基于滇中典型紧窄单斜岩溶水系统特征的隧洞涌水条件分析

黄盛财; 成建梅; 巴净慧; 李仲夏; 徐文杰; 王研

doi:10.11932/karst20230305

基于滇中典型紧窄单斜岩溶水系统特征的隧洞涌水条件分析

doi: 10.11932/karst20230305

1.
中国地质大学(武汉), 湖北武汉 430078
2.
云南地质工程第二勘察院有限公司, 云南昆明 650218

基金项目: 国家自然科学基金项目（42172278）

详细信息

作者简介:
黄盛财（1996－），男，硕士研究生，研究方向为岩溶水文地质。E-mail：hsccug@163.com

通讯作者:
成建梅（1971－），女，教授，主要从事地下水水流和污染数值模拟方面的教学与科研工作。E-mail：jmcheng@cug.edu.cn

中图分类号: P641；U456
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出版历程
- 收稿日期: 2022-08-08
- 录用日期: 2023-02-23
- 修回日期: 2022-10-26
- 刊出日期: 2023-06-30

Analysis of tunnel inflow conditions based on the characteristics of typical tight-narrow monoclinic karst water system in the central Yunnan Province, China

1.
China University of Geosciences, Wuhan, Hubei 430078, China
2.
No.2 Yunnan Institute for Geological Engineering Survey Co., Ltd., Kunming, Yunnan 650218, China

摘要

摘要: 中国西南地区分布着大面积的碳酸盐岩，地层和构造的空间组合结构差异形成了多种复杂而各具特色的岩溶水系统。当隧洞穿越岩溶水系统时，涌水问题表现各异，涌水条件难以识别，这一直是隧洞工程建设面临的重要挑战。滇中引水工程小扑隧洞隧址区发育线状延伸、紧密互层的可溶与非可溶岩地层，构成典型的紧窄单斜岩溶水系统。文章细致梳理研究区岩溶水系统特征的控制性因素，结合地下水监测信息和水化学特征识别小扑隧洞的涌水条件。结果表明：紧窄单斜构造影响了岩溶发育的空间格局和地下水的径流及转换方式，控制着含水层介质发育和地下水补径排分布的特征，进而可将研究区细分为4个特征各异的小尺度岩溶水系统。小扑隧洞不同段穿越的岩溶水系统特征差异较大，隧洞涌水经历的水文地球化学作用过程不尽相同，综合认为隧洞1#洞段涌水来源于暗河管道，2#洞段涌水为揭露岩溶裂隙所致，补给高程分别为2 165.4 m和2 234.69 m，并初步确定各自的充水水源补给范围。研究结果可为后续隧洞防排水工程方案设计以及突涌水灾害防治提供依据。
- 紧窄单斜构造 /
- 岩溶水系统 /
- 水化学特征 /
- 涌水条件
Abstract: The southwest China is covered by large areas of carbonate rock strata, in which the movement of many terranes results in strong folds and rock fractures. The spatial structure diversity of strata and tectonics has formed various complex and distinctive karst water systems. Therefore, tunnels for traffic lines and water diversion projects are often built in southwest China, but when tunnels cross karst water systems, the tunnel inflow conditions are difficult to be identified due to the complexity of water inflow, which has been a challenge in tunnel construction projects. In the Xiaopu tunnel area of the central Yunnan Province, linear extension and closely interbedded soluble and non-soluble rock strata are developed, forming a typical tight-narrow monoclinic karst water system. Since the tunnel construction, the water inrush has respectively occurred in Section 1 and Section 2 with large and long-lasting water inflow. The complexity of the water inflow brings a great challenge for the tunnel construction. Therefore, it is urgent to find out the source and mode of water inflow in Xiaopu tunnel. Focusing on specific engineering problems, this study carefully sorts out the controlling factors of the characteristics of the tight-narrow monoclinic karst water system in Xiaopu tunnel. The division of the karst water system is reduced to a small scale, and the water inflow conditions of the tunnel are identified according to the groundwater monitoring data as well as the inflow conditions such as the hydrochemical characteristics and hydrogen and oxygen isotopes of water inflow.The results show that the tight-narrow monoclinic structure affects the spatial pattern of karst development, the runoff and the transformation mode of groundwater. This structure also controls the characteristics of aquifer media development and groundwater recharge, runoff and discharge distribution. Hence, the study area can be subdivided into four small-scale karst water systems with different characteristics, i.e., the bare-covered fissure flow and conduit flow with concentrated discharge, bare conduit flow with concentrated discharge, the bare-covered fissure flow with multiplex discharge, and the bare fissure flow with concentrated discharge. The hydrochemical type of groundwater in the Duimen-Daliyuan-Niuliancun karst water system, which is crossed by the Section 1 of Xiaopu tunnel, is mainly HCO₃·SO₄-Ca·Mg. And the concentration of Ba²⁺ in groundwater is higher than that in other karst water systems due to the dissolution of barite minerals in the strata of the Weining group of the middle Carboniferous and the upper Devonian. The hydrochemical type of groundwater in the Piantoushan-Lunacun-Jinxiandong karst water system crossed by Section 2 is HCO₃-Ca·Mg, indicating relatively pure karst water. This shows that dolomite dissolution is the main hydrochemical process for controlling water quality. Due to the slow flow of the karstic fracture network, the groundwater has a long residence time in the runoff path, and the water-rock interaction and evaporation are relatively strong, thus the heavy hydrogen and oxygen isotopes are more enriched. Huge differences in hydrogen and oxygen isotope composition also rule out the possibility of surface water flooding into the tunnel. It is concluded that the water inflow in Section 1 is caused by the uncovering of the underground conduit and the interception of the discharge spring of the shallow karst downstream. The karst conduit developed in the contact zone of igneous rock constitutes the main water inflow channel, in which the groundwater in the conduit is the water source with a recharge elevation of 2,165.4 m, mainly located in the karst depression in the north of Wangjiawan. The water inflow in Section 2 is caused by the exposure of karst fissures. The fissure network constitutes the main water flow passage, and the groundwater in Dengying formation is the water source, with a recharge elevation of 2,234.6 m, mainly located in the slope area on the north ridge of Piantou mountain.The groundwater in different karst water systems has experienced different water-rock interaction and evaporation processes. Therefore, the hydrochemistry and stable hydrogen and oxygen isotopes of groundwater are good natural tracers for tracing the source of water inflows in tunnels crossing different karst water systems. Comprehensive utilization of multiple approaches and information verification can improve the accuracy of identifying tunnel water inflow conditions, which may provide a basis for the subsequent design of tunnel drainage projects and the prevention of water inrush disasters in the tunnel.
- tight-narrow monoclinic structure /
- karst water system /
- hydrochemical characteristics /
- tunnel inflow conditions

