岩溶热储高矿化度地热流体成因机制研究

余杰; 毛绪美; 彭慧; 文美霞; 王辛; 范威; 汤伟

doi:10.11932/karst2022y32

岩溶热储高矿化度地热流体成因机制研究——以巴东县盐场河地热田为例

doi: 10.11932/karst2022y32

余杰^{1, 2,},
毛绪美³,
彭慧^{1, 2},
文美霞^{1, 2},
王辛^{1, 2},
范威^{1, 2},
汤伟^{1, 2}

1.
湖北省地质环境总站, 湖北武汉 430034
2.
资源与生态环境地质湖北省重点实验室, 湖北武汉 430034
3.
中国地质大学(武汉)环境学院, 湖北武汉 430074

基金项目: 湖北省自然资源厅地勘资金项目2017年计划（鄂地勘基金合〔2017〕45号）

详细信息

作者简介:
余杰（1988－），男，硕士，工程师，从事水文、工程、环境地质研究。E-mail：826643858@qq.com

中图分类号: P314
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出版历程
- 收稿日期: 2022-02-28
- 网络出版日期: 2023-02-14
- 刊出日期: 2023-11-28

Genesis mechanism of geothermal fluid with high mineralization in karst geothermal reservoir: A case study of geothermal field of the Yanchang river, Badong county

YU Jie^{1, 2
,},
MAO Xumei³,
PENG Hui^{1, 2},
WEN Meixia^{1, 2},
WANG Xin^{1, 2},
FAN Wei^{1, 2},
TANG Wei^{1, 2}

1.
Geological Environmental Center of Hubei Province, Wuhan, Hubei 430034, China
2.
Hubei Key Laboratory of Resources and Eco-environmental Geology, Wuhan, Hubei 430034, China
3.
School of Environmental Studies, China University of Geosciences, Wuhan, Hubei 430074, China

