错模式

Fig. 11 Schematic diagram of virtual dislocation model of fault.

图12 2008年汶川 MS8.0 地震前地电阻率异常(负值为挤压)

Fig. 12 Apparent resistivity anomalies before the 2008 Wenchuan MS8.0 earthquake (negative value refers compression).

图13 发生在地电阻率观测站网内及附近的17次(组)MS≥7.0地震

Fig. 13 The 17 earthquakes with MS≥7.0 occurred within or near the apparent resistivity monitoring network China.

表3 中国14次MS≥7.0地震前地电阻率异常变化与震源机制解P轴方位的关系

Table3 The relationship between apparent resistivity anomalies and P-axis before the 14 earthquakes with MS≥7.0 in China

序号	日期	地点	M_S	观测站	D/km	测道	RC/%	T/月	θ/(°)	参考文献
1	1969-07-18	渤海	7.4	隆尧	418	NS	-3.2	10	66	汪志亮等,2002
				隆尧	418	EW	-2.0	10	24
				牛家桥	405	NS	-1.5	8	66
				牛家桥	405	EW			24
				大曹庄	400	NS	-1.5	6	66
				大曹庄	400	EW			24
2	1973-02-06	炉霍	7.6	甘孜	45	N30°E	-7.0	3	50	钱复业等,1980
				甘孜	45	N60°W	-4.5	3	40
				雅安	300	N30°E	-4.5	4	50
				雅安	300	EW			10
				松潘	320	NS	-2.0	7	80
				松潘		EW			10
				康定	220	NS	+2.0	6	80
				康定	220	EW			10
3	1974-05-11	大关	7.1	西昌	180	NS	-5.2	11	88	汪志亮等,2002
				西昌	180	EW	-1.3	11	2
				米易	245	NS	-3.5	11	88
				米易	245	EW	-1.3	11	2
				会理	240	NS	+1.5	15	88
				会理	240	EW	+2.9	15	2
4	1975-02-04	海城	7.3	台安	90	N51°W	+9.0	10	73	汪志亮等,2002
				台安	90	N39°E			27
				昌黎	310	NS	-2.0	9	66
				昌黎	310	EW	-2.0	9	24
5	1976-05-29	龙陵	7.4 7.3	腾冲	54	N73°E	-10.5	25	68	钱家栋等,1985
				腾冲	54	N17°W	-3.7	25	34	钱家栋等,1985
				楚雄	292	N75°E	+7.5	12	54	汪志亮等,2002
				楚雄	292	N60°W			21	汪志亮等,2002
6	1976-07-28	唐山滦县	7.8 7.1	唐山	5	NS	-5.5	18	78	国家地震局预测预防司,1998
				唐山	5	EW	-3.0	18	12
				昌黎	35	NS	-6.4	13	75
				昌黎	35	EW	-6.0	13	15
				宝坻	80	NS	-3.0	16	78
				宝坻	80	EW	-2.2	16	12
				青光	110	NS	-3.1	12	78
				青光	110	EW	-2.7	12	12
				忠兴庄	150	N40°E	-4.5	19	38
				忠兴庄	150	N48°W	-5.0	19	54
				马家沟	10	N25°W	-17.6	2	77
				马家沟	10	N69°E	-15.0	2	9
				八里桥	140	NS	-4.7	17	78
				八里桥	140	EW			12
				西集	120	NS	-3.3	17	78
				西集	120	EW			12
				徐庄子	140	NS	+2.6	9	78
				徐庄子	140	EW	+1.9	9	12
				青县	160	NS	-2.0	2d	78
				青县	160	EW			12
				小汤山	170	N50°W	-5.0	9	52
				小汤山	170	N40°E			38
7	1976-08-16 1976-08-23	松潘平武	7.2 7.2	武都	100	N85°E	-2.0	19	22	钱复业等,1980
						N45°W	-4.0	19	72
						N72°W	-3.4	19	45
				松潘	70	NS	-2.0	14	85
				松潘	70	EW			5
8	1988-11-06	澜沧耿马	7.6 7.2	腾冲	215	EW	-5.0	20	80	汪志亮等,1989
8	1988-11-06	澜沧耿马	7.6 7.2	腾冲	215	NS			10	汪志亮等,1989
9	1990-04-26	共和	7.0	武威	282	EW	+7.1	8	36	张肇诚等,2000
9	1990-04-26	共和	7.0	武威	282	NS			54	张肇诚等,2000
10	1996-02-03	丽江	7.0	冕宁	237	N5°E	-2.3	11	2
						N45°W	-4.4	6	48
						N85°W			88
11	2008-05-12	汶川	8.0	成都	35	N58°E	-6.7	22	61	杜学彬,2010
				成都	35	N49°W			12
				江油	30	N70°W	-1.5	22	65
				江油	30	N10°E			15
				甘孜	330	N30°E	-5.3	22	83
				甘孜	330	N60°W	-4.9	22	7
				武都	110	N54°W	+2.9	22	41
						N73°W			22
						N85°E			0
12	2013-04-20	芦山	7.0	成都	99	N58°E	-6.2	9	58	杜学彬等,2015
12	2013-04-20	芦山	7.0	成都	99	N49°W			15	杜学彬等,2015
13	2017-08-08	九寨沟	7.0	天水	240	N56°E	0.4	5	49	高曙德,2020
						N24°W	0.4	5	51
						N75°W	0.3	5	0
				玛曲	195	N34°E	-2.3	6	71
				玛曲	195	N68°W	-1.5	6	7
				武都	110	垂直Ⅰ	+1.5	9
				武都	110	垂直Ⅱ	+1.5	9
14	2024-01-23	乌什	7.1	柯坪	90	NS	0.5	10	40	解滔等,2025a
14	2024-01-23	乌什	7.1	柯坪	90	EW	0.6	10	50	李新艳等,2025

