Distribution and influencing factors of karst underground rivers in the Pearl River Basin
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摘要: 珠江流域岩溶地下河枯季流量约4 738.69万m3·d−1，赋存丰富的地下水资源，探讨地下河分布和发育特征对我国南方岩溶水资源的开发利用具有重要的指导意义。文章以西南岩溶区大量的野外调查工作为基础，结合珠江流域内1∶20万水文地质普查报告，选择348组岩石样品和1 036条岩溶地下河，从岩性、地形地貌、构造、水动力条件和新构造运动等角度总结分析珠江流域地下河发育规律、分布特征及其影响因素。结果表明：地下河在比溶解度介于0.84~1.2的细粒−鲕粒生物碎屑纯灰岩中最为发育，在比溶解度介于0.43~0.61的泥质灰岩中发育较弱。根据地下河形态及水循环演化条件，将地下河分为发育初期单管型、发育多期羽毛型、新构造控制网络型、发育成熟期树枝型4种类型。地形地貌和地表河网决定岩溶地下河运动的趋势和方向；构造控制地下河发育的空间格局，其中构造反接复合部位、压扭性断裂两侧破碎带、与非可溶岩接触带、褶皱弯曲最大部位、背斜轴部破碎带和向斜轴部地下河发育尤为明显；水动力特征影响地下河发育规模和发育深度；新构造运动促进地下河发育向深性、继承性、新生性发展。Abstract: The Pearl River Basin is the area of first-class water resources at the southernmost end of China. Its geographical location is 102°14′-115°57′ E and 21°35′-26°50′N. The main stream of the Pearl River, with a total length of 2,214 km, flows through Yunnan, Guizhou, Guangxi and Guangdong. The total area of the Pearl River Basin is about 438,100 km2, including Nanbeipan river, Hongliu river, Yujiang river, Xijiang river, Beijiang river, the Pearl River Delta and the dongjiang river basin. The water-bearing rocks in the Pearl River Basin are divided into karst water of carbonate rock, fissure water of clastic rock, pore water of loose rock and fissure water of magmatic rock. The distribution area of exposed carbonate rocks is about 149,500 km2, and that of buried carbonate rocks is about 39,600 km2, accounting for 43.16% of the total area. Because there are 1,036 karst underground rivers, and the discharge of karst underground rivers of the Pearl River Basin in the dry season is about 47.39 million m3·d−1. the basin is rich in groundwater resources. Therefore, it is of great significance to explore the distribution and karstification characteristics of underground rivers for the exploitation and utilization of karst water resources in southern China. Based on a large number of field investigations in the southwest karst area, 200,000 hydrogeological survey reports and the 1∶250,000 and 1∶50,000 karst hydrogeological surveys conducted from 2003 to 2016 in the Pearl River Basin, we selected 348 groups of rock samples and 1,036 karst underground rivers as study objects. Then, taking Dalongtan and Sanqiutian underground rivers in Yunnan Province, Sixiaojing, Tianshengqiao and Huachu underground rivers in Guizhou Province, and Disu, Zhaidi and Dizhou underground rivers in Guangxi as examples, we analyzed and summarized the development law, distribution characteristics and influencing factors of underground rivers in the Pearl River Basin from the perspectives of lithology, landform, structure, hydrodynamic conditions and neotectonic movement. According to the analysis, the outlets of 310 underground river are at an elevation between 200-400 m, accounting for the largest proportion. Among them, more than 30 underground rivers, mainly located in the river basins of Hongliu river, Yuhe river, South Panjiang river and north Panjiang river, respectively cover a catchment area greater than 200 km2. Their discharge in the dry season is greater than 1,000 L·s−1 and the length of main pipeline is greater than 10 km. The study result shows that the underground river is most developed in fine-grained oolitic bioclastic pure limestone with a specific solubility of 0.84-1.2, moderately developed in dolomite with a specific solubility of 0.62-0.83, and weakly developed in argillaceous limestone with a specific solubility of 0.43-0.61. Landform and surface river network determine the trend and direction of karst underground river movement. The structure controls the spatial pattern of underground river development. The development of underground river is particularly obvious in the reverse composite part of the structure, the fracture zone on both sides of the compressional torsional fault, the contact zone with the non-soluble rock, the part with the largest fold bending, and the fracture zone in the anticline axis and the syncline axis. Hydrodynamic characteristics affect the development scale and depth of underground rivers. The neotectonic movement facilitates the constant changes of cycle and alternation conditions of groundwater, as well as the deep, inherited and new development of underground rivers. Finally, according to the morphology of underground river and the evolution conditions of water circulation, the underground river can be divided into four types: single conduit type at the initial stage of development, multi-stage feather type, neotectonic control network type and mature dendritic type. All in all, this study is expected to provide data support for the exploitation and utilization of karst underground rivers, monitoring and evaluation of water resources, and the selection of backup water sources to meet urban emergency in the Pearl River Basin.
