太行山北段金龙洞岩溶泉水化学及同位素动态特征

吕琳; 李伟; 刘元晴; 宋绵; 邓启军; 郑一迪

doi:10.11932/karst20230111

太行山北段金龙洞岩溶泉水化学及同位素动态特征

1.
中国地质调查局水文地质环境地质调查中心, 河北保定 071051

2.
中国地质调查局地下水勘查与开发工程技术研究中心, 河北保定 071051

基金项目: 中国地质调查局地质调查项目(DD20192059，DD2022175403)

详细信息

作者简介: 吕琳（1987－），男，工程师，硕士，主要从事基岩山区水文地质调查、水文地球化学方面工作。E-mail：lvlin0207@126.com

通讯作者: 刘元晴（1988－），男，高级工程师，硕士，主要从事基岩山区水文地质调查工作。E-mail：lyq198896@ 126.com

中图分类号: P641.3

收稿日期: 2021-01-20

刊出日期: 2023-02-25

Dynamic analysis of hydrochemistry and isotope of the karst spring of Jinlong Cave in the northern section of Taihang Mountains

1.
Center for Hydrogeology and Environmental Geology Survey, China Geological Survey, Baoding, Hebei 071051, China

2.
Engineering Research Center for Groundwater Survey and Exploitation, China Geological Survey, Baoding, Hebei 071051, China

