广西武宣盘龙铅锌矿岩溶塌陷成因机制分析

卢丹美; 邓忠; 姚克追; 曾家华; 王生杰; 全铝兴; 郭德恒; 田朋

doi:10.11932/karst20260111

广西武宣盘龙铅锌矿岩溶塌陷成因机制分析

doi: 10.11932/karst20260111

广西水文地质工程地质勘察院, 广西柳州 545006

基金项目: 广西矿山水文地质勘查评价关键技术研究人才小高地建设（桂地矿办[2023]55 号文）

详细信息

作者简介:
卢丹美（1987−），女，硕士研究生，高级工程师，主要从事水文地质工程地质环境地质研究。E-mail：372474664@qq.com

通讯作者:
邓忠（1974−），男，硕士，正高级工程师，主要从事水文地质工程地质环境地质研究。E-mail: 973706528@qq.com。

中图分类号: P642.25
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出版历程
- 收稿日期: 2024-10-16
- 录用日期: 2025-02-20
- 修回日期: 2025-01-03
- 网络出版日期: 2026-05-27
- 刊出日期: 2026-02-25

Analysis of the formation mechanism of karst collapse in the Panlong lead-zinc mine, Wuxuan, Guangxi

Hydrogeological and Engineering Geological Team of the Guangxi Zhuang Autonomous Region, Liuzhou, Guangxi 545006, China

摘要

摘要: 岩溶塌陷是岩溶地区主要地质灾害类型之一，具有突发性和隐蔽性的特征。历年来，在广西武宣盘龙铅锌矿山开采及大藤峡水库蓄水等人类工程活动影响下，矿区陆续发生岩溶塌陷100余处，给人们的生命财产和安全带来威胁。为弄清盘龙铅锌矿连续发生的岩溶塌陷的发育规律和成因机制，开展了现场调查、水文地质工程钻探、物探、地下水动态长期监测、现场水文地质试验等多项工作。结果表明：研究区地质环境条件脆弱，地下岩溶发育强−中等，覆盖层薄，地下水富水性丰富−中等，是岩溶塌陷发生的内在因素。由于矿山疏干排水、降雨和水库蓄水导致的降落漏斗范围内地下水位动态变化大且频繁是引发岩溶塌陷的地质灾害的外在因素。长期大流量疏干地下水，是研究区诱发岩溶塌陷的重要人为因素。根据矿山开采过程和塌陷的发生过程，将盘龙铅锌矿岩溶塌陷分为三个阶段：降落漏斗形成阶段、降落漏斗稳定阶段和水库蓄水阶段，不同阶段的主导地质营力和致塌模式也存在一定的差别。
- 盘龙铅锌矿 /
- 岩溶塌陷 /
- 影响因素 /
- 形成机制 /
- 矿山疏干排水
Abstract: Karst collapse is a major geological hazard in karst areas, characterized by suddenness and concealment. Over the years, human engineering activities-such as mining at the Panlong lead-zinc mine in Wuxuan, Guangxi, and the impoundment of the Datengxia Reservoir-have triggered more than 100 karst collapse events in the mining area. These events pose serious threats to human life, property, and public safety. To elucidate the development patterns and triggering mechanisms of successive karst collapses at the Panlong lead-zinc mine, comprehensive investigations and studies were conducted. These include field surveys, hydrogeological and engineering geological drilling, geophysical exploration, long-term groundwater dynamic monitoring, and in-situ hydrogeological testing. The main research findings are as follows.1. The fragile geological environment, characterized by moderately-to highly-developed underground karst, thin overburden layers, and moderate- to abundant groundwater resources, constitutes an intrinsic factor for karst collapse.The study area is extensively developed with underground karst features that serve as storage spaces or transport channels for groundwater and collapse materials. Groundwater resources are abundant, while the overburden layers are relatively thin, and the soil exhibits poor engineering geological properties, facilitating the formation of soil caves due to groundwater activity. These fragile geological environmental conditions are the internal cause of karst collapse in the study area.2. Long-term, large-scale groundwater dewatering is a key anthropogenic factor inducing karst collapse in the study area.Mine drainage has caused a rapid decline in groundwater levels, an increase in groundwater hydraulic gradient, and an enhanced erosion capacity of groundwater on the overlying soil. Long-term mine drainage, combined with the effects of rainfall (especially heavy