水化学和同位素揭示的甘肃平凉岩溶水成因机制研究

张成文; 郑灏帆; 何剑波; 刘子龙; 毛绪美

doi:10.11932/karst2025y015

水化学和同位素揭示的甘肃平凉岩溶水成因机制研究

doi: 10.11932/karst2025y015

张成文^{1, 2,},
郑灏帆³,
何剑波^{1, 2},
刘子龙³,
毛绪美^3, ,

1.
甘肃省地下水工程及地热资源重点实验室, 甘肃兰州 730050
2.
甘肃省地质矿产勘查开发局水文地质工程地质勘察院, 甘肃张掖 734000
3.
中国地质大学(武汉)环境学院, 湖北武汉 430074

基金项目: 基金项目

详细信息

作者简介:
张成文（1989－），男，工程师，从事水文地质工作。E-mail：804682380@qq.com

通讯作者:
毛绪美（1977－），男，博士，副教授，从事水文地质学研究。E-mail：maoxumei@cug.edu.cn。

中图分类号: P314.2;P597
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- 文章访问数: 13
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- 被引次数: 0
出版历程
- 收稿日期: 2025-01-01
- 录用日期: 2025-03-06
- 修回日期: 2025-02-27
- 网络出版日期: 2025-08-20

Genetic mechanism of karst water revealed by hydrochemistry and isotopes in Pingliang, Gansu province

ZHANG Chengwen^{1, 2
,},
ZHENG Haofan³,
HE Jianbo^{1, 2},
LIU Zilong³,
MAO Xumei^{3
, ,}

1.
Key Laboratory of Groundwater Engineering and Geothermal Resources in Gansu Province, Lanzhou, 730050, Gansu, China
2.
Institute of Hydrogeology and Engineering Geology, Exploration and Development Bureau of Geology and Mineral Resources of Gansu Province, Zhangye 734000, Gansu, China
3.
School of Environment, China University of Geosciences (Wuhan), Wuhan 430074, Hubei, China

