岩溶山区隧道工程对地下水资源的影响分析

温金梅; 吴涛; 李娴; 江晨; 陈立; 刘胜; 蒙丽

doi:10.11932/karst20250304

岩溶山区隧道工程对地下水资源的影响分析——以重庆巫山某隧道为例

doi: 10.11932/karst20250304

温金梅^1,,
吴涛^1, ,,
李娴²,
江晨²,
陈立¹,
刘胜¹,
蒙丽³

1.
重庆市地质矿产勘查开发局208水文地质工程地质队(重庆市地质灾害防治工程勘查设计院), 重庆 400700
2.
合肥工业大学土木与水利工程学院, 安徽合肥 230009
3.
重庆大学环境与生态学院, 重庆 400045

基金项目: 重庆市长江经济带1∶5万奉节幅、巫山幅水文地质调查（ ZC-2021109(21C01730) ）；国家自然科学青年科学基金项目 (42107082)；安徽省自然科学基金项目(2108085QD166）

详细信息

作者简介:
温金梅（1982－），女，正高级工程师，硕士，从事水工环地质调查研究工作。E-mail：576563874@qq.com

通讯作者:
李娴（1984—），女，副教授，博士，从事水文地质研究工作。E-mail：xianli@hfut.edu.cn。

中图分类号: U453.6；P641
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- 文章访问数: 23
- HTML浏览量: 6
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- 被引次数: 0
出版历程
- 收稿日期: 2024-09-04
- 录用日期: 2024-12-27
- 修回日期: 2024-12-24
- 网络出版日期: 2025-09-03
- 刊出日期: 2025-06-25

Analysis of the influence of tunnel engineering on groundwater resources in karst mountain areas: A case study of a tunnel in Wushan county of Chongqing City

WEN Jinmei^1
,,
WU Tao^{1
, ,},
LI Xian²,
JIANG Chen²,
CHEN Li¹,
LIU Sheng¹,
MENG Li³

1.
No.208 Hydrogeology and Engineering Geology Team, Chongqing Bureau of Geology and Mineral Exploration and Development (Chongqing Institute of Geological Hazard Prevention Engineering Investigation and Design), Chongqing 400700, China
2.
College of Civil Engineering, Hefei University of Technology, Hefei, Anhui 230009, China
3.
College of Environment and Ecology, Chongqing University, Chongqing 400045, China