表3 中国14次MS≥7.0地震前地电阻率异常变化与震源机制解P轴方位的关系

Table3 The relationship between apparent resistivity anomalies and P-axis before the 14 earthquakes with MS≥7.0 in China

序号	日期	地点	M_S	观测站	D/km	测道	RC/%	T/月	θ/(°)	参考文献
1	1969-07-18	渤海	7.4	隆尧	418	NS	-3.2	10	66	汪志亮等,2002
				隆尧	418	EW	-2.0	10	24
				牛家桥	405	NS	-1.5	8	66
				牛家桥	405	EW			24
				大曹庄	400	NS	-1.5	6	66
				大曹庄	400	EW			24
2	1973-02-06	炉霍	7.6	甘孜	45	N30°E	-7.0	3	50	钱复业等,1980
				甘孜	45	N60°W	-4.5	3	40
				雅安	300	N30°E	-4.5	4	50
				雅安	300	EW			10
				松潘	320	NS	-2.0	7	80
				松潘		EW			10
				康定	220	NS	+2.0	6	80
				康定	220	EW			10
3	1974-05-11	大关	7.1	西昌	180	NS	-5.2	11	88	汪志亮等,2002
				西昌	180	EW	-1.3	11	2
				米易	245	NS	-3.5	11	88
				米易	245	EW	-1.3	11	2
				会理	240	NS	+1.5	15	88
				会理	240	EW	+2.9	15	2
4	1975-02-04	海城	7.3	台安	90	N51°W	+9.0	10	73	汪志亮等,2002
				台安	90	N39°E			27
				昌黎	310	NS	-2.0	9	66
				昌黎	310	EW	-2.0	9	24
5	1976-05-29	龙陵	7.4 7.3	腾冲	54	N73°E	-10.5	25	68	钱家栋等,1985
				腾冲	54	N17°W	-3.7	25	34	钱家栋等,1985
				楚雄	292	N75°E	+7.5	12	54	汪志亮等,2002
				楚雄	292	N60°W			21	汪志亮等,2002
6	1976-07-28	唐山滦县	7.8 7.1	唐山	5	NS	-5.5	18	78	国家地震局预测预防司,1998
				唐山	5	EW	-3.0	18	12
				昌黎	35	NS	-6.4	13	75
				昌黎	35	EW	-6.0	13	15
				宝坻	80	NS	-3.0	16	78
				宝坻	80	EW	-2.2	16	12
				青光	110	NS	-3.1	12	78
				青光	110	EW	-2.7	12	12
				忠兴庄	150	N40°E	-4.5	19	38
				忠兴庄	150	N48°W	-5.0	19	54
				马家沟	10	N25°W	-17.6	2	77
				马家沟	10	N69°E	-15.0	2	9
				八里桥	140	NS	-4.7	17	78
				八里桥	140	EW			12
				西集	120	NS	-3.3	17	78
				西集	120	EW			12
				徐庄子	140	NS	+2.6	9	78
				徐庄子	140	EW	+1.9	9	12
				青县	160	NS	-2.0	2d	78
				青县	160	EW			12
				小汤山	170	N50°W	-5.0	9	52
				小汤山	170	N40°E			38
