Hydrochemistry and H-O Isotopic Constraints of Geothermal Fluids in the Guantao Formation in the Eastern Hebei Plain: Implications for Geothermal Reservoir Dynamics

doi:10.19657/j.geoscience.1000-8527.2023.056

Abstract

Abstract:

The Neogene Guantao Formation geothermal reservoir in the Eastern Hebei Plain represents a clastic porous layered heat reservoir characterized by superior geothermal geological conditions. To facilitate the scientific conservation and rational utilization of these geothermal resources, this study presents comprehensive analysis of the chemical and H-O isotopic compositions of 16 geothermal water samples collected from various geological units within the Eastern Hebei Plain. Experimental results reveal that the primary hydrochemical types of the Guantao Formation geothermal water are HCO₃· SO₄-Na, HCO₃·Cl-Na, SO₄·Cl-Na, with pH values ranging from 7.78 to 8.62 and salinity levels between 722.3 and 2619 mg/L. The geothermal water exhibits elevated concentrations of F^-, SiO₂, TDS, Sr, Zn, Br, I, Fe, Mn, and HBO₂. However, concentrations of certain elements associated with magmatic hydrothermal activities (such as F, B, As, Li, etc.) are significantly lower compared to those found in Yangbajing and Dagejia in Tibet. H-O isotopic analysis indicates δD values ranging from -71‰ to -73‰ and δ¹⁸O values from -7.6‰ to -9.8‰, suggesting a recharge elevation of 800 to 1300 meters. The geothermal water primarily flows from northwest to southeast, with minimal interaction with overlying shallow strata water. It is predominantly recharged by lateral flow within the same layer and the upward migration of Ordovician hot fluids from the Paleozoic erathem, classifying it as deep-circulation heated groundwater. Atmospheric precipitation from the Yanshan area percolates downward along fault structures under gravitational force, flowing southeastward. As the groundwater is progressively heated by deep crustal thermal sources, water-rock interactions intensify, leading to a significant increase in mineral content. With increasing circulation depth and distance, the geothermal water environment becomes more confined, resulting in a gradual reduction in water renewal rates. Desulfation processes occur within the geothermal water, which also mixes with underlying deep geothermal fluids, altering the primary ion composition. This study provides a scientific foundation for understanding the formation and evolution of geothermal water in the Guantao Formation.

Key words: hydro-geochemical characteristics, isotopic characteristics, geothermal, Guantao formation, eastern Hebei Plain

CLC Number:

P641.3

XU Yiming, LI Aoyu, CHENG Liqun, DU Lixin, ZHANG Yanshuai, HAO Wenhui, LIU Liang. Hydrochemistry and H-O Isotopic Constraints of Geothermal Fluids in the Guantao Formation in the Eastern Hebei Plain: Implications for Geothermal Reservoir Dynamics[J]. Geoscience, 2025, 39(02): 429-439.

