Analysis of groundwater runoff patterns in Zhangguan-Paihuadong karst water system in the south of the Mingyue gorge anticline
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摘要:
川东明月峡背斜地下岩溶发育的强烈非均质性造就了独特的地下水径流模式，孕育出区域复杂的岩溶工程水文地质问题，查明明月峡背斜南段地下水径流模式对指导区内隧道工程选址及建设具有重要意义。文章在已有研究基础上，以“张关—排花洞”岩溶水系统为研究区，通过系统厘清区内水文地质条件，深入剖析区内地下水水文地球化学特征及水动力条件，明确区内岩溶含水介质不均一性控制下的地下水小尺度径流规律。结果显示：研究区地下水在平面上表现为形似“扫帚状”的径流模式：在补给、径流区，三叠系下统嘉陵江组一段（T1j1）、嘉陵江组三段(T1j3)地层（强岩溶化）与嘉陵江组二段（T1j2）、嘉陵江组四段 （T1j4）地层（弱岩溶化）呈间互状分布的特点导致相邻地层之间水力联系较弱，以地层为单位形成多个相对独立的岩溶水子系统；在研究区排泄区，受控于势汇最强的T1j3内部管道流对其他地层地下水持续的袭夺效应，地下水统一汇聚至排花洞暗河出口向御临河排泄，各岩溶水子系统最终整合为一个岩溶水系统。
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关键词:
- 川东褶皱带 /
- 明月峡背斜 /
- 张关—排花洞岩溶水系统 /
- 地下水径流模式 /
- 小尺度
Abstract:The long-term interaction between groundwater and karst development in eastern Sichuan has created a unique groundwater runoff pattern and caused a complex hydrogeological problem of karst engineering. Hence, finding out the groundwater runoff pattern in the southern section of Mingyue gorge anticline is of great significance for guiding the site selection and construction of tunnel engineering in this area.
Based on previous studies, hydrogeological conditions of the study area are systematically sorted out. Mingyue gorge anticline is a typical closed one in eastern Sichuan, and there is no fault in the area. Atmospheric rainfall is the main recharge source in the water system. Controlled by the boundary of the non-soluble rock formation on the two sides of anticline and topographic relief, groundwater converges and is recharged through the karst structures such as depressions and sinkholes, flowing toward the river runoff at the lowest discharge datum along the tectonic line within the region. The outlet of S05 (Paihuadong), exposed on the bank slope of Yulin river, is a main discharge point of groundwater in the system. The discharge is about 365 L·s-1 in the dry season, accounting for 95.94% of the total discharge of all natural groundwater outcrops in the study area. Main aquifers in the area are composed of carbonate rocks of Jialingjiang formation and Leikoupo formation. The lithology of T1j1 and T1j3 is mainly limestone, while the lithology of T1j2 , T1j4 and T2lis mainly dolomite. The difference of rock solubility results in different karst development in each aquifer. From the perspective of surface karst phenomenon, the area of depression and the number of falling holes developed in T1j1 and T1j3 strata respectively account for 67.38% and 69.84% of the total amount of the system. From the perspective of underground karst phenomenon, 121 karst caves have been revealed by 22 boreholes in the study area. The number of karst caves distributed in T1j1 and T1j3 strata accounts for 75.8% of the total. Statistical results of surface and underground karst phenomenon reflect that the degrees of karst in T1j1 and T1j3 strata is significantly higher than those in T1j2 , T1j4 and T2l strata. Because aquifers with different degrees of karstic distribution are intersectional in the plane, the heterogeneity of water-bearing media leads to relatively weak hydraulic connection in adjacent strata, and the groundwater level revealed by boreholes and spring points is obviously different in different layers.