摘要

摘要: 岩溶热储中地热流体多为中低温低矿化度热水，而岩溶热储中出现高矿化度地热水多与岩溶含水层矿物溶解有关。然而，湖北省巴东县盐场河地热田中地热水TDS高达12 477.7 mg·L⁻¹，水温约34 ℃，含水层矿物溶解并不足以解释其成因。文章在野外调查和地热钻探的基础上，对4个地热钻孔、1个温泉及附近4个冷泉进行了水文地球化学采样和测试。研究结果表明：盐场河地热田地热水化学类型为Cl-Na型，单位涌水量最大可达1 767 m³·d⁻¹，出水口温度在30.2~34.5 ℃。对比钻孔测温和SiO₂温度计分析，热储温度为59.1 ℃，循环深度为1 923 m。Phreeqc水化学模拟揭示含水层中的水–岩相互作用（主要是含水层矿物溶解）为地热水化学组分提供了部分贡献，主要来源于径流过程中咸化潮坪泻湖相盐岩的溶解。水文地质条件和氢氧同位素指示地热水的大气降水来源，但季节性的冷水混入控制了水−岩相互作用的平衡。可见，巴东县盐场河岩溶热储高矿化度地热水主要是径流过程中盐岩的溶解提供了水化学组分，但是出露过程中受到季节性的冷水混合影响。
- 高矿化度 /
- 岩溶热储 /
- 水化学 /
- 同位素 /
- 成因机制
Abstract: At present, China's energy development has entered a new stage of carbon reduction and energy conservation. In order to achieve the goal of "carbon peak" and "carbon neutrality", the development and utilization of geothermal energy has been ushered in unprecedented opportunities. However, not all geothermal resources can be directly exploited and utilized. Based on a funded project—Feasibility of Geothermal Resources Exploration in Yanchang river, Badong county, Hubei Province, we have built a genesis model of the geothermal field mainly by means of software analysis, traditional geological survey, drilling, sampling analysis and systematic temperature measurement. In the aspect of hydrochemistry, we also analyzed the genesis of geothermal fluid with high mineralization in karst geothermal reservoir in the Yanchang river. According to previous research, hydrogeological survey, geophysical exploration and drilling, we found out the geothermal geological conditions, regional stratigraphic distributions, lithologic characteristics and structural distributions in the study area, which can provide data for the construction of genesis model of geothermal field. In addition, by sampling, testing, and monitoring water temperatures, we compared the chemical components of cold springs and geothermal fluids in different periods, and further analyzed the hydrogeochemical characteristics of geothermal fluids and the reasons for temperature anomalies. The research findings may provide the technical and theoretical basis for the genesis mechanism of geothermal fluid with high mineralization in karst geothermal reservoir as well as the basis for the scientific development and utilization of karst geothermal reservior.The geothermal fluid in the karst geothermal reservoir is mostly hot water with low mineralization at low temperature, while the highly mineralized geothermal water is often related to the dissolution of karst aquifer minerals. However, the TDS of geothermal water in the geothermal field of the Yanchang river is as high as 12,477.7 mg·L⁻¹, and the water temperature is about 34 ℃. The dissolution of aquifer minerals is unlikely to explain the genesis mechanism. On the basis of field investigation and geothermal drilling, we conducted the hydrogeochemical sampling and testing in four geothermal boreholes, one hot spring and four nearby cold springs. The research shows that the study field belongs to the convection-type geothermal resource at medium-low temperatures under the control of deep and large faults. The Ordovician limestone and dolomite are the main strata for geothermal reservoir, belonging to the karst fissure type. The chemical type of geothermal water in the Yanchang river is Cl-Na. The maximum unit water inflow can reach 1,767 m³·d⁻¹, with the outlet temperatures from 30.2 ℃ to 34.5 ℃. Compared with the analysis of borehole temperature and SiO₂ thermometer, the temperature of geothermal fluid is 59.1 ℃, and the circulation depth is 1,923 m. It is found that the geothermal fluid can complete sufficient heat exchange with heat source in the long migration path and long runoff time, the process of which may gradually increase groundwater temperatures. The sulfur isotope analysis shows that sulfate in karst water is derived from recharge water including atmospheric precipitation, surface water, and water formed by the oxidation of pyrite in rock mass. Groundwater maintains a relatively stable balance between oxidation and reduction. The aquifer is a transition between the alternation of a weak (lagging) and a strong environment, having a certain but low-degree recharge condition. Phreeqc hydrochemical simulations reveal the water-rock interactions (mainly the dissolution of aquifer minerals) in the aquifer, and further reveal that the high salinity of chemical composition in geothermal water is derived mainly from the dissolution of salt rocks in the salinized tidal flat lagoon facies during the runoff process. According to the analysis of tritium isotope, the content of tritium in geothermal fluid increases significantly, mainly because the geothermal fluid with low tritium content is mixed with shallow water or surface cold water when the geothermal fluid pours out along the fault under the influence of deep heat source and long runoff path. Hydrogeological conditions and hydrogen and oxygen isotopes can indicate the origin of atmospheric precipitation of geothermal water. The groundwater recharge height ranges from 1,261.21 m to 1,298.25 m, while the height of the Xiaoshennongjia mountain area in the north of the geothermal field ranges from 900 m to 1,300 m, which is the recharge area of the geothermal field of the Yanchang river. However, seasonal cold water addition controls the balance of water-rock interactions. It can be concluded that the high mineralization in geothermal water of the Yanchang river is mainly formed by the dissolution of salt rock during the runoff process, during which the upward flow is affected by seasonal mixing of cold water. Furthermore, F6 tensile faults and F7 water-blocking faults in geothermal fields affect not only the flow direction and velocity of groundwater, but also the increasing content of TDS in geothermal fluids.
- high mineralization /
- karst geothermal reservoir /
- hydrochemistry /
- isotopes /
- genesis mechanism

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图 1 盐场河地热田地热地质简图

1-三叠系下统大冶组 2-二叠系中统瓦屋湾组 3-二叠系上统茅口组 4-二叠系上统栖霞组 5-泥盆系中上统云台观组 6-志留系中统纱帽组 7-志留系下统罗惹坪组 8-志留—奥陶系龙马溪组 9-奥陶系中上统宝塔组 10-奥陶系下统南津关组 11-寒武系上统娄山关组 12-寒武系中统覃家庙组 13-寒武系下统石龙洞组 14-寒武系下统天河板组 15-寒武系下统牛蹄塘+石牌组 16-震旦系中统陡山沱组 17-地层界线 18-正断层 19-逆断层 20-钻孔 21-温泉 22-冷泉 23-剖面线 24-地下水流向 25-研究区范围 26-地热田范围

