Front. Earth Sci. Frontiers in Earth Science Front. Earth Sci. 2296-6463 Frontiers Media S.A. 872620 10.3389/feart.2022.872620 Earth Science Original Research Effects of Seawater Recharge on the Formation of Geothermal Resources in Coastal Areas and Their Mechanisms: A Case Study of Xiamen City, Fujian Province, China Liu et al. Seawater-Recharged Geothermal System Liu Chunlei 1 2 Li Yasong 1 2 Cao Shengwei 1 2 Wang Wanli 1 Li Jing 3 * 1 The Institute of Hydrogeology and Environmental Geology, Chinese Academy of Geological Science, Shijiazhuang, China 2 Fujian Provincial Key Laboratory of Water Cycling and Eco-Geological Processes, Xiamen, China 3 Faculty of Environment, China University of Geosciences, Wuhan, China

Edited by: Dawei Hu, (CAS), China

Reviewed by: Walter D'Alessandro, National Institute of Geophysics and Volcanology, Section of Palermo, Italy

Kunal Singh, Geological Survey of India, India

 *Correspondence: Jing Li, lijing915@cug.edu.cn

This article was submitted to Geochemistry, a section of the journal Frontiers in Earth Science

 15 06 2022 2022 10 872620 09 02 2022 23 05 2022 Copyright © 2022 Liu, Li, Cao, Wang and Li. 2022 Liu, Li, Cao, Wang and Li

This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.

The southeast coastal areas of China have abundant geothermal resources. Most especially, seawater-recharged geothermal systems in the coastal areas have large quantiles of recharge but suffer water salinization and low water temperature. Moreover, the geothermal water development in these areas may induce seawater intrusion. Understanding the genetic patterns of geothermal resources is significant for rational exploration and protection. This study analyzed the hydrochemical and environmental isotopic characteristics of geothermal water, groundwater, and surface water samples collected in the area with geothermal resources in Xiamen Province in the southeast coastal areas of China. Based on this, the recharge of geothermal water circulation and the genetic patterns of geothermal resources were revealed. The results of this study indicate that the geothermal water in mountainous areas and piedmonts in Xiamen is mainly recharged by rainfall infiltration. In contrast, the geothermal water in coastal areas in Xiamen is recharged by seawater mixing to different extents, as indicated by hydrochemical types, isotopic characteristics, and the C1-/Br- ratio of geothermal water. As revealed by the calculation results using the Cl− mixing model, 10 of 13 geothermal fields in Xiamen are recharged by seawater mixing, with a mixing ratio of up to 73.20% in the Pubian geothermal field. After being recharged by rainfall in the low mountainous areas, geothermal water migrates toward deep parts along NW-trending faults. