海南陵水英州−新村高氟高盐度地热系统成因机制

王江思; 王文梅; 甘浩男; 林师兴; 欧阳正平; 马海涛; 王贤峰; 王晓林; 王项; 王月蕾; 常振宇

doi:10.19509/j.cnki.dzkq.tb202607024

海南陵水英州−新村高氟高盐度地热系统成因机制

doi: 10.19509/j.cnki.dzkq.tb202607024

王江思^{1, 2, 3,},
王文梅^{1, 2, ,},
甘浩男^{1, 4},
林师兴^{1, 2},
欧阳正平^{1, 2},
马海涛^{1, 2},
王贤峰^{1, 2},
王晓林^{2, 3},
王项^{1, 2},
王月蕾²,
常振宇²

海南省海洋地质资源与环境重点实验室，海口 570206
海南省生态环境地质调查院，海口 570206
海南省地质局，海口 570206
中国地质科学院水文地质环境地质研究所，石家庄 050061

基金项目: 海南省海洋地质资源与环境重点实验室开放课题（25-HNHYDZZYHJK F059）；深地国家科技重大专项课题“中高温地热资源评价与开发目标优选”（2025ZD1010004）

详细信息

作者简介:
王江思：E-mail：zcqy_w@163.com

通讯作者:
E-mail：wmhn_w@163.com

中图分类号: P641.3；P592
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- 文章访问数: 71
- PDF下载量: 5
- 被引次数: 0
出版历程
- 收稿日期: 2026-07-08
- 录用日期: 2026-08-27
- 修回日期: 2026-08-13
- 网络出版日期: 2026-08-28

Genetic mechanism of a high-fluoride and high-salinity geothermal system in Yingzhou-Xincun area, Lingshui, Hainan Province

WANG Jiangsi^{1, 2, 3
,},
WANG Wenmei^{1, 2
, ,},
GAN Haonan^{1, 4},
LIN Shixing^{1, 2},
OUYANG Zhengping^{1, 2},
MA Haitao^{1, 2},
WANG Xianfeng^{1, 2},
WANG Xiaolin^{2, 3},
WANG Xiang^{1, 2},
WANG Yuelei²,
CHANG Zhenyu²

Hainan Key Laboratory of Marine Geological Resources and Environment, Haikou 570206, China
Hainan Ecological Environment Geological Survey Institute, Haikou 570206, China
Hainan Bureau of Geology, Haikou 570206, China
Institute of Hydrogeology and Environmental Geology, Chinese Academy of Geological Sciences, Shijiazhuang 050061, China