Figure 1. Thermal geology diagram of geothermal field of the Yanchang river

1-Lower Triassic Daye Formation 2-Middle Permian Wawuwan Formation 3-Upper Permian Maokou Formation 4-Upper Permian Qixia Formation 5-Middle Upper Devonian Yuntaiguan Formation 6- Middle Silurian Shamao Formation 7-Lower Silurian Luojiaping Formation 8-Silur-Ordovician Longmaxi Formation 9-Middle Upper Ordovician Baota Formation 10-Lower Ordovician Nanjinguan Formation 11-Upper Cambrian system Loushanguan Formation 12-Middle Cambrian Qinjiamiao Formation 13-Lower Cambrian Shilongdong Formation 14-Lower Cambrian Tianheban Formation 15- Lower Cambrian Niutitang and Shipai Formation 16-Middle Sinian Doushantuo Formation 17-stratigraphic boundary 18-normal fault 19-reverse fault 20-borehole 21-hot spring 22-cold spring 23-section line 24-groundwater flow direction 25-study area 26-geothermal field area

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图 2 Piper三线图

Figure 2. Piper triplet

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图 3 离子与温度关系图

a. F⁻与温度关系图 b. SiO₂与温度关系图 c. SO₄²⁻与温度关系图 d. Cl⁻与温度关系图 e. HCO₃⁻与温度关系图 f. Na⁺与温度关系图 g. Mg²⁺与温度关系图 h. Ca²⁺与温度关系图

Figure 3. Relationship between ions and temperatures

a. Relationship between F⁻and temperatures b. Relationship between SiO₂ and temperatures c. Relationship between SO₄²⁻and temperatures d. Relationship between Cl⁻and temperatures e. Relationship between HCO₃⁻and temperatures f. Relationship between Na⁺and temperatures g. Relationship between Mg²⁺and temperatures h- Relationship between Ca²⁺and temperatures

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图 4 与降水线关系图

Figure 4. Relationship with precipitation line

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图 5 地下含水层与地表水硫同位素关系图

Figure 5. Sulfur isotope relationship between underground aquifer and surface water

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图 6 地热田成因模式示意图

Figure 6. Genesis model of the geothermal field

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表 1 地下水赋存条件统计表

Table 1. Statistics of groundwater occurrence conditions

地层年代	含水地层代号	主要岩性	赋存地下水类型	富水性
第四系	Qh	砂卵砾石	松散岩类孔隙水	弱
二叠、三叠系	P₂w、P₁m、P₁q、 T₁d	微晶灰岩	碳酸盐岩裂隙岩溶水	中等
泥盆系	D_2-3y	石英砂岩	碎屑岩类裂隙水	弱
寒武、奥陶系	O₁n、O₁Є₃l、Є₂qn、Є₁sl	白云岩、微晶灰岩	碳酸盐岩裂隙岩溶水	中等
志留系	/	页岩、泥岩、泥质粉砂岩	隔水层	差

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表 2 地热田地层岩性和水温基本特征一览表

Table 2. Basic characteristics of lithology and water temperature of the geothermal field