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图 1 研究区水文地质略图及小扑隧洞位置

Figure 1. Sketch map of hydrogeology and location of Xiaopu tunnel in the study area

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图 2 滇中典型紧窄单斜岩溶水系统结构示意图

a-裸露–覆盖隙–管流集中排泄型 b-裸露管流集中排泄型 c-裸露–覆盖隙流复合排泄型 d-裸露隙流集中排泄型

Figure 2. Schematic diagram of the typical tight-narrow monoclinic karst water system in central Yunnan Province

a.bare-covered fissure flow and conduit flow with concentrated discharge, b.bare conduit flow with concentrated discharge, c.bare-covered fissure flow with multiplex discharge, d.bare fissure flow with concentrated discharge

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图 3 小扑隧洞沿线水文地质剖面图

Figure 3. Hydrogeological profile along Xiaopu tunnel

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图 4 a-地下水中Ba²⁺质量浓度沿地下水流向变化曲线，b-小扑隧洞涌水δD-δ¹⁸O关系图

N- 对门－大梨园－牛恋村岩溶水系统 J-偏头山－鲁纳村－金线洞岩溶水系统 W- 王家湾－青菜村－干硐村岩溶水系统 L- 三印村－龙潭村岩溶水系统

Figure 4. a-Variation curves of mass concentration of Ba²⁺ in the groundwater flow direction; b-Plot of δD-δ¹⁸O in water inflow of Xiaopu tunnel