More Information

Author Bio:
E-mail：zcqy_w@163.com

Corresponding author: E-mail：wmhn_w@163.com

摘要

摘要:
海南岛东南部陵水英州−新村地区广泛赋存中高温高氟地热系统，但氟组分与盐分负向耦合的机制尚不明确，制约了区域地热资源精细化开发。为揭示研究区 3 处地热田的地热水成因、空间分布规律及氟−盐负向耦合形成机理，以高峰、红鞋、新村 3 处地热田为研究对象，综合采用水化学组分测试、同位素示踪及水文地球化学模拟等方法开展多端元流体溯源与水−岩作用解析。结果表明：①受九所−陵水深大断裂分段控热控组分作用制约，研究区为中生代花岗岩裂隙型地热系统，地热流体源自北部低山丘陵区大气降水，补给高程 989～1150 m，地下水年龄 2844～13444 a，热储温度 125～165 ℃，呈内陆高、滨海低的空间分异；②地热水总溶解固体（TDS）最高可达 2600 mg/L，高盐度特征与现代海水入侵无关，TDS自内陆向滨海呈递增；盐分来源受控于深部封存古海相流体与花岗岩硅酸盐矿物溶滤，阳离子交换进一步放大了地下水咸化的空间分异；③地热水 F⁻质量浓度为2.6～12.8 mg/L，由内陆向滨海递减；Ca²⁺活度是氟富集主控因素，HCO₃⁻为辅助因子，温度起增效作用；古海相富钙流体混入诱发萤石沉淀是滨海低氟的关键诱因，最终形成全区 F⁻与 TDS，Cl⁻显著负耦合的分布规律。本研究厘清了滨海花岗岩地热系统氟、盐负耦合成因机理，填补海南滨海花岗岩地热系统氟−盐耦合演化机理的研究空白，可为华南滨海高氟高盐地热资源可持续开发提供理论依据。
- 陵水英州–新村 /
- 地热水 /
- 花岗岩裂隙型地热系统 /
- 古海相流体 /
- 氟、盐负向耦合机理 /
- 水文地球化学特征
Abstract:
Objective
Medium-to-high temperature fractured granite-hosted geothermal systems with elevated fluoride concentrations are widely developed in the Yingzhou-Xincun area of Lingshui, southeastern Hainan Island, representing a major occurrence of coastal geothermal resources in South China. Regional geothermal investigations have revealed a prominent negative coupling between fluoride and salinity in geothermal waters. Nevertheless, the genetic mechanism underlying this distinctive hydrogeochemical phenomenon remains poorly understood, which prevents an accurate characterization of hydrochemical evolution and greatly restricts the refined assessment, rational planning, and sustainable exploitation of regional geothermal resources. This study focuses on three representative geothermal fields, namely Gaofeng, Hongxie, and Xincun geothermal fields. It systematically investigates the recharge origin, formation genesis, and thermal reservoir evolution of geothermal water, characterizes the spatial variations in hydrochemical constituents, and elucidates the intrinsic mechanism governing the negative coupling between fluoride and salinity, thereby providing observational constraints and theoretical references for the scientific development and protection of regional geothermal resources.
Methods
Based on field surveys and systematic water sampling, multiple approaches including hydrochemical analysis, isotope tracers, and hydrogeochemical modelling were integrated. A multi-dimensional analysis of fluid provenance, water-rock interactions, ionic migration and transformation, and multi-end-member fluid mixing was performed to interpret the genesis and compositional evolution of the geothermal system.
Results
① The geothermal system, constrained by the segmental heat-controlling and component-controlling effect of the Jiusuo-Lingshui deep major fault, was classified as a typical fractured geothermal reservoir hosted in Mesozoic granite. Geothermal fluids were recharged by infiltrating meteoric precipitation from low hilly terrain in the northern study area. Estimated recharge elevations ranged from 989 m to 1150 m, groundwater residence ages varied from 2844 a to 13444 a, and reservoir temperatures fell between 125 ℃ and 165 ℃, showing a spatial pattern with higher values inland and lower values toward the coast. ② The total dissolved solids (TDS) of geothermal water reached up to 2 600 mg/L, and the high salinity was unrelated to modern seawater intrusion. TDS generally increased progressively from inland to coastal zones. Salinity originated from mixing of deeply sequestered paleo-marine fluids and water-rock leaching of silicate minerals in granite. Cation exchange during groundwater circulation further amplified spatial contrasts in groundwater salinization. ③ Dissolved fluoride concentrations in geothermal water ranged from 2.6 mg/L to 12.8 mg/L and decreased gradually from inland to the coast. The activity of aqueous Ca²⁺ was the primary control on fluoride enrichment and mobilization. Bicarbonate (${\mathrm{HCO}}_3^- $) acted as an important secondary control, and elevated reservoir temperature substantially promoted fluoride release from mineral phases. Mixing of deeply sequestered Ca-rich paleo-marine fluids within coastal zones induced fluorite precipitation, the dominant driver of low fluoride concentrations in coastal geothermal water. This process ultimately yielded a pronounced negative coupling between F⁻ and both TDS and Cl⁻ across the entire study area.
Conclusion
This study systematically clarifies the genetic mechanism for negative coupling between fluoride and salinity in coastal granite-hosted geothermal systems. It fills the knowledge gap of the fluoride-salinity coupling evolution mechanism for coastal granite-hosted geothermal systems on Hainan Island and provides an important theoretical foundation for detailed exploration, rational exploitation, and sustainable utilization of high-fluoride, high-salinity geothermal resources in coastal South China.
- Yingzhou-Xincun area of Lingshui /
- geothermal water /
- fractured granite-hosted geothermal system /
- paleo-marine fluid /
- fluoride-salinity negative coupling mechanism /
- hydrogeochemical characteristics

