西藏南部叶普曲流域水化学和同位素初步研究

任坤; 王艳; 刘海永; 王雨; 吴华英; 曾洁; 彭聪; 潘晓东; 兰干江; 唐薇薇; 蒋丹丝

doi:10.11932/karst2026y004

西藏南部叶普曲流域水化学和同位素初步研究

doi: 10.11932/karst2026y004

任坤^{1, 2,},
王艳³,
刘海永^3, ,,
王雨³,
吴华英^{1, 2},
曾洁^{1, 2},
彭聪^{1, 2},
潘晓东^{1, 2},
兰干江¹,
唐薇薇¹,
蒋丹丝¹

1.
中国地质科学院岩溶地质研究所/自然资源部、广西岩溶动力学重点实验室/联合国教科文组织国际岩溶研究中心，广西桂林 541004
2.
广西平果喀斯特生态系统国家野外科学观测研究站, 广西平果 531406
3.
西藏自治区地质科学研究院, 西藏拉萨 851400

基金项目: 中央引导地方专项（XZ202301YD0005C）；国家自然科学基金（U24A20597）；中国地质科学院岩溶地质研究所基本科研业务项目（2023008, 2023018）；西藏重点研发计划项目（XZ202501ZY0123）；中国地质调查局地质调查项目（DD20250501408）

详细信息

作者简介:
任坤（1988－），男，副研究员，博士，主要从事岩溶水资源水环境方面研究。E-mail：rkhblhk@163.com

通讯作者:
王雨（1989－），男，工程师，主要从事西藏环境地质、水文地质方面研究。E-mail：wangyu_430@163.com。

中图分类号: P342
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出版历程
- 收稿日期: 2025-02-26
- 录用日期: 2025-07-02
- 修回日期: 2025-06-13
- 网络出版日期: 2026-03-24
- 刊出日期: 2026-04-01

Preliminary study of hydrochemical and isotopic characteristics of the Yepuqu basin, southern Xizang

REN Kun^{1, 2
,},
WANG Yan³,
LIU Haiyong^{3
, ,},
WANG Yu³,
WU Huaying^{1, 2},
ZENG Jie^{1, 2},
PENG Cong^{1, 2},
PAN Xiaodong^{1, 2},
LAN Ganjiang¹,
TANG Weiwei¹,
JIANG Dansi¹

1.
Institute of Karst Geology, CAGS/Key Laboratory of Karst Dynamics, MNR & GZAR/International Research Centre on Karst under the Auspices of UNESCO, Guilin, Guangxi 541004, China
2.
Pingguo Guangxi, Karst Ecosystem, National Observation and Research Station, Pingguo, Guangxi 531406, China
3.
Xizang Autonomous Region Institute of Geological Sciences, Lhasa, Xizang 851400, China