More Information

Corresponding author: LIU Yuanqing, lyq198896@ 126.com

Received Date: 20 January 2021

Publish Date: 25 February 2023

摘要

摘要:
以太行山北段金龙洞岩溶泉为研究对象，通过数理统计、离子比值及饱和指数等方法，分析泉水水化学和同位素动态特征、水中主要离子来源及演化、水–岩相互作用过程等内容。结果显示：（1）金龙洞泉补给来源为大气降水，泉流量对其响应程度高，泉流量较小时，水中主要离子含量相对高，水化学类型为HCO₃ · SO₄-Ca·Mg型，泉流量大时，水中离子含量低，水化学类型为HCO₃-Ca、HCO₃·SO₄-Ca型，泉流量增加引起的稀释作用对离子含量影响明显；（2）控制泉水水化学特征的主要因素为溶滤作用和稀释作用，且Ca²⁺、Mg²⁺、${\rm{HCO}}_3^{-}$主要来源于碳酸盐岩溶解，${\rm{SO}}_4^{2-}$、Na⁺、K⁺、Sr主要来源于安山岩中长石、黄铁矿等矿物的风化溶解，${\rm{NO}}_3^{-}$则来源于人类活动；（3）降水集中期，泉水主要由灰岩区孔洞裂隙水进行补给，补给路径短，降水较小期，则由海拔相对较高的火山岩分化裂隙水进行补给，径流路径较长；（4）氢氧稳定同位素动态特征表明：水中D、¹⁸O含量变化主要受降水和入渗过程中的蒸发及地表水混入影响，且不同季节和时期泉水主要补给来源不同。
- 太行山北段 /
- 岩溶泉 /
- 水化学动态 /
- 同位素 /
- 水−岩相互作用
Abstract:
Karst groundwater is an important part of the groundwater system and one of the important resources to ensure human survival and development. The study area is located in the northern part of Taihang Mountains in the west of Baoding City, Hebei Province. The spring water samples were collected monthly in Jinlong Cave, and their dynamic characteristics of hydrochemistry and isotope were analyzed. The study area presents a low-middle mountain landform with erosive structure and warm temperate semi-arid climate. It is a volcano-sedimentary basin with complex geological and structural conditions, which is one of the typical representatives of the thrust nappe structure in the north-central section of Taihang Mountains. The caprock is exposed in a large area. And the strata are well developed with Precambrian, Cambrian, Ordovician, Carboniferous Benxi Formation and Jurassic strata from the bottom to the top. The lithology is mainly composed of dolomite, limestone, shale and andesite. The Fupingian gneiss, in fault contact with the caprock, is exposed around the sedimentary rock mass. The main water-bearing rock formations are medium-thick limestone and dolomite of the middle and upper Ordovician Majiagou formation, Yeli formation and Liangjiashan formation, and limestone of the upper Cambrian Gushan formation. The groundwater type is the fissure water in exposed carbonate karst cave.
Through the analysis of spring water samples and spring flow monitoring data, the change of spring flow is basically synchronized with the change of precipitation, indicating that the local precipitation is the main source of supply for the spring. According to the flow monitoring data, the response of spring flow to precipitation lags 14-50 days. The main ion concentration in the spring, the spring flow and precipitation all experience changes in different degrees. Generally speaking, the concentration of each ion in the spring water is relatively low at the period of concentrated precipitation (July and August). However, it is opposite in other periods that the concentration of each ion in water is relatively high with different fluctuation ranges in different periods. In a word, the main controlling factors of the chemical characteristics of spring water are leaching and dilution. In addition, trace elements such as Sr and ${\rm{NO}}_3^{-}$ in spring water also change with the spring flow. Sr is negatively correlated with spring flow, which is mainly controlled by dilution. On the contrary, ${\rm{NO}}_3^{-}$ is positively correlated with the spring water volume, indicating that the range of spring water supply changes in different seasons. Based on the dynamic analysis of precipitation isotope, spring water δ¹⁸O and δD is positively correlated with the change of spring discharge. The main reason is that the evaporation under cloud is strong in summer, and raindrops experience unbalanced fractionation, which may result in the increase of δ¹⁸O value and δD value during the precipitation. Besides, the spring water may also be subject to evaporation in the process of infiltration into underground fissures. According to the analysis of d-excess data, the spring water is mainly supplied by the precipitation of ocean water vapor. The analysis of ³⁴S and ⁸⁷Sr/⁸⁶Sr data also proves that the spring water of Jinlong Cave is supplied by regional atmospheric precipitation, and the ${\rm{SO}}_4^{2-}$ in water is not from gypsum dissolution, while the spring water is mixed with the groundwater from the silicate area and the groundwater from the carbonate area. Furthermore, according to the analysis of ion ratio and mineral saturation data of spring water, ${\rm{HCO}}_3^{-}$, Ca²⁺and Mg²⁺in spring water mainly come from the dissolution of carbonate rock dominated by sulfuric acid; ${\rm{SO}}_4^{2-}$ mainly comes from the oxidation dissolution of sulfur-containing minerals such as pyrite in Jurassic andesite. The PHREEQCI software was used to calculate the saturation indexes of calcite, dolomite, gypsum, aragonite and quartz in the groundwater of Jinlong Cave. Results show that the saturation indexes of gypsum and quartz do not change significantly with the change of precipitation and spring water, but gypsum is in an unsaturated state and quartz in a slightly saturated state. Calcite and dolomite are in unsaturated states when the spring flow is large, while they are in saturated states at other times. Aragonite is always in an unsaturated state, but when the spring flow is large, the degree of unsaturation increases. These phenomena prove that dilution is one of the main factors controlling the chemical dynamics of spring water. Therefore, it is considered that the groundwater of Jinlong Cave can be divided based on two periods: during the period of intense precipitation, the groundwater of Jinlong Cave is mainly recharged by the precipitation infiltration in the carbonate rock area where karst fissures such as karst caves are very developed and can quickly convert precipitation into groundwater; during the period of small precipitation, the groundwater is mainly recharged by the groundwater with relatively slow flow rate in the volcanic sedimentary rock area dominated by weathered fissures at high altitude.
- the northern section of Taihang Mountains /
- karst spring /
- hydrochemical dynamics /
- isotope /
- water-rock interaction

HTML全文

图 1 区域地质图及金龙洞地理位置图

Figure 1.

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图 2 pH、水温、电导率动态曲线图

Figure 2.

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图 3 主要离子浓度动态曲线图

Figure 3.

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图 4 Sr、H₂SiO₃、${\rm{NO}}_3^{-}$动态曲线图

Figure 4.

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图 5 δD-δ¹⁸O 关系曲线图

Figure 5.

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图 6 δD、δ¹⁸O 动态曲线图

Figure 6.

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图 7 Cl⁻-δ¹⁸O 关系曲线图

Figure 7.