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图 1 珠江流域含水岩组及二级分区
Figure 1. Aquifer characteristics and secondary watershed boundary of the Pearl River Basin
图 4 珠江流域大型地下河分布
Figure 4. Distribution of large underground rivers in the Pearl River Basin
图 11 河间地块地下河展布
Figure 11. Distribution of karst underground river in the inter-river land mass
图 12 构造对大小井地下河分布的控制作用（修改自罗甸幅1∶20万水文地质普查报告）
Figure 12. Controlling Effect of geological structure on the distribution of Daxiaojing Underground Rivers
图 13 构造对地苏地下河分布的控制作用
Figure 13. The controlling effect of structure on the distribution of Disu underground rivers
图 15 豪猪岩至东究岩溶管道形态示意图（据中英探险资料修改）
Figure 15. Schematic diagram of karst conduit form from Haozhuyan to Dongju in Zhaidi underground river (modified according to Sino-British exploration materials)
图 16 寨底地下河流域北部地表水地下水分水岭
Figure 16. Watershed of surface water and groundwater in the north of Zhaidi underground river basin
图 17 新构造运动促进地下河的发展
Figure 17. Distribution of karst underground river in the inter-river land
表 1 各二级流域岩溶地下河发育情况
Table 1. Development of karst underground rivers in each secondary watershed
二级
流域裸露型碳酸盐岩
面积/万km2占流域面
积比例/%岩溶地下
河条数密度/
条·100 km−2南北盘江 5.30 64.09 173 0.33 红柳江 5.90 52.07 440 0.75 郁江 2.06 26.44 216 1.05 西江 0.65 9.79 96 1.48 北江 1.04 22.27 111 1.07 合计 14.95 38.63 1036 0.69 
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表 2 大型地下河发育特征表
Table 2. Development characteristics of large underground rivers
代码 地下河名称 出口位置 主管道长
度/km分布方向 地下河支流
数/个汇水面
积/km2枯季流
量/m3·s−1主要含水
岩组UGR1 六郎洞 云南丘北县 15.00 NE 2 2 064.00 10.50 T2g UGR2 水源洞 广西凌云县 80.30 SW 5 667.18 9.74 D2t UGR3 洛帆 贵州册亨县 11.25 SE 3 339.00 8.43 P1m UGR4 外孟塘 贵州荔波县 15.00 SE 2 1 418.80 6.60 P1m UGR5 谷 布 广西田阳区 19.20 NE 5 611.19 5.78 D3r UGR6 坡心－坡月 广西巴马瑶族自治县 47.30 SE 11 852.44 5.75 D2t UGR7 地 苏 广西都安瑶族自治县 55.90 SE 12 1 128.00 4.86 D3d-e UGR8 大小井 贵州罗甸县 35.00 SE 7 1 855.70 4.73 T1d UGR9 盘溪 云南弥勒市 13.75 NE 2 744.80 3.33 Dx UGR10 小七孔 贵州荔波县 20.00 SE 2 337.30 3.23 P1q-m UGR11 拉 浪 广西宜州区 20.90 SE转NE 7 221.20 3.00 C2d-h UGR12 定 业 广西那坡县 26.60 NNW 4 423.52 2.73 D1y UGR13 作 登 广西田东县 76.00 SEE转NE 4 1 409.05 2.16 D3r、C1yt UGR14 百 朗 广西乐业县 63.00 N 13 600.03 2.14 CPm UGR15 索 潭 广西都安瑶族自治县 31.20 N转NW 6 226.31 2.13 C2h、P1q UGR16 坡 雷 广西田东县 16.70 NE 2 377.37 1.79 D3r、CPm UGR17 鸡 叫 广西忻城县 28.80 SW 3 327.81 1.79 CPm、P1q UGR18 沙锅 贵州镇宁布依族苗族自治县 23.75 SW 4 480.20 1.70 T2f UGR19 东里－板文 广西东兰县 37.40 E 5 502.29 1.48 C1-2d UGR20 龙临－头布 广西靖西市 28.20 SE 3 320.81 1.46 D3r UGR21 录峒－鹅泉 广西靖西市 22.00 SE 2 226.95 1.40 D3r UGR22 哑口寨 贵州镇宁布依族苗族自治县 12.50 NE 5 252.20 1.36 P1m、P2w UGR23 布泉－大龙潭 广西隆安县 54.80 E 10 1 347.14 1.35 D3r UGR24 中 旧 广西都安瑶族自治县 35.90 SE 6 369.44 1.30 CPm、P1q UGR25 坝纳 贵州平塘县 17.50 NW 5 455.20 1.20 P1 UGR26 下 末 广西鹿寨县 20.00 S 3 463.60 1.20 D3g、C1h UGR27 石 牌 广西来宾市 23.00 SE转NEE 3 221.44 1.14 C1d、P1q UGR28 模 范 广西田东县 20.50 SE转NE 3 210.21 1.06 D3r、C1d UGR29 大龙洞 广西上林县 24.00 N转SSE 4 437.65 1.03 D2t、D3g UGR30 古 蓬 广西忻城县 17.00 NW转E 2 213.68 1.01 CPm、P1q
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表 3 不同岩性化学成份及比溶解度对比
Table 3. Comparison of chemical composition and specific solubility of different lithologies
发育强弱 主要岩性结构 化学成份/% 比溶解度 CaO MgO 地下河发育强 细粒−鲕粒生物碎屑纯灰岩 52.58~56.03 0.08~1.62 0.84−1.20 地下河发育中等 微粒白云质灰岩 30.77~52.14 0.31~7.68 0.62~0.83 地下河发育弱 含泥质−燧石灰岩、细粒−中粒白云岩 30.72~34.84 10.94~21.11 0.43~0.61 无发育 非碳酸盐岩（粉砂岩） 1.15~3.33 0.12~2.14 /
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