rainfall) and reservoir impoundment on groundwater within the cone of depression, results in significant and frequent fluctuations in groundwater levels. These fluctuations are a critical external factor contributing to karst collapse in the study area.3. Based on the mining process and characteristics of collapse occurrences, karst collapse events at the Panlong Lead-Zinc Mine can be divided into three stages: the formation stage of depression funnel, the stabilization stage of depression funnel, and the impoundment stage of reservoir. The dominant geological forces and collapse modes vary moderately across these stages.(1) Formation stage of depression funnel: Mine drainage causes a decline in groundwater levels, forming a depression funnel and altering regional hydrogeological and engineering geological conditions. Before mining, the soil was mostly in a pressured, saturated state; however, after the sudden drop in water levels, it lost water buoyancy support, resulting in reduced stability and increased load effects. In addition, the increased groundwater flow velocity enhances soil transport capacity, while karst pipelines act as discharge channels for soil particles, thereby promoting the development of soil caves. Meanwhile, the rapid decline in water levels generates negative pressure within karst caves, triggering collapse under the combined effects of erosion and negative pressure.(2) Stabilization stage of depression funnel: Under specific mining depths, the drainage remains stable, and the depression funnel temporarily stops expanding. However, the dewatering effect continues, maintaining groundwater levels below the bedrock surface for an extended period. Sudden fluctuations in water and gas pressure within karst pipelines caused by heavy rainfall are the main triggering factors. For instance, six concentrated collapses occurred after a 120 mm heavy rainfall event on June 11, 2022. This heavy rainfall caused a sharp rise and fall in groundwater levels, forming an alternating cycle of positive and negative pressures. The rising water levels triggered a gas explosion effect, while the subsequent decline intensified seepage erosion and negative pressure effects. The combination of these factors with pre-existing soil caves ultimately resulted in collapse.(3) Impoundment stage of the Datengxia Reservoir: After the reservoir was impounded in March 2020, the water level of the Qianjiang River rose to 35–53 m. Changes in river water levels, combined with the effects of mine drainage and rainfall, exacerbated fluctuations in groundwater levels. During impoundment, river water recharges the groundwater, causing its level to rise; during regulation and storage phases, the decline in river water levels leads to a corresponding drop in groundwater levels. High-frequency variations in mine drainage result in frequent and significant fluctuations in groundwater levels, providing sufficient hydrodynamic and aerodynamic conditions for the formation, expansion, and collapse of soil caves.
- Panlong lead-zinc mine /
- karst collapse /
- influencing factors /
- formation mechanism /
- mine dewatering and drainage