7	1976-08-16 1976-08-23	松潘平武	7.2 7.2	武都	100	N85°E	-2.0	19	22	钱复业等,1980
						N45°W	-4.0	19	72
						N72°W	-3.4	19	45
				松潘	70	NS	-2.0	14	85
				松潘	70	EW			5
8	1988-11-06	澜沧耿马	7.6 7.2	腾冲	215	EW	-5.0	20	80	汪志亮等,1989
8	1988-11-06	澜沧耿马	7.6 7.2	腾冲	215	NS			10	汪志亮等,1989
9	1990-04-26	共和	7.0	武威	282	EW	+7.1	8	36	张肇诚等,2000
9	1990-04-26	共和	7.0	武威	282	NS			54	张肇诚等,2000
10	1996-02-03	丽江	7.0	冕宁	237	N5°E	-2.3	11	2
						N45°W	-4.4	6	48
						N85°W			88
11	2008-05-12	汶川	8.0	成都	35	N58°E	-6.7	22	61	杜学彬,2010
				成都	35	N49°W			12
				江油	30	N70°W	-1.5	22	65
				江油	30	N10°E			15
				甘孜	330	N30°E	-5.3	22	83
				甘孜	330	N60°W	-4.9	22	7
				武都	110	N54°W	+2.9	22	41
						N73°W			22
						N85°E			0
12	2013-04-20	芦山	7.0	成都	99	N58°E	-6.2	9	58	杜学彬等,2015
12	2013-04-20	芦山	7.0	成都	99	N49°W			15	杜学彬等,2015
13	2017-08-08	九寨沟	7.0	天水	240	N56°E	0.4	5	49	高曙德,2020
						N24°W	0.4	5	51
						N75°W	0.3	5	0
				玛曲	195	N34°E	-2.3	6	71
				玛曲	195	N68°W	-1.5	6	7
				武都	110	垂直Ⅰ	+1.5	9
				武都	110	垂直Ⅱ	+1.5	9
14	2024-01-23	乌什	7.1	柯坪	90	NS	0.5	10	40	解滔等,2025a
14	2024-01-23	乌什	7.1	柯坪	90	EW	0.6	10	50	李新艳等,2025

图14 横向不均匀模型的地电阻率各向异性变化 a 模型结构示意图; b 模型表面8个方向的对称四级装置; c 第1层介质各向同性, 第2~3层各向异性; d 第1层介质各向异性, 第2~3层各向同性; e 3层均为各向异性

Fig. 14 Anisotropic changes in apparent resistivity of the lateral inhomogeneity model.

图15 1976年唐山 MS7.8 地震断层虚位错模式结果

Fig. 15 Deformation based on fault virtual dislocation model before the Tangshan MS7.8 earthquake.

图16 地电阻率观测正常与异常形态 a 定西站正常观测数据; b 2021年漾濞 MS6.4 地震前红格站年尺度下降异常; c 2021年漾濞 MS6.4 地震前红格站去年变曲线; d 1998年张北 MS6.2 地震前宝昌站年变畸变异常; e 1976年松潘-平武 MS7.2 地震前武都站加速下降短期异常; f 2013年芦山 MS7.0 地震前天水站高频扰动短期异常

Fig. 16 Normal and anomalous changes of apparent resistivity.

