Characterization of karst development and groundwater circulation in the middle part of the Jinshajiang fault zone
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摘要:
金沙江断裂带中段碳酸盐岩分布区水文地质结构复杂、岩溶水量丰富, 是工程地质安全的重要威胁之一。文章在岩溶地貌和水文地质调查的基础上, 采用水化学和新型同位素测年与示踪的方法, 研究了金沙江断裂带中段岩溶发育特征, 分析了岩溶水补给、径流和排泄过程。结果表明: 岩溶空间分布和地下水补给、径流、排泄均受构造控制; 在垂向上主要存在3个高程级别的岩溶发育分区, 其中二级和三级顶部岩溶的发育时间分别为晚中新世至晚更新世和上新世至晚更新世; 岩溶水补给区海拔4400~4600 m, 主要补给源为大气降水和冰湖水, 水中228Ra/226Ra数据显示非定曲断裂控制范围内水源难以形成跨断裂影响范围的补给; 岩溶水循环速度快, 岩溶大泉的85Kr年龄＜15 a, 且基本没有年龄较大的地下水混合; 径流过程中碳酸盐岩溶蚀和阳离子交换作用不充分。在工程中应充分考虑活动断裂影响下岩溶水径流通道空间分布、高水压影响和特殊天气条件带来的地质灾害威胁。
Abstract:The complex hydrogeological structure and abundant karst water in the carbonate rock distribution area in the Jinshajiang fault zone's middle section are essential threats to engineering safety. Based on karst landform and hydrogeological investigations, the article presents the karst development characteristics in the Jinshajiang fault zone's middle section, and analyzes the recharge source, runoff process, and discharge characteristics of karst water using the methods of hydrochemical and new isotopic dating and tracing. The results show that structures control the spatial distribution of karst and the groundwater circulation in the study area. There are mainly three elevation-level karst development zones in the vertical direction. The development time of the second elevation-level karst is from the late Miocene to the late Pleistocene, and the top of the third elevation-level karst is from the Pliocene to the late Pleistocene. The karst water recharge area is at an elevation of 4400~4600 m. The primary recharge sources are atmospheric precipitation and glacial lake water. The 228Ra/226Ra data in the water shows that it is difficult for water sources under the control of a non-fixed-curvature fault to form recharge across the affected area of the fault. The karst water circulates fast, the 85Kr age of the karst spring is < 15 a, and there is basically no older groundwater mixing. Carbonate rock dissolution and cation exchange are not sufficient during groundwater runoff. In the engineering project, the spatial distribution of karst water runoff channels under the control of active faults, the influence of high-water-pressure and the threat of geological disasters caused by special weather conditions should be fully considered.
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图 2 水体中Ra和85Kr采样照片
a—Ra同位素采集与富集；b—85Kr样品采集
Figure 2. Photos of Ra and 85Kr sampling
(a) Ra isotopes sampling; (b) 85Kr sampling
图 3 研究区不同高程的岩溶地貌
a—第一级岩溶，溶洞，海拔约5000 m；b—第二级岩溶，溶洞(样品编号H19)，海拔约4050 m；c—第三级岩溶，溶洞(样品编号H60)，海拔约3600 m；d—波密泉(样品编号BM)，海拔约3550 m；e—根久泉(样品编号GJ；据马剑飞等，2022a修改)，海拔约3450 m；f—定曲泉(样品编号LB)，海拔约3670 m
Figure 3. Karst landforms at different elevations in the study area
(a) The first-elevation-level krast (Krast cave at 5000 m); (b) The second-elevation-level (Krast cave at 4050 m; Sample H19); (c) The third-elevation-level (Krast cave at 3600 m; Sample H60); (d) The Bomi Spring at 3550 m (Sample BM); (e) The Genjiw Spring at 3450 m (Sample GJ; Modified from Ma et al., 2022b); (f) The Dingqu Spring at 3670 m (Sample LB)
图 5 水样226Ra和228Ra与盐度的关系及226Ra与228Ra的关系图
a—盐度/226Ra；b—盐度/228Ra；c—228Ra/226Ra
Figure 5. 226Ra and 228Ra vesus salinity and 226Ra vesus 228Ra
(a) Salinity vesus 226Ra; (b) Salinity vesus 228Ra; (c) 228Ra vesus 226Ra
图 6 研究区水体中离子关系图
Figure 6. The relationship between ions in the water from the study area
a—(Ca2+/Na+)/(HCO3-/Na+); b—(Na++K+-Cl-)/(Ca2++Mg2+-HCO3--SO42-)
图 7 水样T值与TDS和85Kr关系图
a—水样TDS与氚值(T)关系；b—岩溶泉85Kr活度与氚值(T)关系(图中虚线表示根据基于延迟输入函数的活塞流模型计算出的过去几十年的混合分数，实线表示年轻水占50%和99%时的模型计算值；Avrahamov et al., 2018)
Figure 7. T value vesus TDS value and 85Kr value in the water sample
(a) TDS value vesus T value in the water sample; (b) 85Kr value vesus T value in the karst springs The dashed lines are mixing lines between an old, T and 85Kr free component and groundwater of different ages. The solid lines are the calculated values by the model when the young water accounts for 50% and 99% based on Avrahamov et al., 2018.