摘要

摘要: 岩溶水是平凉地区的重要水资源之一。探明岩溶水的形成机制对于该地区岩溶水资源的可持续利用、水源地保护以及环境保护措施的制定具有重要意义，为推动区域水资源的可持续发展和水环境健康提供了科学依据和理论支持。岩溶水的水化学成分可以揭示补给、径流和排泄过程，而同位素示踪方法则有助于指示岩溶水系统的范围和动态变化。因此，本研究通过水化学和同位素分析阐明了平凉地区岩溶水的成因机制。研究结果表明，该地区地下水主要可分为HCO₃-Ca型和HCO₃·SO₄-Na型两类。Spearman相关分析和离子比例系数分析表明，白云石、方解石和蒸发盐主导了平凉岩溶水的水化学形成。水文地质条件及氢氧同位素结果进一步证实，岩溶水主要来源于大气降水补给。基于岩溶水成因模型的识别，确定平凉地区存在两种岩溶水成因模式。尽管两者均接受来自山前的大气降水补给，并通过岩溶裂隙流经上覆地层进入含水层，但由于上覆地层的差异，导致水化学特征的不同。这表明，上覆地层中矿物溶解作用是平凉岩溶水化学成分形成的主要因素。
- 水化学 /
- 同位素 /
- 成因机制 /
- 岩溶水 /
- 平凉
Abstract: Karst water is one of the significant water resources in the Pingliang region. Investigating the formation mechanism of karst water is crucial for the sustainable utilization of karst water resources, the protection of water sources, and the formulation of environmental protection measures in the area. It provides a scientific basis and theoretical support for promoting the sustainable development of regional water resources and the health of the water environment. The hydrochemical composition of karst water can reveal the processes of recharge, runoff, and discharge, while isotopic tracing methods help indicate the scope and dynamic changes of the karst water system. To uncover the genetic mechanism of karst water in Pingliang City, we comprehensively analyzed the hydrochemical characteristics and sources of karst water in Pingliang City using methods such as Piper trilinear diagrams, mathematical approaches, and ion ratio coefficients. The research results indicate that the groundwater in the region can be mainly divided into two types: HCO₃-Ca and HCO₃·SO₄-Na, with Ca²⁺ and Na⁺ as the primary cations and ${\rm{HCO}}_3^{-}$ as the primary anion. The pH value ranges from 6.72 to 6.9, exhibiting weakly alkaline hydrochemical characteristics overall. The total dissolved solids (TDS) value of groundwater ranges from 158.01 mg·L⁻¹ to 1519.40 mg·L⁻¹. Spearman correlation analysis shows that the hydrochemistry of karst water in the study area is primarily controlled by the dissolution of minerals such as dolomite and evaporites. TDS is highly positively correlated with the contents of Na⁺, Mg²⁺, Cl⁻, ${\rm{SO}}_4^{2-}$, and ${\rm{HCO}}_3^{-}$. Additionally, the content of Mg²⁺ is significantly positively correlated with the contents of the main anions Cl⁻, ${\rm{SO}}_4^{2-}$, and ${\rm{HCO}}_3^{-}$ (r > 0.7, p < 0.01), and the content of Na⁺ also has a significant positive correlation with the contents of Cl⁻ and ${\rm{SO}}_4^{2-}$ (r > 0.98, p < 0.01). In the analysis of ion proportional coefficients, the hydrochemical characteristics of karst water in Pingliang City are mainly influenced by rock weathering. Na⁺ not only originates from the dissolution of rock salt but may also come from the dissolution of sulfate or silicate minerals; Mg²⁺ is derived from the combined action of calcite and dolomite; Ca²⁺ is produced not only from the dissolution of dolomite but also from the dissolution of calcite and dolomite. During the rock weathering process, dolomite, calcite, and evaporites dominate the hydrochemical formation of Pingliang karst water. Gibbs diagram combined with mineral saturation index analysis further confirms that the dissolution of evaporites, carbonates, and silicate minerals is the natural source of hydrochemical components in Pingliang City. Ca²⁺, Mg²⁺, and ${\rm{HCO}}_3^{-}$ in the karst groundwater of Pingliang City mainly originate from the combined dissolution of calcite and dolomite. Hydrogeological conditions and hydrogen-oxygen isotope results show that δD values range from -75.45‰ to -64.80‰, with an average of -69.20‰; while δ¹⁸O values range from -11.26‰ to -9.16‰, with an average of -10.07‰, indicating that all groundwater is recharged by atmospheric precipitation infiltration. Based on the identification of the karst water genetic model, it is determined that there are two genetic modes of karst water in the Pingliang area. Mode 1: Atmospheric precipitation infiltrates through the overlying Quaternary loess layer, continuously dissolving sulfate minerals in the loess, and enters the limestone confined aquifer through karst fissures formed by faults, eventually emerging as springs at the interface between the loess and limestone aquifer. In this mode, the chemical type of karst water is mainly HCO₃·SO₄-Na. Mode 2: Atmospheric precipitation infiltrates through the overlying Quaternary sandstone layer, continuously dissolving carbonate minerals in the sandstone layer, and enters the limestone confined aquifer through karst fissures formed by faults, eventually emerging as springs at the interface between the sandstone and limestone aquifer. In this mode, the chemical type of karst water is mainly HCO₃-Ca. Although both modes receive atmospheric precipitation recharge from the front of the mountain and enter the aquifer through karst fissures through the overlying strata, the differences in the overlying strata lead to different hydrochemical characteristics. This indicates that the mineral dissolution in the overlying strata is the main factor in the formation of the hydrochemical composition of Pingliang karst water.
- hydrochemistry /
- isotopes /
- genetic mechanism /
- karst water /
- Pingliang region

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图 1 平凉地区地质简图

Figure 1. Schematic geological map of the Pingliang region

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图 2 Piper三线图

Figure 2. Piper Trilinear map

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图 3 阴阳离子关系图

Figure 3. Cation-Anion Relationship Diagram

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图 4 水化学Gibbs图

Figure 4. Hydrochemical Gibbs Diagram

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图 5 氢氧同位素关系图

Figure 5. Crisis Diagram of Hydrogen and Oxygen Isotopes

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图 6 岩溶水成因模型

Figure 6. Karst Water Genesis Model

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表 1 样品的水化学和同位素结果（mg∙L⁻¹）

Table 1. Hydrochemical and Isotope Results of Samples (mg∙L⁻¹)