摘要

摘要: 隧道工程建设可破坏施工区的地下水平衡，引发地下水疏降以及其他生态环境问题。文章以某引水隧道为研究对象，基于隧道周边水库蓄水量明显减少的问题，采用水文地质调查、示踪试验等方法，查明补径排条件变化特征，分析引水隧道工程与周边地下水之间的水力联系及其对周边水库蓄水量变化的影响。引水隧道施工过程中，周边3 km范围内有12处泉点呈疏干或半疏干状态，且隧道南西侧泉点受影响程度较北西侧小。基于解析法计算可知引水隧道开挖后对地表水及地下水的影响半径范围为649~2073 m，影响面积为13.7 km²，与水库集水范围重叠面积为4.02 km²。野外示踪试验结果表明引水隧道上部地表落水洞与引水隧道排水口、部分泉点之间存在密切的水力联系，水库的部分补给水源改向隧道口径流和排泄，致使水库蓄水量减少。研究结果表明引水隧道工程建设改变了周边地下水补径排条件，从而导致水库水源不足，蓄水量减少，影响了城市居民供水。
- 隧道工程建设 /
- 地下水 /
- 蓄水量 /
- 影响 /
- 示踪试验
Abstract: Tunnel construction can disrupt the groundwater balance, impacting the drainage of both surface water and groundwater, as well as causing other eco-environmental effects. This study takes a water-diversion tunnel as the research object. Prompted by a pronounced decline in the storage of the adjacent reservoir of the tunnel, it integrates hydrogeological surveying and tracer tests to characterize the altered recharge–flow–discharge conditions, elucidate the hydraulic interactions between the tunnel and the surrounding groundwater system, and quantitatively evaluate the tunnel’s impact on the observed reservoir-storage variations.Field investigations indicate that groundwater in the study area can be divided into three categories: karst water from carbonate rock fissures, karst water from fissures characterized by carbonate rock interbedded with clastic rock, and karst water from pores and fissures characterized by mudstone interbedded with silty mudstone. The water bearing formations of karst water from carbonate rock fissures consist of the Lower Triassic Jialingjiang Formation (T₁j) and the Daye Formation (T₁d³⁺⁴) along the axis and wings of an anticline. These units exhibit significant water abundance and are well developed with karst landforms, such as karst depressions, sinkholes, caves, and underground rivers. Karst water from fissures characterized by carbonate rock interbedded with clastic rock occurs within the first and third members of the Middle Triassic Badong Formation (T₂b¹⁺³) along the axis and wings of a syncline. The water abundance of the formation is moderate, and karst features are only locally developed. Karst water from pores and fissures characterized by mudstone interbedded with silty mudstone is primarily stored in the second member of the Middle Triassic Badong Formation (T₂b²) and exhibits comparatively low water abundance. Groundwater recharge is derived primarily from atmospheric precipitation and surface water bodies such as reservoirs and fish ponds. Due to the large terrain cutting, the speed of surface water runoff is fast.The catchment of the reservoir is located west of the axis of the water-diversion tunnel on the southeast wing of the anticline. Exposed strata comprise limestone, dolomitic limestone, dolomite, and rock-solution breccia of T₁j and T₁d³⁺⁴, as well as limestone, argillaceous limestone, argillaceous dolomite, and mudstone of T₂b. Within the Jialingjiang and Daye Formations, sinkholes, depressions, and dissolution fissures are well developed, facilitating efficient infiltration of rainwater through karst conduits to the saturated zone. Although karst development is weak in the Badong Formation, secondary structures have intensely fractured the rock mass; rainwater recharge, therefore, occurs dominantly through fissures. Overall, the catchment exhibits favorable groundwater recharge conditions. After infiltration, groundwater migrates southwestward along either longitudinal karst conduits or fissure networks. The deeply cut watercourse in which the reservoir is located, along with the dense network of tributary gullies, ultimately leads to the discharges of groundwater in the form of karst springs within these gullies.The water-diversion tunnel crosses the anticline, traversing limestone and dolomite of T₁d and T₁j, with T₁j serving as the principal aquifer. The anticlinal axis functions as a watershed, resulting in the southern and northern segments of the tunnel each forming an independent groundwater system. The tunnel site is deeply cut, resulting in poor recharge conditions. Scattered precipitation accumulates only within the upper narrow peak-cluster depressions, subsequently infiltrating vertically along sinkholes. Southwest of the tunnel, the reservoir catchment consists of T₁j, T₁d, and T₂b formations, which are characterized by well-developed sinkholes, karst depressions, and corrosion fissures that create favorable discharge conditions. Following rainfall events, groundwater is directed southwestward along longitudinally oriented karst conduits. These conduits are cut by gullies, where groundwater ultimately discharges as karst springs. Before the construction of the water-diversion tunnel, atmospheric precipitation infiltrated through surface karst depressions, sinkholes, dolines, or corrosion fissures to recharge groundwater. Afterward, a portion of the precipitation flowed through the aquifer and discharged in the form of an underground river along the riverbank. Another portion of flowed through the runoff that crossed fissures perpendicular to the structural trend, and discharged in the form of karst springs (including the S01 spring point) or underground rivers within the gully and watercourse that cut the south-eastern wing of the anticline. The spring points exposed in the gully and watercourse were the main source of water supply for the reservoir. Because the water-diversion tunnel intersected the transition zone between the vertical and horizontal circulation cells of the karst aquifer, its excavation repeatedly intersected underground rivers and cave systems. Severe water inflows were encountered, resulting in twelve springs within a 3-km radius becoming either completely or partially dewatered. Springs located to the southwest of the tunnel were less affected than those to the northwest.Analytical calculations indicate that the influence radius of the water-diversion tunnel on surface water and groundwater extends from 649 to 2,073 m, covering 13.7 km². The overlapping area of the reservoir catchment is 4.02 km². Tracer tests confirm a strong hydraulic connection between the surface sinkholes located above the tunnel, and the drainage outlet of the water-diversion tunnel and several spring points. Consequently, a portion of the reservoir’s recharge has been diverted to runoff at the tunnel exit and subsequently discharged, thereby reducing the storage capacity of the reservoir. The findings demonstrate that the alteration of regional groundwater recharge–flow–discharge conditions induced by the tunnel project is the primary cause of the observed decline in groundwater-derived inflow to the nearby reservoir.
- tunnel projects /
- groundwater /
- storage capacity of the reservoir /
- influence /
- tracer test