孔号	孔深/m	含水层/m	岩性特征	温度特征
ZK01	203.59	74.0~80.60	白云岩：黑色、灰黑色，可见方解石晶簇及小溶孔	该孔地热流体温度21.93~28.45 ℃。其中，在第一段含水层平均水温24.1 ℃，第二段含水层平均水温23.7 ℃。在18.00 m处温度达最高，而后逐渐降低，在134.00 m处温度达最低，孔底温度升至23.97 ℃
ZK01	203.59	101.3~105.2	白云岩：黑色、灰黑色，可见溶蚀现象，多为溶孔，见方解石晶体
ZK02	111.29	12.30~13.10	白云岩：灰白色，可见溶蚀现象，溶孔连续呈线状发育，可见方解石晶体充填	该孔地热流体温度23.70~32.36 ℃。其中，在第一段含水层平均水温30.9 ℃，第二段含水层平均水温30.4 ℃。在10.00 m处温度达最高，而后逐渐降低，在107.07 m处温度达最低，孔底温度升至24.30 ℃
ZK02	111.29	21.50-21.70	白云岩夹灰岩角砾：灰白色、深灰色，岩石节理裂隙发育，可见溶蚀现象，可见方解石晶体充填
ZK03	141.61	22.30~26.90	碎裂白云岩：灰白色、深灰色，可见溶蚀现象，节理裂隙较发育。	该孔地热流体温度21.62~35.34 ℃。其中，在第一段含水层平均水温35.2 ℃，第二段含水层平均水温29.9 ℃，第三段含水层平均水温25.6 ℃。在19.00 m处温度达最高，而后逐渐降低，在98.08 m处温度达最低，孔底温度升至23.62 ℃
		34.05~41.35	白云岩：灰白色，可见溶蚀现象，见方解石晶体充填
		54.75~60.10	角砾岩：灰黑色，受断层挤压，节理裂隙较发育，可见溶蚀现象，在58.1 m处见硅化现象，59.1-59.15 m处岩芯可见黄铁矿富集
ZK04	199.6	18.45~27.80	碎裂白云岩：灰白色，节理裂隙较发育，可见溶蚀现象，多为溶孔	该孔地热流体温度22.96~29.42 ℃。其中，在第一段含水层平均水温29.3 ℃，第二段含水层平均水温29.0 ℃。在40.00 m处温度达最高，而后逐渐降低，在169.01 m处温度达最低，孔底温度升至24.96 ℃
ZK04	199.6	32.40~36.60	碎裂白云岩：灰白色，节理裂隙较发育，可见溶蚀现象，多为溶孔、溶槽

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表 3 盐场河地热田水化学及同位素数据

Table 3. Hydrochemistry and isotope data of the geothermal field of the Yanchang river

样品		采样时间	温度	pH	TDS	HCO₃⁻	Cl⁻	NO₃⁻	SO₄²⁻	K⁺	Na⁺	Ca²⁺	Mg²⁺	SiO₂	Li	Ba	Sr	F	Si	B	δD ‰	δ¹⁸O ‰	δ³⁴S_CDT‰	水化学类型
神农温泉	BD- QS-001	2017.08	31	7.86	8 402.7	2 003.23	3 754.82	0.12	283.5	49.7	3 090.55	130.81	27.96	15.21	0.19	0.09	2.68	−	7.09	0.27	−60.37	−8.97	−6.07	Cl-Na
神农温泉	BD- QS-002	2017.11	25	7.92	11 193.5	606.65	6 052.44	2.94	470.76	45.12	4 109.26	155.37	32.42	8.53	0.56	0.10	3.92	−	8.53	0.35	−54.48	−7.72		Cl-Na
	BD- QS-003	2018.04	31	7.89	11 545.4	597.92	6 252.55	3.76	489.03	46.07	4 245.12	155.61	31.75	18.79	0.58	0.12	4.02	−	8.76	0.36	−63.7	−9.5	−6.83	Cl-Na
盐场河地热田	ZK01	2017.12	26.5	7.66	9 379.1	531.90	5 003.53	16.3	451.63	53.31	3 397.11	149.52	34.23	5.33	0.00	0.06	2.95	1.14	2.48	0.30	−62.34	−9.31		Cl-Na
	ZK02	2018.04	32	7.79	12 477.7	655.25	6 773.64	5	504.18	49.51	4 598.92	163.19	33	18.87	0.62	0.10	4.21	−	8.80	0.37	−63.1	−9.6	−8.11	Cl-Na
	ZK03	2018.05	34.5	7.52	10 968.7	577.63	5 933.04	9.55	454.68	44.42	4 028.19	151.04	31.82	18.53	0.55	0.11	3.81	4.93	8.64	0.34	−62.9	−9.4	−8.13	Cl-Na
	ZK04	2018.04	30.5	7.62	10 839.6	604.5	5 852.33	2.12	452.48	44.17	3 973.4	155.13	33.09	17.79	0.55	0.09	3.8	3.39	8.30	0.34	−62.9	−9.5	−8.06	Cl−Na
冷泉	SW006	2017.12	16.6	7.49	345	384.97	4.96	1.15	17.5	6.53	1.59	80.45	31.05	7.54	0.00	0.05	0.14	0.26	3.52	0.00	−	−		HCO₃- Ca+Mg
	SW007	2017.12	18	7.83	271.3	307.02	5.01	3.49	9.27	6.23	1.47	52.87	30.73	7.2	0.01	0.01	0.04	0.09	3.36	0.00	−	−		HCO₃- Ca+Mg
	SW023	2017.12	16.3	7.45	155.4	119.01	5.55	13.99	11.12	0.14	0.15	2.03	0.22	10.24	0.00	0.00	0.14	0.09	4.77	0.00	−	−		HCO₃- Ca
	SW027	2018.04	18.5	7.84	237.4	254.43	4.7	52.38	11.03	5.73	1.2	47.9	24.6	7.06	0.00	0.04	0.10	0.17	3.29	0.00	−	−		HCO₃− Ca+Mg
河水	BD- HL001	2017.08	−	−	−	−	−	−	−	−	−	−	−	−	−	−	−	−	−	−	−59.98	−9.06	−11.5	−
雨水	BD- YS001	2018.04	−	−	−	−	−	−	−	−	−	−	−	−	−	−	−	−	−	−	−8.00	−1.40	−	−
注：单位水温为℃，pH为无量纲，其他为mg·L ⁻¹。钻孔监测为出水口温度。 Note: The unit of water temperature is ℃; pH is dimensionless; others are mg·L−1. Borehole monitoring is the temperature of water outlet.