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图 1 区域地质、地热田位置及采样点分布

Figure 1. Distribution map of regional geology, geothermal field locations, and sampling points

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图 2 地热水水化学组分spearman相关性

Figure 2. Spearman correlation diagrams of hydrochemical components in geothermal water

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图 3 地热水水化学Piper三线图

Figure 3. Hydrochemical Piper trilinear diagrams of geothermal water in the study area

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图 4 研究区地热水水文地球化学成因判别图（γ. 离子毫克当量浓度；下同）

Figure 4. Hydrogeochemical origin discrimination map of geothermal water in the study area

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图 5 研究区地热水阳离子交换作用判别图

Figure 5. Cation exchange potential discrimination diagram for geothermal water in the study area

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图 6 研究区热水样品F⁻离子饱和指数关系图

Figure 6. Relationship between F⁻ and saturation index of geothermal water samples in the study area

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图 7 研究区地热流体氟离子与主要离子、温度相关关系图（T. 温度；α. 离子活度）

Figure 7. Correlations between fluoride ion, main ions, and temperature of geothermal fluids in study area

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图 8 水文地球化学相演化图（HFE-D）（图中数值均为离子毫克当量百分比，%）

Figure 8. Hydrochemical facies evolution diagram (HFE-D)

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图 9 研究区地热水Na-K-Mg阳离子三线图

Figure 9. Na-K-Mg cation trilinear diagram of geothermal water in study area

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图 10 研究区热水井的多种矿物饱和指数（SI）与温度关系图

Figure 10. Relationship between saturation index (SI) and temperature of various minerals in thermal well water at the study area

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图 11 地下热水的δD-δ¹⁸O关系图

Figure 11. δD-δ¹⁸O relationship of geothermal groundwater

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图 12 研究区地热成因模式概念模型

Figure 12. Conceptual model of geothermal genesis in study area

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表 1 海南陵水英州−新村地区水化学组分

Table 1. Hydrochemical components in Yingzhou–Xincun area, Lingshui, Hainan Province