摘要

摘要: 研究典型流域水化学和同位素组成对青藏高原水资源保护具有重要意义。文章以青藏高原南部叶普曲为例，系统采集了泉水、河流、雨水和冰雪融水，分析其水化学和同位素组成，剖析流域水循环和岩石风化机制。结果表明：（1）泉水和河流水化学类型以Ca-HCO₃·SO₄型为主（占82%），其次为Ca-HCO₃（占12%）。（2）利用氢氧同位素分割径流，得到冰雪融水和雨水对泉水的贡献分别为84%和16%；河流水补给来源中冰雪融水和地下水占68%，雨水占32%。（3）大气降水、碳酸盐岩和硅酸盐岩风化是流域水体溶质主要来源；硫酸和碳酸共同参与流域岩石风化，其中硫酸分别贡献泉水和河流阳离子总量的53%和52%。（4）泉水氘过量参数d值分布分散，揭示流域多数泉水属于独立的水文地质单元；河流分布集中，表明河流补给来源较泉水稳定。文章明确了叶普曲地下水和地表水水化学特征及成因机制，指出了硫化物氧化产酸对岩石风化的贡献，丰富了青藏高原流域水和物质循环理论研究，有利于地表水和地下水资源的保护和合理开发。
- 水化学 /
- 氢氧同位素 /
- 氘盈余 /
- 水循环 /
- 岩石风化 /
- 岩溶水 /
- 叶普曲
Abstract: Known as the "Asian Water Tower", the study of water cycle in typical basins of the Qinghai-Xizang Plateau plays a critical role for water resources conservation. This study takes the Yepuqu basin in southern Xizang as the research object, through systematic sampling of spring water, river water, snowmelt, and rainwater (a total of 21 samples collected in June 2023),we comprehensively employed hydrochemical analysis, hydrogen-oxygen isotope tracers (δD, δ¹⁸O), and deuterium excess (d-excess) techniques to investigate water circulation pathways,solute sources and rock weathering mechanism. Key findings include: (1) The dominant water chemical type is Ca-HCO₃·SO₄(82%), followed by Ca-HCO₃ (12%). Isotopic hydrograph separation reveals distinct recharge patterns: spring water recharge derives 84% from snowmelt and 16% from rainfall, while river water recharge comprises 68% from snowmelt and groundwater and 32% from rainfall. Furthermore, the contribution ratio of snowmelt and groundwater decrease progressively along the river flow direction. (2) The solutes are primarily derived from atmospheric precipitation and the weathering of carbonate and silicate rocks. Rainwater contributes 7.6% and 4.2% to the total cation concentration and ${\rm{SO}}_4^{2-}$ in spring water, respectively, and 6.7% and 2.5% in river water, respectively. Notably, sulfate plays a significant role in the rock weathering, accounting for 53% in springs and 52% of the total cation content in spring and river water, respectively, which exceeds the contribution from carbonate weathering. This is mainly attributed to acid production via sulfide oxidation in coal-bearing strata. (3) Springs exhibit highly variable and scattered d-excess values (7.5‰ to 22.4‰), indicating that most springs belong to independent hydrogeological units. In contrast, the d-excess values of river water are concentrated (11.2‰ to 12.7‰), suggesting more stable recharge sources. The downstream decline in river d-excess values reflect an increasing proportion of groundwater recharge. This study quantitatively identifies the dominant contribution of sulfide oxidation-induced acidification to rocking weathering in typical Qinghai-Xizang Plateau basins for the first time. It elucidates the hydrogeological significance of the d-excess parameter in identifying hydrated structural units and water-rock interactions. These findings advance the theoretical framework of water-rock interaction in alpine regions and provide a scientific basis for sustainable water resource management and development on the plateau.
- hydrochemistry /
- hydrogen and oxygen isotope /
- d-excess /
- water cycle /
- rock weathering /
- karst water /
- Yepuqu

HTML

图 1 叶普曲流域位置和采样点分布

Figure 1. Location of the Yepuqu basin and distribution of sampling sites

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图 2 叶普曲流域水体Piper图

Figure 2. Piper diagram for sampled water bodies in the Yepuqu basin

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图 3 叶普曲流域水体δD与δ¹⁸O-H₂O的关系

Figure 3. Dual isotopic plot of δD and δ¹⁸O-H₂O of sampled waters in the Yepuqu basin

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图 4 叶普曲流域地下水和地表水同位素径流分割结果

Figure 4. Results of isotopic hydrograph separation for groundwater and surface water in the Yepuqu basin

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图 5 叶普曲流域地下水和地表水不同离子浓度关系

Figure 5. Plots of relationships between different ion concentrations in groundwater and surface water in the Yepuqu basin

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图 6 叶普曲流域硫酸和碳酸参与岩石风化贡献

Figure 6. Contributions of sulfuric and carbonic acids to rock weathering in the Yepuqu basin

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图 7 叶普曲流域d值变化范围及沿河流流程变化

Figure 7. Variation range of d-excess value and its changes along the river flow in the Yepuqu basin