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图 1 大藤峡水利枢纽与武宣县盘龙铅锌矿区位置示意图

Figure 1. Location diagram of Datengxia Water Conservancy Project and Panlong lead-zinc mining area in Wuxuan County

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图 2 区域水文地质图

Figure 2. Regional hydrogeological map

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图 3 岩溶塌陷空间分布图

Figure 3. Spatial distribution map of karst collapse

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图 4 WT6测线物探结果

Figure 4. Geophysical exploration results of WT6 survey line

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图 5 疏干排水影响范围

Figure 5. Influence zone of dewatering and drainage

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图 6 −70 m中段疏干巷西42线溶洞“8·30”突水两个月后降落漏斗横断面图

Figure 6. Cross section of depression funnel two months after water inrush from cave "8·30" at west 42 line of the −70 m middle section of the dewatering roadway

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图 7 G25、G26监测点地下水位-降雨历时曲线

Figure 7. Groundwater table-rainfall duration curve at G25 and G26 monitoring points

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图 8 G25、G26监测点地下水位变化速率

Figure 8. Change rate of groundwater level at G25 and G26 monitoring points

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表 1 中部矿区地下水系统水文地质特征

Table 1. Hydrogeological characteristics of the groundwater system in the central mining area

地下水系统	大岭矿地下水子系统	崩山矿地下水子系统	大坪岭地下水子系统	六沙地下水子系统
水文地质结构特征	南、北隔水边界长度分别为4.8 km、3.1 km，西部弱透水（F₂）长为1.1 km，东部黔江补给边界长为0.9 km，面积2.51 km²	北西为二塘组（D₁e）泥灰岩相对隔水边界，长4.40 km；东为F₂断层弱透水边界，长4.45 km，面积1.58 km²	东至黔江、北至F₄断层，南北宽约0.6 km，东西长约2.4 km，面积2.01 km²	西为F₂断层、东面与北面为黔江，近似梯形状，为河岸突出地块，面积3.08 km²
地下水补径排条件	黔江常年补给地下水，漏斗中心及其以西地下水由西往东径流	充水来源于降雨补给及北东部地下水经浅层溶洞、溶蚀裂隙进入，穿过F₂断层浅部岩体向东方向运移，以渗流形式向大岭矿坑径流	主要靠降雨入渗，局部分水岭以西的地下水往西径流，分水岭以东地段的地下水部分向黔江排泄，官桥组地层地下水经2线−18线的降落漏斗补给矿坑	地下水与大岭矿坑基本无水力联系，与黔江具有互补关系，地下水由南西向北东径流，排泄于黔江
地下水水位动态特征	漏斗中心动水位变幅约26 m，西部动水位变幅9~13 m，东部动水位变幅6~35 m	降落漏斗已经扩展到崩山矿地下水子系统，动水位年变幅约1~25 m；水位动态与降雨量基本一致	含水层结构呈隔水、含水间隔条带平行组合受矿坑疏干排水的影响，动水位年变幅1~31 m	黔江蓄水前该系统地下水位变幅8.31~11.66 m，与黔江呈互补关系，表现出气象型动态特征

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表 2 岩溶发育程度统计表

Table 2. Statistics of karst development degree

分布地段	崩山矿地下水子系统	大岭矿地下水子系统	大坪岭地下水子系统	六沙地下水子系统
塌陷/个	32	22	53	17
地裂缝/个	1	1	0	0
岩溶洼地/个	2	8	4	9
地表岩溶合计/个	35	31	57	26
统计面积/km²	1.54	2.45	2.01	3.10
岩溶发育密度/(个·km⁻²）	22.73	12.65	26.50	5.48
遇洞隙率/%	33	27.74

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表 3 钻孔单位涌水量统计表

Table 3. Statistics of borehole specific yield

地段	盘古至崩山矿一带		大岭矿−大坪岭−黔江沿岸一带
钻孔编号	DK4	SK5	DK1	DK2	DK3	DK5	DK6	SK4
单位涌水量/L·(s·m）⁻¹	0.20	0.82	0.18	0.25	0.06	0.18	0.25	0.08 （F2断层带）

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表 4 矿区下伏岩层-120 m标高以上岩溶发育程度统计表

Table 4. Statistics of karst development degree in the underlying strata above elevation −120 m in the mining area

代号	钻孔揭露地层遇洞隙率/%	线岩溶率/ %	塌陷数量/ 个
D₃r	0	0	18
D₂d	0	0	5
D₁d	0	0	0
D₁g	17.52	1.39	36
D₁e	4.97	0.27	14
D₁sl²	31.37	1.77	60

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表 5 −70中段西42线溶洞突水前后西部主要疏干区观测井水位动态变化统计表

Table 5. Statistics of dynamic changes of observed well water level in the western main drainage areas before and after water inrush from karst cave at west 42 line of the −70 middle section

孔号	2021年8月29日水位标高/m （突水前一天）	2021年9月6日水位标高/m （突水后一周）	降深/ m	2021年11月3日水位标高/m （突水后2个月）	突水后2个月稳定降深
B01	−4.06	−9.45	5.39	−24.25	20.19
B02	17.50	11.74	5.76	−3.18	20.68
B05	59.28	59.94	0.66	57.57	1.71
B06	4.40	−5.64	10.04	−19.36	23.76
B07	2.07	−13.65	15.72	−27.15	29.22
B08	−9.78	−29.96	20.18	−40.72	30.94
B09	69.57	69.56	−0.10	68.67	0.90
水421	−18.40	−50.69	32.29	−56.00	37.6
G01	−4.39	−24.54	20.15	−49.99	45.6
G03	−0.46	−15.38	15.84	−30.35	29.89
G04	8.59	8.60	−0.01	−18.79	27.38
G30	12.94	2.52	10.42	−13.12	26.06
G31	16.37	10.97	5.40	−2.33	18.70
G32	27.35	23.23	4.12	10.76	16.59
G33	42.25	39.67	2.58	29.33	12.92
SK5	29.94	30.92	−0.98	18.41	11.53

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