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表 4 同位素补给高程统计表

Table 4. Statistics of isotope recharge elevation

名称	采样点	类型	δD/‰	补给高程/m
盐场河地热田	ZK01	地热流体	−62.34	1 261.21
	ZK02	地热流体	−63.1	1 281.71
	ZK03	地热流体	−62.9	1 274.30
	ZK04	地热流体	−62.9	1 298.25

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表 5 各矿物组分饱和指数一览表

Table 5. Saturation index of mineral components

	神农温泉						ZK04		ZK02		ZK03
矿物组分	2017.08取样		2018.04取样		2017.11取样		2018.04取样		2018.04取样		2018.05取样
	模拟反应		模拟反应		模拟反应		模拟反应		模拟反应		模拟反应
	前	后	前	后	前	后	前	后	前	后	前	后
硬石膏	−1.79	0	−1.54	0	−1.54	0	−1.56	0	−1.53	0	−1.57	0
文石	0.37	−0.14	−0.1	−0.14	−0.1	−0.14	−0.09	−0.14	−0.06	−0.14	−0.12	−0.14
方解石	0.51	0	0.04	0	0.04	0	0.05	0	0.09	0	0.02	0
玉髓	−0.35	−0.43	−0.25	−0.43	−0.25	−0.43	−0.28	−0.43	−0.25	−0.43	−0.26	−0.43
温石棉	−8.37	−11.59	−8.01	−11.59	−8.01	−11.59	−7.99	−11.59	−7.98	−11.59	−8.01	−11.59
白云石	0.72	0	−0.24	0	−0.24	0	−0.19	0	0.15	0	−0.26	0
萤石	/	/	/	/	/	/	−0.2	0	/	/	0.12	0
石膏	−1.57	0.17	−1.33	0.17	−1.33	0.17	−1.34	0.17	−1.32	0.17	−1.36	0.17
石盐	−3.68	−1.91	−3.34	−1.86	−3.34	−1.86	−3.39	−1.87	−3.28	−1.87	−3.38	−1.87
石英	0.07	0	0.18	0	0.18	0	0.15	0	0.18	0	0.17	0
菱锰矿	−0.73	−2.56	−1.10	−2.41	−4.82	−8.73	−1.10	−2.43	−1.05	−2.39	−1.12	−2.43
滑石	−5.37	−8.73	−4.82	−8.73	−1.1	−2.42	−4.85	−8.73	−4.77	−8.73	−4.83	−8.73
注：以上数据均为无量纲。 Note: Above data are all dimensionless.

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表 6 水化学温标计算表

Table 6. Calculation of hydrochemistry temperature scales

项目（℃）	神农温泉		ZK04	ZK02	ZK03
项目（℃）	2017.08	2018.04	2018.04	2018.04	2018.05
二氧化硅温标	53.45	61.11	61.28	59.10	60.59
Na-K温标	69.02	48.85	50.02	48.47	49.63
K-Mg温标	93.98	90.32	88.70	91.70	89.35
Na-K-Ca温标	113.29	98.41	99.28	98.12	98.99
热储层温度	59.11

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参考文献(22)

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