Figures/Tables 12

Fig.1 Schematic diagram of bedrock geology and structure in the study area

Table 1 Main chemical compositions of geothermal water in the study area

构造单元	编号	T (℃)	主要离子浓度/(mg/L)							矿化度 (mg/L)	pH	水化学类型
构造单元	编号	T (℃)	K⁺	Na⁺	Ca²⁺	Mg²⁺	Cl^-	S $O 4 2 -$	HC $O 3 -$	矿化度 (mg/L)	pH	水化学类型
北塘断凹	R21	54	1.31	206.0	7.00	0.14	44.56	147.50	277.30	722.3	8.39	HCO₃·SO₄-Na
北塘断凹	R22	42	1.48	257.1	8.48	0.23	65.10	181.90	317.20	873.5	8.50	HCO₃·SO₄-Na
柏各庄断凸	R5	54	3.72	332.8	33.62	1.74	149.90	438.20	192.80	1197	8.02	SO₄·Cl-Na
	R8	50	5.59	423.8	53.50	3.00	288.90	508.00	166.10	1500	7.83	SO₄·Cl-Na
	R17	53	2.59	302.9	26.56	0.67	54.90	415.60	236.40	1082	8.34	SO₄·HCO₃-Na
	R19	57	2.59	348.8	16.09	0.60	116.10	352.60	287.40	1175	8.35	SO₄·HCO₃-Na
南堡断凹	R1	56	7.05	592.5	52.70	2.06	481.40	605.10	209.10	2026	7.78	SO₄·Cl-Na
	R211	69	2.48	309.7	4.60	0.31	146.80	16.89	533.70	1089	8.52	HCO₃·Cl-Na
	R214	76	2.18	290.5	5.15	0.20	53.84	150.00	485.20	1055	8.62	HCO₃-Na
马头营台凸	R205	70	2.57	253.3	24.57	4.76	244.60	15.08	349.00	932.9	7.91	Cl·HCO₃-Na
	R206	55	3.57	523.9	6.79	0.45	475.10	4.23	653.10	1737	8.12	Cl·HCO₃-Na
	R207	60	4.33	762.3	9.78	1.67	773.80	9.49	704.20	2337	8.41	Cl·HCO₃-Na
	R208	60	3.11	473.0	5.34	0.46	393.90	4.38	565.90	1535	8.55	Cl·HCO₃-Na
	R210	77	6.90	748.4	4.70	0.36	307.90	3.44	1480.00	2619	8.16	HCO₃·Cl-Na
	R263	73	4.61	631.0	4.09	0.84	395.90	36.44	1015.00	2166	8.38	HCO₃·Cl-Na
	R272	78	3.46	618.4	3.41	0.92	392.20	3.17	922.60	2011	8.10	HCO₃·Cl-Na
基岩热储	R215	93	118.10	277.2	131.20	13.80	148.90	827.40	55.98	1597	7.48	SO₄-Na·Ca

Table 1 Main chemical compositions of geothermal water in the study area

构造单元	编号	T (℃)	主要离子浓度/(mg/L)							矿化度 (mg/L)	pH	水化学类型
构造单元	编号	T (℃)	K⁺	Na⁺	Ca²⁺	Mg²⁺	Cl^-	S $O 4 2 -$	HC $O 3 -$	矿化度 (mg/L)	pH	水化学类型
北塘断凹	R21	54	1.31	206.0	7.00	0.14	44.56	147.50	277.30	722.3	8.39	HCO₃·SO₄-Na
北塘断凹	R22	42	1.48	257.1	8.48	0.23	65.10	181.90	317.20	873.5	8.50	HCO₃·SO₄-Na
柏各庄断凸	R5	54	3.72	332.8	33.62	1.74	149.90	438.20	192.80	1197	8.02	SO₄·Cl-Na
	R8	50	5.59	423.8	53.50	3.00	288.90	508.00	166.10	1500	7.83	SO₄·Cl-Na
	R17	53	2.59	302.9	26.56	0.67	54.90	415.60	236.40	1082	8.34	SO₄·HCO₃-Na
	R19	57	2.59	348.8	16.09	0.60	116.10	352.60	287.40	1175	8.35	SO₄·HCO₃-Na
南堡断凹	R1	56	7.05	592.5	52.70	2.06	481.40	605.10	209.10	2026	7.78	SO₄·Cl-Na
	R211	69	2.48	309.7	4.60	0.31	146.80	16.89	533.70	1089	8.52	HCO₃·Cl-Na
	R214	76	2.18	290.5	5.15	0.20	53.84	150.00	485.20	1055	8.62	HCO₃-Na
马头营台凸	R205	70	2.57	253.3	24.57	4.76	244.60	15.08	349.00	932.9	7.91	Cl·HCO₃-Na
	R206	55	3.57	523.9	6.79	0.45	475.10	4.23	653.10	1737	8.12	Cl·HCO₃-Na
	R207	60	4.33	762.3	9.78	1.67	773.80	9.49	704.20	2337	8.41	Cl·HCO₃-Na
	R208	60	3.11	473.0	5.34	0.46	393.90	4.38	565.90	1535	8.55	Cl·HCO₃-Na
	R210	77	6.90	748.4	4.70	0.36	307.90	3.44	1480.00	2619	8.16	HCO₃·Cl-Na
	R263	73	4.61	631.0	4.09	0.84	395.90	36.44	1015.00	2166	8.38	HCO₃·Cl-Na
	R272	78	3.46	618.4	3.41	0.92	392.20	3.17	922.60	2011	8.10	HCO₃·Cl-Na
基岩热储	R215	93	118.10	277.2	131.20	13.80	148.90	827.40	55.98	1597	7.48	SO₄-Na·Ca