样品编号	上覆地层岩性	采样日期	pH	Ca²⁺	Mg²⁺	Na⁺	K⁺	Cl⁻	${\rm{SO}}_4^{2-}$	Ba²⁺	${\rm{NO}}_3^{-}$	${\rm{HCO}}_3^{-}$	TDS	δ¹⁸O_V-SMOW	δD_V-SMOW	水质类型
样品编号	上覆地层岩性	采样日期	pH	/mg·L⁻¹										/‰		水质类型
LQ	砂岩	2024.07.24	7.17	70.34	27.17	22.23	0.89	6.66	14.24	0.051	3.55	378.79	334.85	−10.43	−71.16	HCO₃-Ca
K4	砂岩	2024.07.24	7.68	65.63	25.56	9.35	1.47	4.76	45.28	0.043	7.69	283.41	301.60	−11.26	−73.67	HCO₃-Ca
K5	砂岩	2024.07.24	7.42	64.94	30.93	16.25	1.85	6.40	38.92	0.018	6.66	333.69	332.98	−10.19	−67.88	HCO₃-Ca
EG1	砂岩	2024.07.24	7.44	54.39	23.95	60.72	1.19	10.89	28.49	0.036	7.69	386.87	381.12	−9.59	−68.95	HCO₃-Ca
BLMSK	砂岩	2024.07.25	7.22	96.59	49.50	55.12	1.32	22.26	60.93	0.048	25.60	552.21	587.89	−9.16	−68.51	HCO₃-Ca
GYD	黄土	2024.07.25	7.58	39.81	41.77	115.47	1.39	28.97	105.78	0.013	14.61	440.85	569.09	−10.29	−75.45	HCO₃·SO₄-Na
ZWC	砂岩	2024.07.25	7.41	82.30	28.15	47.13	2.24	29.95	78.18	0.040	20.45	350.54	464.01	−9.46	−66.32	HCO₃-Ca
YAC	砂岩	2024.07.26	7.46	65.88	6.48	3.97	0.48	6.00	22.59	0.012	25.61	180.39	221.37	−10.42	−70.03	HCO₃-Ca
XJS	砂岩	2024.07.26	7.44	63.00	20.54	5.80	0.67	2.53	10.05	0.027	2.38	293.01	251.65	−10.18	−68.25	HCO₃-Ca
MTC	砂岩	2024.07.26	8.20	41.64	9.90	4.10	1.32	1.83	14.19	0.029	0.95	168.13	158.01	−10.54	−67.33	HCO₃-Ca
YHX	砂岩	2024.07.26	8.15	50.12	13.35	11.19	2.51	7.17	26.09	0.035	14.67	194.09	222.23	−10.12	−68.41	HCO₃-Ca
MCC	砂岩	2024.07.26	7.39	88.00	11.79	16.63	1.26	12.38	29.40	0.042	1.48	314.09	318.05	−10.07	−68.85	HCO₃-Ca
WQZ	黄土	2024.07.26	7.57	57.67	65.39	413.73	2.83	117.36	372.71	0.084	45.28	886.84	1519.40	−9.24	−64.80	HCO₃·SO₄-Na

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表 2 水化学指标Spearman相关系数矩阵

Table 2. Spearman Correlation Coefficient Matrix of Hydrochemical Indicators

		pH	Ca²⁺	Mg²⁺	Na⁺	K⁺	Ba²⁺	Si²⁺	Cl⁻	${\rm{SO}}_4^{2-}$	F⁻	${\rm{NO}}_3^{-}$	${\rm{HCO}}_3^{-}$	TDS
pH	皮尔逊相关性	1
Ca²⁺		−0.672^*	1
Mg²⁺		−0.338	0.105	1
Na⁺		−0.054	−0.156	0.801^**	1
K⁺		0.351	−0.110	0.483	0.582^*	1
Ba²⁺		−0.137	0.280	0.597^*	0.691^**	0.520	1
Si²⁺		−0.368	0.321	0.338	0.195	0.232	0.384	1
Cl⁻		−0.080	−0.035	0.792^**	0.984^**	0.635^*	0.721^**	0.208	1
${\rm{SO}}_4^{2-}$		−0.027	−0.105	0.797^**	0.986^**	0.642^*	0.687^**	0.134	0.991^**	1
F⁻		−0.271	−0.162	0.874^**	0.854^**	0.377	0.441	0.358	0.819^**	0.819^**	1
NO₃-		−0.107	0.107	0.660^*	0.770^**	0.502	0.487	0.020	0.818^**	0.804^**	0.686^**	1
${\rm{HCO}}_3^{-}$		−0.368	0.148	0.940^**	0.906^**	0.469	0.741^**	0.396	0.899^**	0.883^**	0.868^**	0.706^**	1
TDS		−0.183	0.015	0.876^**	0.981^**	0.582^*	0.733^**	0.257	0.984^**	0.978^**	0.864^**	0.803^**	0.960^**	1
. 在 0.05 级别（双尾），相关性显著。*. 在 0.01 级别（双尾），相关性显著。

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表 3 样品水化学指示的矿物溶解饱和指数

Table 3. Mineral Dissolution Saturation Indices Indicated by Sample Hydrochemistry

样品编号	方解石	白云石	石膏	岩盐
LQ	0.18	0.31	−2.48	−8.40
K4	0.54	1.02	−1.99	−8.92
K5	0.34	0.71	−2.08	−8.55
EG1	0.34	0.68	−2.28	−7.75
BLMSK	0.47	0.99	−1.83	−7.50
GYD	0.35	1.07	−1.92	−7.06
ZWC	0.42	0.73	−1.71	−7.43
YAC	0.18	−0.31	−2.2	−9.18
XJS	0.32	0.51	−2.63	−9.40
MTC	0.68	1.1	−2.57	−9.67
YHX	0.75	1.29	−2.27	−8.65
MCC	0.43	0.33	−2.05	−8.25
WQZ	0.66	1.71	−1.43	−5.95

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