Results of hydrochemical analysis of 18 groups of water samples in the study area further illustrate the discontinuity of groundwater in each aquifer. HCO3-Ca type water mainly exists in T1j1 and T1j3 strata. Their conventional hydrochemical and isotope characteristics indicate that the water-rock interaction time is relatively short. Hydrochemical types of T1j2, T1j4and T2lstrata are mainly HCO3·SO4-Ca and HCO3·SO4-Ca·Mg. Their conventional hydrochemical and isotope characteristics indicate that the water-rock interaction time is relatively long, and the hydrochemical characteristics of groundwater outcrop in strong and weak karstified strata are obviously different. From the hydrogeological profile of S01 (Zhangjiadong) to S05 (Bahuadong), the hydrochemical types of water samples S01 and ZK07 in the recharge and runoff area of the system are HCO3-Ca type, and the hydrochemical characteristics of the two are very similar. When sampling sites are located within a drainage area of the system, the hydrochemical type of groundwater near sampling sites ZK10 and S05 is changed to HCO3·SO4-Ca type, and corresponding TDS values are significantly higher than those of recharge and runoff area, indicating that groundwater in different aquifers is mixed in the system discharge area.
Based on the analysis of karst hydrogeological conditions and hydrogeochemical characteristics in the study area, a runoff law of groundwater in Zhangguan-Paihuadong karst water system is summarized (groundwater in the study area generally shows a broom-like runoff pattern). In system recharge and runoff areas, a hydraulic connection between aquifers is not strong. Multiple groundwater flow systems have formed with the stratum as a unit, and groundwater carries out relatively independent bedding runoff in each layer. In the drainage area of the system, the mutual capture of each water flow system is increasingly strong. Hence, these water flow systems gradually merge into one, discharging to Yulin river through the drainage hole. In addition, according to previous research, groundwater inside the system vertically presents a multi-order nested flow system. Controlled by the discharge datum of different cutting depths, this system is successively developed into local flow system, intermediate flow system and regional flow system from the shallow part to the deep.
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表 2 钻孔及泉点揭示的各地层内部地下水水位统计表
Table 2. Statistical table of the groundwater level in each layer revealed by boreholes and spring points
水点编号 ZK05 ZK07 ZK04 S09 S10 地下水水位/m 395.55 497.99 404.14 498.96 526.98 揭露（出露）地层 T1j1 T1j2 T1j3 T1j4 T2l 
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表 1 研究区地表岩溶形态分布特征
Table 1. Distribution characteristics of the surface karst morphology in the study area
地层 洼地 落水洞 面积/km2 面积比/% 数量 数量比/% T2l 0.12 2.16 0 0 T1j4 0.93 16.76 11 17.46 T1j3 2.16 38.92 28 44.44 T1j2 0.76 13.69 8 12.70 T1j1 1.58 28.47 16 25.40
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表 3 研究区取样点信息
Table 3. Information of sampling sites in the study area
样品编号 取样层位 经度 纬度 采样高程/m 矿化度/mg·L−1 地貌位置 S01 T1j1 106.9077° 29.7693° 507 290 补给、径流区 S03 T1j2 106.8965° 29.7563° 507 300 补给、径流区 S04 T1j2 106.9151° 29.7709° 501 325 补给、径流区 S05 T1j2 106.8451° 29.6625° 218 388 排泄区 S06 T1j3 106.8900° 29.7533° 507 325 补给、径流区 S07 T1j4 106.9162° 29.8035° 539 298 补给、径流区 S08 T1j4 106.9197° 29.8145° 547 315 补给、径流区 ZK01 T1j1 106.8873° 29.7279° 422 365 补给、径流区 ZK02 T1j3 106.8921° 29.7257° 422 372 补给、径流区 ZK03 T1j3 106.8773° 29.7248° 250 276 补给、径流区 ZK04 T1j3 106.8924° 29.7355° 443 446 补给、径流区 ZK05 T1j1 106.8801° 29.7244° 398 432 补给、径流区 ZK06 T1j1 106.8825° 29.7228° 270 464 补给、径流区 ZK07 T1j1 106.8845° 29.7197° 338 327 补给、径流区 ZK08 T1j3 106.8637° 29.7043° 160 422 排泄区 ZK09 T1j3 106.8666° 29.7038° 200 310 补给、径流区 ZK10 T1j2 106.8639° 29.7132° 271 340 排泄区 ZK11 T1j3 106.8863° 29.7381° 482 362 补给、径流区
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