图17 部分MS≥7.0地震前地电阻率异常 a 1976年炉霍 MS7.6 地震前甘孜站异常; b 1974年大关 MS7.1 地震前西昌站异常; c 1976年唐山 MS7.8 地震前宝坻站异常; d 2013年芦山 MS7.0 地震前成都站异常; e 1988年澜沧-耿马 MS7.6 地震前腾冲站异常; f 1990年共和 MS7.0 地震前武威站异常; g 1996年丽江 MS7.0 地震前冕宁站异常; h 2008年汶川 MS8.0 地震前成都站异常

Fig. 17 Some examples of apparent resistivity anomalies before MS≥7.0 earthquakes.

图18 部分6.0≤MS≤6.9地震前地电阻率异常 a 1989年大同-阳高 MS6.1 地震前代县站异常; b 1998年张北 MS6.2 地震前宝昌站异常; c 1998年宁蒗 MS6.2 地震前元谋站异常; d 2003年民乐-山丹 MS6.1 地震前山丹站异常; e 2009年姚安 MS6.0 地震前元谋站异常; f 2013年岷县-漳县 MS6.6 地震前通渭站异常; g 2014年鲁甸 MS6.5 地震前西昌站异常; h 2016年门源 MS6.4 地震前山丹站异常

Fig. 18 Some examples of apparent resistivity anomalies before earthquakes with 6.0≤MS≤6.9.

图19 1976年唐山 MS7.8 地震前后昌黎站地电阻率和水位观测数据

Fig. 19 The apparent resistivity and water level data of Changli station before and after the 1976 Tangshan MS7.8 earthquake.

图20 岩土介质电阻率对裂隙变化的放大系数 a 放大系数随裂隙纵横比的变化; b 放大系数随骨架与裂隙水电阻率比值的变化

Fig. 20 The amplification coefficients of rock and soil resistivity on fracture change.

图21 自适应变化幅度方法提取地电阻率弱幅度异常 a 2015年阿左旗 MS5.8 地震前石嘴山站地电阻率年尺度下降异常; b石嘴山站地电阻率相对变化幅度; c 2023年平原 MS5.5 地震前兴济站地电阻率年尺度下降异常; d 兴济站地电阻率相对变化幅度。红色虚线为异常阈值,黑色虚线为零值线, 2条对称的蓝色实线之间的幅度为年变化幅度

Fig. 21 Weak anomalies of the apparent resistivity extracted by adaptive amplitude variation method.

图22 2017年九寨沟 MS7.0 地震周围地电阻率观测站分布与异常变化

Fig. 22 Distribution of resistivity observation stations and anomaly changes before the 2017 MS7.0 Jiuzhaigou earthquake.

图23 6级以上地震前不同震中距范围地电阻率出现异常的比例 a MS≥7.0地震; b 6.0≤MS≤6.9地震

Fig. 23 The proportion of apparent resistivity anomalies at different epicentral distance before MS≥6.0 earthquakes in China.

图24 地电阻率异常持续时间与震级的经验统计关系(修改自钱复业等,1982)

Fig. 24 The empirical relationship between apparent resistivity anomaly duration and earthquake magnitude(modified from QIAN Fu-ye et al., 1982).

图25 地电阻率强度依据异常的阶段划分(汪志亮等,2002)

Fig. 25 The stage division of apparent resistivity anomaly(from WANG Zhi-liang et al., 2002).

图26 2023年积石山 MS6.2 地震周围地电阻率观测站分布与异常变化

Fig. 26 Distribution of resistivity observation stations and anomaly changes before the 2023 MS6.2 Jishishan earthquake.

图27 2023年积石山 MS6.2 地震前区域变形

Fig. 27 Regional deformation before the 2023 MS6.2 Jishishan earthquake.

图28 2024年乌什 MS7.1 地震前区域变形与地电阻率异常变化

Fig. 28 Regional deformation and apparent resistivity anomaly changes before the 2024 MS7.1 Wushi earthquake.

图29 2022年泸定 MS6.8 地震周围地电阻率观测站分布与异常变化

Fig. 29 Distribution of resistivity observation stations and anomaly changes before the 2022 MS6.8 Luding earthquake.

图30 2022年四川3次6级以上地震前的区域变形 a 芦山 MS6.1 地震; b 康定 MS6.0 地震; c 泸定 MS6.8 地震

Fig. 30 Regional deformation before the three earthquakes with magnitude greater than 6 in 2022.

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