图 8 研究区主要岩溶泉多期流量(GJ、BM部分数据源自Ma et al., 2022b)
Figure 8. Multi-flow of main karst springs in the study area (Parts of GJ, BM data are from Ma et al., 2022b)
表 1 不同高程次生方解石的230Th年龄
Table 1. 230Th age of secondary calcite at different elevations
样品编号 高程/m 230Th年龄/a BP H19 4050 36737±11667 H60 3600 14298±903 
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表 2 水化学和同位素测试结果
Table 2. Test results of hydrochemical components and isotopes
水体类型 数据项/样品编号* 水化学指标 同位素指标 TDS Ca2+ Mg2+ K+ Na+ Cl- SO42- HCO3- pH δD δ18O T /mg·L-1 /‰ /‰ TU 岩溶泉 最大值 207.00 54.83 10.86 0.91 5.75 0.30 9.15 223.50 7.89 -142.00 -18.90 4.70 最小值 90.00 22.06 7.44 0.16 0.25 0.17 1.35 102.80 7.71 -146.00 -19.50 4.20 平均值 162.50 42.67 9.66 0.58 3.31 0.22 6.91 175.85 7.82 -143.25 -19.08 4.40 变异系数 0.31 0.33 0.16 0.54 0.69 0.32 0.54 0.29 0.01 -0.01 -0.02 0.06 河水 最大值 251.00 68.62 11.83 1.50 3.35 1.05 91.31 138.90 8.16 -135.00 -17.90 7.00 最小值 52.00 10.65 0.84 0.58 1.61 ＜0.1 7.58 36.28 7.68 -142.00 -18.80 4.30 平均值 139.20 35.18 5.52 0.89 2.17 — 42.21 84.75 7.89 -138.80 -18.34 5.56 变异系数 0.67 0.73 0.83 0.41 0.31 — 0.94 0.57 0.02 -0.02 -0.02 0.23 湖水 Lake-1 69.00 18.39 2.83 0.51 0.97 0.10 6.08 66.45 7.35 -127.00 -16.60 8.10 Lake-2 9.00 1.37 0.10 0.08 0.25 0.15 < 0.20 12.08 7.44 降雨 4月降雨 9.00 1.31 0.18 0.17 0.33 0.21 0.30 12.08 7.70 -79.00 -10.00 10.00 9月降雨 15.00 1.79 0.22 0.08 0.33 1.40 2.00 12.02 6.74 积雪 积雪 10.00 2.11 0.05 0.08 0.09 0.35 1.50 11.42 7.38 -177.00 -24.10 7.20 “*”该列中岩溶泉和河水列出的为数据的统计值；湖水、降雨和积雪列出的为采样编号，其所在行的数据是样品的测试值
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表 3 岩溶泉补给高程计算值
Table 3. Calculated values of the karst water recharge elevation
岩溶泉编号 补给高程h/m δ18O=-0.0028h -3.93① δ18O=-0.0033h-4.29② δ18O=-0.0023h-10.011③ δD=-0.0195h-67.813③ δ18O=-0.0018h-6.86④ GJ 5346 4427 3865 3804 6689 LB 5561 4609 4126 4010 7022 JT 5382 4458 3908 3856 6744 BM 5346 4427 3865 3804 6689 注：①李维杰等，2018；来自川东、渝、滇、黔等四地监测数据；②姚檀栋等，2009；以青海、西藏监测台站为主；③张磊等，2021；来自道孚-康定-石棉-西昌数据；④于津生等，1980；来自渝、黔、川、藏东等地数据
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表 4 研究区主要水体226Ra和228Ra活度
Table 4. 226Ra and 228Ra activity in the water samples from the study area
水样编号 226Ra活度/dpm·100 L-1 228Ra活度/dpm·100 L-1 228Ra/226Ra GJ 6.27±1.07 7.18±2.38 0.91 BM 8.75±1.06 7.00±1.97 3.07 LB 7.56±0.98 4.28±1.91 0.80 Lake-1 3.95±0.78 5.27±1.97 0.57 Lake-2 9.57±1.11 29.42±2.70 1.34 定曲-2 14.95±1.16 13.56±2.13 1.14
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