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图 8 离子比值动态变化图

Figure 8.

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图 9 金龙洞泉矿物饱和度动态变化图

Figure 9.

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表 1 金龙洞泉流量及水化学组分

Table 1. Spring flow and hydrochemical parameters in Jinlong Cave

样品编号	取样日期	水温/ ℃	当月降水量/mm	流量/ m³·h⁻¹	pH	Ec/ μs·cm^-1	TDS	Na⁺	K⁺	Ca²⁺	Mg²⁺		Cl⁻			Sr	H₂SiO₃
样品编号	取样日期	水温/ ℃	当月降水量/mm	流量/ m³·h⁻¹	pH	Ec/ μs·cm^-1	mg·L⁻¹
JLDQ01	2019.9.23	13.8	38.6	973.9	7.76	490.0	279.92	9.50	1.75	66.72	13.98	152.34	5.42	69.79	24.60	0.63	11.00
JLDQ02	2019.11.21	12.6	6.2	521.3	7.83	525.0	285.75	13.98	1.77	64.65	14.90	170.62	5.55	79.40	20.20	0.65	13.74
JLDQ03	2019.12.12	13.1	1.6	693.7	7.70	450.0	300.33	14.12	1.73	65.49	14.52	207.18	7.24	74.72	18.92	0.58	11.98
JLDQ04	2020.1.14	13.3	2.4	568.8	7.85	388.0	273.76	16.46	1.71	63.74	14.95	194.99	5.24	70.41	16.11	0.77	13.74
JLDQ05	2020.4.23	13.4	0.4	398.9	7.32	506.0	290.83	15.20	1.88	57.80	17.94	205.93	5.59	75.69	13.77	1.25	12.89
JLDQ06	2020.5.18	14.0	61.6	655.2	7.61	513.0	297.16	14.49	1.83	65.57	16.57	175.65	7.02	77.31	14.63	1.20	12.89
JLDQ07	2020.6.16	13.7	46.0	224.3	7.80	517.0	295.08	14.30	1.85	65.62	16.65	151.42	7.60	80.46	15.02	1.28	13.45
JLDQ08	2020.7.16	14.7	137.8	1061.1	7.46	513.3	311.07	14.59	2.16	68.39	16.26	205.93	7.40	79.81	19.49	0.91	12.55
JLDQ09	2020.8.22	14.7	203.5	3330.0	7.29	437.7	264.89	5.27	1.59	63.02	12.25	159.16	5.60	75.39	22.19	0.62	9.83
JLDQ10	2020.9.28	14.2	25.3	1524.6	7.58	447.0	279.20	5.20	1.55	63.63	12.85	198.95	5.60	70.74	20.17	0.65	11.19
JLDQ11	2020.10.18	13.5	0.0	1160.2	8.00	400.8	264.50	5.67	1.46	62.73	12.89	189.45	5.38	70.12	18.28	0.65	10.85
JLDQ12	2020.11.20	13.4	28.7	663.1	7.90	499.0	287.04	14.22	1.68	65.56	14.14	185.69	5.99	79.00	13.61	0.79	10.34
JLDQ13	2020.12.14	13.4	0.4	501.6	7.91	474.0	282.30	13.77	1.68	63.36	14.36	179.05	4.86	77.71	17.03	0.51	11.01

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表 2 金龙洞泉同位素测试数据

Table 2. Isotopic data of the spring in Jinlong Cave

样品编号	取样时间	δ¹⁸O_VSMOW/‰	δD_VSMOW/‰	d-excess	δ³⁴S /‰	⁸⁷Sr/⁸⁶Sr
JLDQ01	2019.10.14	−9.0	−62.4	9.6	−0.5	0.710197
JLDQ07	2020.6.16	−10.2	−69.5	12.1
JLDQ08	2020.7.16	−9.9	−66.8	12.4
JLDQ10	2020.9.28	−9.6	−68.0	8.8
JLDQ11	2020.10.18	−9.1	−66.8	6.0
JLDQ12	2020.11.20	−10.1	−70.6	10.2
JLDQ13	2020.12.14	−9.5	−64.7	11.3

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