Fig. 2 Piper trigraph of geothermal water in the eastern Hebei Plain

Table 2 Content of special components of geothermal water in Guantao Formation of eastern Hebei Plain

构造单元	井号	含量:(mg/L)
构造单元	井号	Sr	Fe	Mn	Li	Zn	As	F^-	SiO₂	碘化物	溴化物	偏硼酸
北塘断凹	R21	0.134	0.049	0.012	0.019	2.230	-	0.82	30.20	-	0.10	0.65
北塘断凹	R22	0.158	0.030	0.018	0.022	0.008	-	0.95	27.21	0.03	0.10	1.58
柏各庄断凸	R5	0.834	0.156	0.073	0.052	1.745	-	1.57	30.52	-	0.30	8.46
	R8	1.390	0.463	0.166	0.096	0.555	-	3.13	31.76	0.03	0.84	15.28
	R17	0.510	0.075	0.063	0.021	0.004	-	0.75	32.77	-	0.10	0.34
	R19	0.326	0.084	0.028	0.057	0.003	-	1.52	34.83	0.03	0.10	6.09
南堡断凹	R1	1.956	0.404	0.122	0.205	0.036	-	4.04	39.12	0.04	1.26	30.20
	R211	0.117	0.095	0.014	0.054	0.043	-	5.20	41.41	0.04	0.35	8.88
	R214	0.146	0.059	0.012	0.024	0.005	-	4.36	40.75	-	0.10	4.79
马头营台凸	R205	0.396	0.141	0.107	0.025	0.392	-	2.35	29.95	0.24	0.65	5.92
	R206	0.231	0.254	0.018	0.036	0.027	-	5.03	39.95	0.40	1.20	22.91
	R207	0.390	0.097	0.020	0.043	0.154	-	3.90	35.97	0.15	0.93	10.58
	R208	0.210	0.097	0.022	0.021	1.460	-	7.55	35.81	0.17	0.85	22.94
	R210	0.218	0.083	0.012	0.059	0.024	-	5.87	46.82	0.15	0.53	13.22
	R263	0.209	0.225	0.014	0.033	0.043	-	7.24	43.21	0.16	0.77	14.58
	R272	0.133	0.111	0.014	0.038	0.910	-	8.25	39.72	0.21	0.96	17.15
基岩热储	R215	9.508	0.527	0.043	1.900	0.008	-	5.26	7.77	0.04	0.23	13.24

Fig.3 Diagram of F- SiO2 vs. temperature of geothermal water in Guantao Formation of eastern Hebei Plain

Fig. 4 Histogram of chemical composition of geothermal water from Guantao Formation in the eastern Hebei, Xiongan New Area Yangbajing and Dagegjia in Tibet

Table 3 Recharge elevation of geothermal water in Guantao Formation of eastern Hebei Plain