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表 1 叶普曲流域地下水和地表水同位素径流分割结果

Table 1. Results of isotopic hydrograph separation for groundwater and surface water in the Yepuqu basin

采样点类型	ID	pH	T	K⁺	Na⁺	Ca²⁺	Mg²⁺	${\rm{HCO}}_3^{-}$	Cl⁻	${\rm{SO}}_4^{2-}$	${\rm{NO}}_3^{-}$	TDS	δD	δ¹⁸O-H₂O	d-excess	离子平衡
采样点类型	ID	pH	℃	mg·L⁻¹									‰			%
泉水	S1	8.2	3.9	0.44	3.20	31.5	3.73	23	0.50	76.97	3.59	128	−125.2	−17.4	13.7	−0.71
	S2	7.8	6.2	0.53	3.34	72.7	3.61	191	1.74	45.31	2.52	223	−125.6	−17.1	11.4	−0.86
	S3	8.3	16.4	0.13	1.95	37.6	1.10	72	0.18	40.58	0.37	118	−138.4	−18.2	7.5	0.49
	S4	8.5	11.5	0.66	2.90	59.0	2.60	149	1.08	39.86	2.11	180	−133.4	−17.8	9.1	−0.50
	S5	8.2	8.1	0.44	3.60	82.1	3.14	218	1.34	49.47	1.12	249	−140.5	−18.6	8.6	−1.47
	S6	8.5	10.8	0.45	2.12	16.1	1.77	51	0.74	7.82	2.78	54	−123.5	−16.5	8.8	−0.28
	S7	8.3	22.0	3.12	5.22	22.7	3.21	99	0.67	2.67	<0.05^a	87	−114.4	−17.1	22.4	0.16
	S8	7.9	17.8	2.07	5.21	21.9	1.88	58	3.44	19.51	2.09	83	−101.5	−14.1	11.4	1.09
冰雪融水	R1	8.0	13.2	0.39	1.78	13.0	2.31	37	<0.1	15.10	0.12	51	−134.2	−17.8	8.0	0.09
冰雪融水	R2	8.0	12.6	0.32	0.99	7.3	1.18	25	0.25	7.84	2.36	31	−123.7	−17.0	12.6	−9.65
河流	R3	8.2	20.6	0.41	1.48	8.7	1.25	25	0.52	12.46	1.88	37	−120.7	−16.5	11.5	−8.12
	R4	8.1	13.4	0.37	1.45	19.4	1.56	45	0.57	16.42	2.49	62	−115.7	−16.1	12.7	1.59
	R5	8.4	15.1	0.41	1.59	22.1	1.61	54	0.62	17.25	2.21	71	−116.8	−16.1	12.2	0.43
	R6	8.4	14.9	0.42	1.64	23.4	1.64	58	0.64	17.50	2.23	74	−117.1	−16.2	12.3	0.43
	R7	8.4	22.9	0.51	1.82	23.7	1.72	62	0.70	18.51	<0.05	78	−116.8	−16.1	12.2	−0.38
	R8	8.2	19.7	0.58	1.82	24.5	1.72	66	0.72	18.35	<0.05	81	−116.8	−16.1	12.2	−1.06
	R9	8.7	16.6	1.87	4.87	19.0	1.90	52	3.28	19.70	<0.05	77	−102.1	−14.2	11.7	−0.08
	R10	8.1	17.9	2.05	4.96	21.4	1.85	60	3.29	19.22	0.06	83	−101.0	−14.0	11.2	0.13
	R11	8.1	15.7	1.88	4.21	18.0	1.86	49	2.75	17.76	1.17	71	−104.6	−14.6	12.4	0.76
雨水	P1												−82.5	−11.3	7.8
雨水	P2			0.16	0.35	2.9	0.14	16	0.38	1.07	0.43	13	−95.8	−12.8	6.8	−25.23
注：^a 表示离子浓度低于检测限

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