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图 1 研究区地理位置图

Figure 1. Location map of the study area

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图 2 研究区水文地质图

T₁d^1-4.三叠系下统大冶组1-4段 T₁J^1-4.三叠系下统嘉陵江组1-4段 T₂b^1-4.三叠系中统巴东组1-4段 1.碳酸盐岩裂隙溶洞水 2.碳酸盐岩夹碎屑岩裂隙溶洞水 3.泥页岩夹粉砂质泥岩孔隙裂隙水 4.泉点(左编号，右流量L·s⁻¹) 5.疏干泉 6.无水隧道口 7.有水隧道口 8.落水洞 9.示踪剂投放点 10.示踪剂接收点 11.水文地质钻孔 12.地下水流向 13.分水岭

Figure 2. Hydrogeological map of the study area

T₁d^1-4.Members 1-4 of the Daye Formation of the Lower Triassic Series T₁J^1-4.Members 1-4 of the Jialingjiang Formation of the Lower Triassic Series T₂b^1-4.Members 1-4 of the Badong Formation of the Middle Triassic Series 1. karst water from carbonate rock fissures 2. karst water from fissures characterized by carbonate rock interbedded with clastic rock 3. karst water from pores and fissures characterized by mudstone interbedded with siltstone 4. spring points (left: number; right: flow L·s⁻¹) 5. draining spring 6. waterless tunnel entrance 7. watery tunnel entrance 8. sinkhole 9. tracer injection point 10. tracer receiving point 11. hydrogeological borehole 12. direction of groundwater flow 13. watershed.

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图 3 影响半径计算点

Figure 3. Calculation points for influence radius

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图 4 引水隧道口和泉点S01的Na⁺浓度历时变化曲线图

Figure 4. Variation curves of the concentration of Na⁺at the tunnel exit and the spring S01

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表 1 水库补给源泉点水资源调查情况统计表

Table 1. Statistics of water resource investigation of the spring recharge for the reservoir

泉点编号	地层	施工前调查流量/L·s⁻¹	施工后调查时流量/L·s⁻¹	动态特征	目前利用情况	疏降情况
S01	T₂b¹	1.00~5.00	0.50	常年不干，枯丰季流量变化幅度1~5倍，暴雨可增至10倍	供附近10余户居民作生活用水	半疏干
S02	T₂b¹	1.00~10.00	0	隧道修通后完全断流	未利用	疏干
S03	T₁j⁴	0.05~0.50	0	隧道修通后完全断流	未利用	疏干
S04	T₁j⁴	1.00~3.00	0	季节性泉，隧道修建后完全断流	未利用	疏干
S05	T₂b²	0.10~1.00	0	原常年有水，隧道修建后完全断流	未利用	疏干
S06	T₁j³	0.10~0.50	0	季节性泉，隧道修通后完全断流	平时无人利用，有水时供附近2~3户人作生活用水	疏干
S07	T₁j⁴	0.50~2.00	0.10	常年不干，枯丰季流量变化幅度1~10倍，暴雨可增至50倍	研究区水库的主要地下水来源之一，供周边3~5户人作生活用水及灌溉用水	半疏干
S08	T₂b²	0.01~0.05	0.001	常年不干，枯丰季流量变化幅度1~3倍，暴雨可增至5倍	供附近1~2户人作生活用水	半疏干
S09	T₂b²	0.02~0.10	0.065	常年不干，枯丰季流量变化幅度1~3倍，暴雨可增至5倍	供附近5~8户人作生活用水	无影响
S10	T₂b²	0.10~1.00	0.10	常年不干，枯丰季流量变化幅度1~5倍，暴雨可增至10倍	淹没于水库之下，为水库的主要地下水补给源之一	无影响

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表 2 引水隧道对周边地下水的影响范围计算结果

Table 2. Calculation results of the influence range of the water-diversion tunnel on the surrounding groundwater

计算点	地层	岩性	渗透系数/m·d⁻¹	含水层厚度/m	给水度	降水补给强度/m·d⁻¹	时间/d	影响半径/m
1	T₁d³	灰泥灰岩	0.038	730	0.09	0.003	3559	1450
2	T₁d³	灰泥灰岩	0.038	490				1079
3	T₁d³	灰泥灰岩	0.065	830				2073
4	T₁d⁴	灰岩		760				1951
5	T₁j¹	灰岩		600				1646
6	T₁j³	灰岩		200				649

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