N.Duimen-Daliyuan-Niuliancun karst water system; J.Piantoushan-Lunacun-Jinxiandong karst water system; W. Wangjiawan-Qingcaicun-Gandongcun karst water system; L. Sanyincun-Longtancun karst water system

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表 1 紧窄单斜小尺度岩溶水系统特征

Table 1. Characteristics of the tight-narrow monoclinic karst water system at a small scale

岩溶水系统名称		对门－大梨园－牛恋村	王家湾－青菜村－干硐村	偏头山－鲁纳村－金线洞	三印村－龙潭村
特征		裸露-覆盖隙-管流集中排泄型	裸露管流集中排泄型	裸露-覆盖隙流复合排泄型	裸露隙流集中排泄型
岩溶含水系统	含水岩组	二叠系阳新组、泥盆系－石炭系、震旦系灯影组	二叠系阳新组、泥盆系－石炭系	震旦系灯影组、陡山沱组
	含水介质	溶隙、溶管	溶管	裂隙、溶隙
	空间结构	单斜、陡倾
岩溶水流系统	补给方式	集中贯入		分散入渗
	补给特点	量大、集中、迅速		连续、面广
	径流方式	顺岩层走向集中流		顺岩层走向散流	四周散流
	径流面积	25.6 km²	15 km²	23.4 km²	13.9 km²
	排泄方式	集中排泄		集中排泄和湖盆排泄带分散排泄	集中排泄
	排泄高程	1 886~1 932 m	2 149 m	1 890 m	2 105~2 114 m
	泉成因	溢流	溢流	侵蚀	溢流、侵蚀
	动态特征	季节性、水文响应快		水量稳定、水文响应滞后
岩溶水系统边界		岩性界线、分水岭、滇池南岸	岩性界线、分水岭	岩性界线、分水岭、滇池南岸	岩性界线、分水岭

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表 2 小扑隧洞区水样的水化学测试结果

Table 2. Hydrogeological test results of water samples in Xiaopu tunnel area

编号	取样位置	Ca²⁺	Mg²⁺	Ba²⁺	${\rm{HCO}}_3^{-}$	TDS	舒卡列夫水化学分类
编号	取样位置	mg·L⁻¹					舒卡列夫水化学分类
N1	对门－大梨园－牛恋村岩溶水系统	7.67	3.71	0.001 9	18.3	32	HCO₃·SO₄-Ca·Mg·Na
N2		31.65	10.48	0.007 6	48.8	100	HCO₃-Ca·Mg
N3		143.50	36.19	0.060 0	97.6	385	HCO₃·SO₄-Ca·Mg
J1	偏头山－鲁纳村－金线洞岩溶水系统	10.80	2.46	0.003 3	115.9	222	HCO₃-Ca·Na
W1	王家湾－青菜村－干硐村岩溶水系统	12.01	4.87	0.012 6	30.5	45	HCO₃·SO₄-Ca·Mg
W2		13.40	8.26	0.003 7	18.3	59	HCO₃·SO₄·Cl-Mg·Ca
W3		−	14.99	0.040 1	−	−	−
W4		43.90	19.33	0.112 2	79.3	147	HCO₃·SO₄-Ca·Mg
L1	三印村－龙潭村岩溶水系统	55.39	20.26	0.003 6	134.2	208	HCO₃-Ca·Mg
L2	三印村－龙潭村岩溶水系统	13.49	1.04	0.004 0	51.3	102	HCO₃-Ca
SD1	1#洞段涌水	51.26	18.22	0.018 5	81.8	172	HCO₃·SO₄-Ca·Mg
SD2	2#洞段涌水	40.34	18.92	0.006 2	85.4	134	HCO₃-Ca·Mg
注：“−”未检测。 Note: "−" Not detect.

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表 3 隧洞涌水补给高程计算结果

Table 3. Calculation results of the recharge elevation of tunnel water inflow

项目	δD_VSMOW/‰	δ¹⁸O_VSMOW/‰	推算补给高程/m
1#洞段涌水	−87.12	−11.8	2165.4
2#洞段涌水	−89.05	−11.98	2234.6

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