序号	编号	pH值	温度/(℃）	TDS	Na⁺	K⁺	Mg²⁺	Ca²⁺	F⁻	Cl⁻	SO₄²⁻	HCO₃⁻	Br⁻⁻	SiO₂	水化学类型	平衡差/%
序号	编号	pH值	温度/(℃）	ρ_B/(mg·L⁻¹)											水化学类型	平衡差/%
1	G1	8.37	53.0	546	126	5.0	0.38	15.2	9.90	93.1	58.3	101.0	0.31	115.0	Cl.HCO₃−Na	3.3
2	G2	8.33	50.0	576	135	5.3	0.36	15.0	11.30	93.6	58.6	120.0	0.31	115.0	Cl .HCO3-Na	3.0
3	G3	8.31	70.0	765	181	7.2	1.10	39.8	7.80	232.0	64.9	118.0	0.79	100.0	Cl-Na	−0.4
4	G4	7.86	48.5	856	193	7.6	1.50	28.7	8.90	158.0	107.0	219.0	0.43	132.0	Cl.HCO₃−Na	−2.6
5	G5	8.32	71.6	535	119	6.6	0.06	6.6	12.80	71.8	63.4	75.8	0.23	157.0	Cl.SO4.HCO3-Na	4.0
6	G6	7.78	30.0	1446	359	13.3	2.80	141.0	4.70	683.0	90.2	70.2	2.44	82.0	Cl-Na.Ca	1.5
7	G7	8.44	46.0	788	203	10.3	0.29	22.9	9.00	256.0	71.7	96.6	0.81	115.0	Cl-Na	−2.3
8	G8	8.45	54.5	703	165	8.0	0.50	20.8	9.40	150.0	76.5	149.0	0.45	121.0	Cl.HCO₃−Na	−1.5
9	G9	8.36	56.5	801	195	8.3	0.75	39.1	8.50	270.0	68.6	105.0	0.87	103.0	Cl-Na	−2.2
10	G10	5.36	29.0	161	18.1	6.1	2.30	4.1	<0.02	14.6	2.5.0	26.0	<0.016	53.4	HCO₃.Cl-Na	20.6
11	H1	7.77	53.2	1040	270	9.4	0.50	58.4	7.00	408.0	132.0	70.2	1.47	84.4	Cl-Na	−2.7
12	H2	7.21	35.7	1304	335	11.9	3.40	87.6	6.10	562.0	124.0	87.0	1.92	84.1	Cl-Na	−1.6
13	H3	6.48	50.5	955	234	7.8	1.80	63.1	4.50	370.0	89.4	112.0	1.37	70.7	Cl-Na	−2.4
14	H4	6.44	28.2	663	65.6	1.6	12.10	76.5	0.97	63.0	21.5	358.0	<0.016	63.6	HCO₃−Ca.Na	−2.0
15	H5	6.93	28.5	1187	178	7.2	17.20	141.0	2.20	366.0	79.5	322.0	<0.016	70.7	Cl.HCO₃−Na.Ca	−2.6
16	X1	8.01	41.5	2600	620	21.0	9.50	311.0	3.30	1350.0	106.0	71.2	2.00	108.0	Cl -Na.Ca	2.6
17	X2	7.45	42.7	2540	603	25.2	9.00	271.0	2.60	1380.0	93.6	81.3	1.80	73.8	Cl -Na.Ca	−1.4
18	X3	8.33	40.5	2330	549	19.2	7.60	256.0	3.00	1240.0	93.7	79.8	0.90	73.4	Cl -Na.Ca	−0.7
19	X4	6.58	25	106	8.5	2.5	1.30	6.9	0.19	15.0	4.0	38.0	/	24.6	HCO3.Cl-Na.Ca	−12.0
20	X5	6.69	27.6	164	18	2.4	4.00	13.4	0.23	19.7	14.8	62.2	/	22.5	HCO3.Cl-Na.Ca	−0.8
注： G表示高峰地热田，H表示红鞋地热田，X表示新村地热田，“/”表示未检测，G10，H4，H5，X4，X5为常温地下水，其余为温泉或地热钻孔水。G9，H2，H5 为村民自建家用洗浴民井，采用机泵抽水开采，其余地热点保持自然状态，以自流出水为主，无机械开采活动。所有地热水电荷平衡均<5%，其中G10增加硝酸盐后平衡2.9%，X4电荷平衡误差较大可能受人为污染影响

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表 2 特征离子比

Table 2. Characteristic ion ratios

编号	Na⁺/Cl⁻	Br⁺/Cl⁻	Ca²⁺/Sr⁺	Mg²⁺/Ca²⁺	编号	Na⁺/Cl⁻	Br⁺/Cl⁻	Ca²⁺/Sr⁺	Mg²⁺/Ca²⁺
G1	2.09	1.47×10⁻³	127.33	0.04	H1	1.02	1.60×10⁻³	286.51	0.01
G2	2.23	1.4×10⁻³	131.69	0.04	H2	0.92	1.52×10⁻³	342.66	0.06
G3	1.20	1.51×10⁻³	210.58	0.05	H3	0.98	1.65×10⁻³	164.55	0.05
G4	1.89	1.20×10⁻³	178.85	0.09	H4	1.61	0.00	578.84	0.26
G5	2.56	1.44×10⁻³	101.45	0.02	H5	0.75	0.00	571.96	0.20
G6	0.81	1.59×10⁻³	262.86	0.03	X1	0.71	6.58×10⁻⁴	243.30	0.05
G7	1.22	1.41×10⁻³	197.49	0.02	X2	0.67	5.80×10⁻⁴	215.86	0.06
G8	1.70	1.34×10⁻³	194.71	0.04	X3	0.68	3.22×10⁻⁴	197.11	0.05
G9	1.11	1.42×10⁻³	198.72	0.03	X4	0.87	0	/	0.31
G10	1.91	0	101.48	0.93	X5	0.54	0	/	0.25