构造单元	编号	井口高程(m)	δD(‰)	δ¹⁸O(‰)	δD计算高程(m)	δ¹⁸O计算高程(m)	平均值(m)
北塘断凹	R21	1.65	-73	-9.7	1448	1088	1268
北塘断凹	R22	1.45	-73	-9.7	1448	1088	1268
柏各庄断凸	R5	2.81	-73	-9.5	1450	1023	1236
	R8	3.00	-73	-9.2	1450	923	1187
	R17	1.52	-73	-9.8	1448	1122	1285
	R19	3.79	-73	-9.5	1451	1024	1237
南堡断凹	R1	4.63	-73	-8.6	1451	725	1088
	R211	1.12	-73	-9.2	1448	921	1185
	R214	2.67	-73	-9.7	1449	1089	1269
马头营台凸	R205	5.62	-71	-7.6	1372	392	882
	R206	3.90	-71	-8.1	1371	557	964
	R207	3.81	-72	-9.1	1411	890	1150
	R208	3.61	-72	-8.7	1410	757	1084
	R210	1.96	-72	-9	1409	855	1132
	R263	2.34	-72	-8.9	1409	822	1116
	R272	1.74	-72	-8.6	1409	722	1065
基岩热储	R215	2.10	-74	-9.3	1488	952	1220

Fig.5 Diagram of δD-δ18O of geothermal water in GuantaoFormation

Fig. 6 Diagram of δD vs. well depth and temperature of geothermal water in Guantao Formation of eastern Hebei Plain

Fig.7 Diagram of δ18O vs. well depth and temperature of geothermal water in Guantao Formation of eastern Hebei Plain

Table 4 Calculation results of characteristic coefficients in Guantao Formation of eastern Hebei Plain

构造单元	编号	变质系数	脱硫系数	盐化系数	ω(Cl)/ ω(Br)
构造单元	编号	(γNa/ γCl)	(γSO₄/ γCl)	(γC1/ (γHCO₃+ γCO₃))	ω(Cl)/ ω(Br)
北塘断凹	R21	4.62	3.31	0.16		446
北塘断凹	R22	3.95	2.79	0.20		651
柏各庄断凸	R5	2.22	2.92	0.78		500
	R8	1.47	1.76	1.74		344
	R17	5.52	7.57	0.23		549
	R19	3.00	3.04	0.40		1161
南堡断凹	R1	1.23	1.26	2.30		382
	R211	2.11	0.12	0.27		419
	R214	5.40	2.79	0.11		538
马头营台凸	R205	1.04	0.06	0.70		376
	R206	1.10	0.01	0.73		396
	R207	0.99	0.01	1.07		832
	R208	1.20	0.01	0.67		463
	R210	2.43	0.01	0.21		581
	R263	1.59	0.09	0.39		514
	R272	1.58	0.01	0.43		409

Fig.8 Schematic diagram of the genesis of geothermal water in the east Hebei Plain

