Tong Xiao-xia; Gan Rong; Gu Shu-qian; Sun Xing-le; Huang Kai-tuo; Yan Xiao-feng

doi:10.19637/j.cnki.2305-7068.2022.04.007

doi: 10.19637/j.cnki.2305-7068.2022.04.007

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出版历程
- 收稿日期: 2022-07-20
- 录用日期: 2022-11-04
- 网络出版日期: 2022-12-27
- 刊出日期: 2022-12-31

Stable chlorine isotopic signatures and fractionation mechanism of groundwater in Anyang, China

1.
China geological Environmental Monitoring Institute, Beijing 100081, China
2.
School of Water Conservancy Engineering, Zhengzhou University, Zhengzhou 450001, China
3.
Henan ProvincialGeological Environment PlanningDesign Co., ltd, Zhengzhou 450001, China
4.
Henan Provincial Institute of Geological Environment Exploration, Zhengzhou 450001, China
5.
Henan Baoyuan Exploration Technology Co., Ltd, Zhengzhou 476341, China

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Corresponding author: ktz2022@163.com

摘要

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Abstract: The present work provides an online Bench II-IRMS technique for the measurement of stable chlorine isotope ratio, which is used to measure the δ³⁷Cl of 38 groundwater samples from the Karst and Quaternary aquifers in Anyang area. The regional distribution and signature of δ³⁷Cl value are characterized on the base of isotopic data. The results suggest that the δ³⁷Cl value of Quaternary groundwater decreases with increasing Cl⁻ concentration, and has no correlation with δ¹⁸O and δD values, but closely correlates with the depth to water table. The fractionation mechanism of the chlorine isotope is expounded according to the type of groundwater. The δ³⁷Cl value of karst water is generally positive, which is relevant to the dissolution of evaporite (gypsum mine), and may be caused by the mixing of groundwater and precipitation. The groundwater of Quaternary unconfined aquifer is mainly recharged by precipitation, and the δ³⁷Cl value of groundwater is generally negative. The δ³⁷Cl value of groundwater in Quaternary confined aquifer is more negative with increasing the depth to water level and elevated Cl⁻ concentration, which is possible to result from the isotope fractionation of ion filtration. The groundwater with inorganic pollutants in Quaternary unconfined aquifer has generally a positive δ³⁷Cl value.
- North China Plain /
- Groundwater /
- Gas Bench II-IRMS /
- Chlorine isotope /
- Karst aquifer

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Figure 1. Geological map of the study area and distribution of sampling points

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Figure 2. Correlation between groundwater Cl⁻ concentration and δ³⁷Cl values

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Figure 3. Relationship between δ¹⁸O and δD values of groundwater

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Figure 4. δ³⁷Cl-δ¹⁸O_H₂O relationship

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Figure 5. δ³⁷Cl-δD_H₂O relationship

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Figure 6. Relationship between groundwater Cl⁻ ion concentration and burial depth

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Figure 7. Relationship between groundwater δ³⁷Cl value and burial depth

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Figure 8. (a) Relationship between Cl⁻ and δ³⁷Cl values in pore pressurized water of the Quaternary system (b) Conceptual illustration of ion permeation. 034 (0.21, 105.5) indicates point 034 (δ³⁷Cl, Cl⁻) , respectively

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Table 1. Results of chemical compositions and isotope of groundwater in the Anyang area

Num	Position	Well	Type	Cl⁻	δ³⁷Cl_SMOC (‰)	δ¹⁸O_VSMOW (‰)	δD_VSMOW (‰)
001	Beishan Village 1	120	Karst water	16.1	0.25	−8.06	−60.7
002	Beishan Village	120	Karst water	15.9	0.30	−8.36	−62.6
003	Xi-quyang	160	Karst water	41.5	0.29	−7.47	−58.6
004	Shangtao Village	25	Quaternary	13.4	0.03	−8.22	−63.0
005	Shang-yanke	185	Karst water	28.2	0.07	−7.91	−61.7
006	Redflag canal	C	Canal water	52.1	0.48	−7.80	−62.0
007	Redflag canal	sp	Spring water	10.6	0.04	−8.78	−64.5
008	Jian Village	sp	Spring water	10.5	0.20	−8.43	−61.3
009	Guojia Village	sp	Spring water	8.6	−0.26	−9.59	−65.9
010	Ni-hetou	15	Quaternary	191.6	−0.28	−7.81	−58.4
011	Beiqu Ditch	40	Quaternary	87.4	0.12	−7.55	−57.4
012	Pearl-spring	sp	Spring water	14.9	0.15	−8.31	−64.1
013	Jishan Village 1	15	Quaternary	89.1	0.32	−7.74	−60.8
014	Jishan Village 2	20	Karst water	17.0	0.49	−8.27	−63.4
015	Gutuo Village	6	Quaternary	146.5	0.56	−7.16	−54.4
016	Zhongle Village	10	Quaternary	23.1	0.02	−7.64	−61.2
017	Shaojia Tun	40	Quaternary	37.9	0.65	−7.52	−58.8
018	Biaojian Village	19	Quaternary	85.3	0.13	−7.97	−61.2
019	Guo-wangdu	20	Quaternary	38.4	5.12	−8.41	−66.9
020	Geological seven	70	Quaternary	130.4	0.20	−7.61	−60.0
021	Xiao-nanhai	sp	Spring water	22.3	0.35	−7.89	−62.6
022	Zhang er Village	13	Karst water	15.7	0.35	−8.41	−62.2
023	Xiabao Village	20	Karst water	16.7	0.60	−8.32	−63.0
024	Tielu Village	20	Karst water	16.5	0.11	−8.33	−62.2
025	Xiao-tun Village	17	Karst water	16.0	0.17	−8.50	−64.2
026	Guojiayuan	18	Karst water	23.6	0.13	−7.92	−61.0
027	Xiaodian Village	18	Karst water	20.0	0.12	−8.41	−63.0
028	Bei-xiangkou	19	karst water	20.9	0.27	−8.47	−63.4
029	Jiao-jiawan	17	Quaternary	17.6	−0.02	−9.12	−66.1
030	Beiwu Village	30	Quaternary	48.7	0.20	−10.0	−75.6
031	Fengsu Village	40	Quaternary	85.3	0	−7.28	−56.0
032	Lu Villge	70	Quaternary	154.8	0.14	−8.69	−66.3
033	Bei-liugou	20	Quaternary	291.5	−0.01	−9.20	−71.1
034	Dudian Village	40	Quaternary	105.5	0.21	−8.30	−63.0
035	Shang-cheng	40	Quaternary	29.4	0.03	−8.16	−61.6
036	Shi-changtun	12	Quaternary	150.8	0.09	−7.20	−56.8
037	Gaojia Village	20	Quaternary	33.1	−0.14	−7.70	−61.5
038	Ma-toujian Village	70	Quaternary	52.6	0.19	−8.33	−64.6

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Table 2. The measured chlorine isotope values of the Bohai Sea and the Yellow Sea

	Sampling location	Sampling time（year）	Measured δ³⁷Cl (‰)
The Bohai sea	Peitaiho	2010	0.06
	Peitaiho (500 m from the shore)	2010	−0.10
	Huanghua City, Hebei Province	2010	−0.08
Yellow Sea	Yantai, Shandong	1995	0.00
The East China Sea	Shanghai	2010	−0.01
Notes: ISL-354 seawater was used as the standard (Xiao et al. 2007)

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