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表 3 研究区热储温度计算成果表

Table 3. Results of geothermal reservoir temperature calculation in study area

取样点编号	玉髓	石英	Na-K	K-Mg	Na-K-Ca	硅焓图解法	考虑最大蒸汽损失硅焓图解法	多矿物平衡法^[43]
G1	119	145	168	91	252	272	177	158
G2	119	145	167	94	253	283	183	160
G3	110	137	168	87	249	202	147	152
G4	128	153	167	84	254	319	199	154
G5	141	164	189	126	287	272	174	165
G6	99	126	164	91	245	335	/	135
G7	119	145	183	115	277	301	193	155
G8	123	148	180	100	270	276	178	158
G9	112	139	172	96	256	240	163	151
H1	100	128	160	105	244	207	/	141
H2	100	128	161	85	246	280	143	142
H3	90	119	158	83	237	183	183	135
X1	63	93	159	87	242	175	126	130
X2	64	95	171	92	259	250	/	125
X3	62	92	160	87	244	259	/	125
注：石英（无蒸汽损失）^[44]，T=1309/[5.19−lg(SiO₂)]−273.15；玉髓（无蒸汽损失）^[44]，T=1032/[4.69−lg(SiO₂)]−273.15；Na-K^[44]，T=1390/(1.75+lg([Na⁺]/[K⁺])−273.15；K-Mg^[44]，T=4410/13.95−\lg([K⁺]²/[Mg²⁺])}−273.15；Na-K-Ca^[44-45]，$ T=1\;647/[\lg ([{{\mathrm{Na}}}^{+}]/[{{\mathrm{K}}}^{+}])+\beta \lg ({[{{{\mathrm{Ca}}}^{2+}}]}^{0.5}/[{{\mathrm{Na}}}^{+}])+2.24]- 273.15 $，若T<100℃，β=4/3，T>100℃和$ \lg ({\left(\left[{{\mathrm{Ca}}}^{2+}\right]\right)}^{0.5}/[{{\mathrm{Na}}}^{+}] $<0，β=1/3；石英温标（最大蒸汽损失）^[44]，$ T=1\;522/[5.75-\lg ({{\mathrm{SiO}}}_{2})]-273.15 $

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表 4 研究区氘氧同位数

Table 4. Hydrogen and oxygen isotopes in study area

取样点编号	¹⁸O	D	取样点高程/m	补给高程/m
G3	−7.61	−50.89	26	1150
G9	−7.94	−50.34	25	1128
H1	−7.8	−49.17	30	1086
H5	−7.49	−46.59	36	989
XC(雨水)	−4.13	−23.5	29	/

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表 5 研究区地热水¹⁴C年龄校正结果

Table 5. ¹⁴C age correction results of geothermal water in study area

取样点编号	¹⁴C活度/pMC	δ¹³C/‰	Vogel模型校正/a	Tamers模型校正/a	Pearson模型校正/a	Gonfiantinie模型校正/a	Mook模型校正/a	热水年龄/a
G3	58.37	−17.49	3580	−1180	1497	2844	6871	2844
G5	15.92	−17.3	14320	9559	12148	13444	17444	13444
G8	53.71	−17.54	4268	−519	2209	4081	7629	4081
G9	34.97	−17.8	7815	3045	5878	7677	11385	7677
H1	20.37	−18.48	12283	7755	10656	12575	16194	12575
X1	41.00	未测试	6500	1836	/	/	/	6500
注：pMC. 现代碳百分比；“/”表示未测试¹³C的含量，无法计算地下水年龄

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