References 28

[1]	王贵玲, 张薇, 蔺文静, 等. 全国地热资源调查评价与勘查示范工程进展[J]. 中国地质调查, 2018, 5(2): 1-7.
[2]	王奎峰, 杨德平, 宋香锁, 等. 临清市馆陶组地热水化学特征及结垢腐蚀性研究[J]. 水文地质工程地质, 2010, 37(1): 130-134.
[3]	赵铭海, 李晓燕, 宋明水, 等. 济阳坳陷东营组—馆陶组地热资源评价[J]. 油气地质与采收率, 2015, 22(4): 1-5, 13.
[4]	阮传侠, 冯树友, 沈健, 等. 天津滨海新区地热资源循环利用研究——馆陶组热储回灌技术研究与示范[J]. 地质力学学报, 2017, 23(3): 498-506.
[5]	靳宝珍, 杨永江, 李俊峰, 等. 天津静海县史家庄一带馆陶组地热流体质量及实用性[J]. 地质调查与研究, 2007, 30(3): 219-223.
[6]	李秀英, 蔡洪涛, 任清岭. 沧州市区地热地质特征及地热资源开发探讨[J]. 地球学报, 2000, 21(2): 171-176.
[7]	刘明亮, 何曈, 吴启帆, 等. 雄安新区地热水化学特征及其指示意义[J]. 地球科学, 2020, 45(6): 2221-2231.
[8]	赵佳怡, 张薇, 马峰, 等. 雄安新区容城地热田地热流体化学特征[J]. 地质学报, 2020, 94(7): 1991-2001.
[9]	李攻科, 王卫星, 杨峰田, 等. 河北遵化汤泉地热田成因模式[J]. 现代地质, 2015, 29(1): 220-228.
[10]	李娟, 周训, 方斌, 等. 河北秦皇岛市温泉堡温泉的形成与开发利用建议[J]. 地质通报, 2007, 26(3): 344-349.
[11]	程立群, 徐一鸣, 杜立新, 等. 冀东燕山中段地热地质条件分析与资源潜力评价[J]. 矿产勘查, 2020, 11(12): 2637-2646.
[12]	杨立顺. 唐山沿海地区地热资源开发利用及前景[J]. 中国环境管理干部学院学报, 2011, 21(1): 23-25.
[13]	原若溪, 王贵玲, 刘峰, 等. 冀东北地区中低温对流型地热系统的氟指示意义研究[J]. 地质论评, 2021, 67(1): 218-230.
[14]	孙红丽, 马峰, 刘昭, 等. 西藏高温地热显示区氟分布及富集特征[J]. 中国环境科学, 2015, 35(1): 251-259.
[15]	YUAN J F, GUO Q H, WANG Y X. Geochemical behaviors of boron and its isotopes in aqueous environment of the Yangbajing and Yangyi geothermal fields, Tibet, China[J]. Journal of Geochemical Exploration, 2014, 140: 11-22.
[16]	LIU M L, GUO Q H, WU G, et al. Boron geochemistry of the geothermal waters from two typical hydrothermal systems in Southern Tibet (China): Daggyai and Quzhuomu[J]. Geothermics, 2019, 82: 190-202.
[17]	路畅, 李营, 陈志, 等. 华北断陷盆地中北部地热水地球化学特征及成因初探[J]. 矿物岩石地球化学通报, 2018, 37(4): 663-673, 795.
[18]	刘士林, 刘蕴华, 林舸, 等. 渤海湾盆地南堡凹陷新近系泥岩稀土元素地球化学特征及其地质意义[J]. 现代地质, 2006, 20(3): 449-456.
[19]	CRAIG H. Isotopic variations in meteoric waters[J]. Science, 1961, 133: 1702-1703. PMID
[20]	郑淑蕙, 侯发高, 倪葆龄. 我国大气降水的氢氧稳定同位素研究[J]. 科学通报, 1983, 28(13): 801-806.
[21]	张洪平, 刘恩凯, 王东升, 等. 中国大气降水稳定同位素组成及影响因素[J]. 中国地质科学院水文地质工程地质研究所所刊, 1991, (7): 101-110.
[22]	姜哲, 周训, 陈柄桦, 等. 四川康定市二道桥地区地下热水稳定同位素特征及热储温度计算[J]. 现代地质, 2022, 36(4): 1183-1192.
[23]	PANG Z H, KONG Y L, LI J, et al. An isotopicgeoindicator in the hydrological cycle[J]. Procedia Earth and Planetary Science, 2017, 17: 534-537.
[24]	李真, 姚檀栋, 田立德, 等. 慕士塔格冰川地区降水中δ¹⁸O的时空变化特征[J]. 中国科学(D辑: 地球科学), 2006, 36(1): 17-22.
[25]	吴艳军, 方郭志, 张盛生, 等. 海东市平安区张其寨地热田水化学特征及其成因分析[J]. 青海大学学报, 2018, 36(5): 65-71.
[26]	殷晓曦, 陈陆望, 谢文苹, 等. 采动影响下矿区地下水主要水-岩作用与水化学演化规律[J]. 水文地质工程地质, 2017, 44(5): 33-39.
[27]	王贵玲, 蔺文静. 我国主要水热型地热系统形成机制与成因模式[J]. 地质学报, 2020, 94(7): 1923-1937.
[28]	陈墨香, 汪集旸, 汪缉安, 等. 华北断陷盆地热场特征及其形成机制[J]. 地质学报, 1990, 64(1): 80-91.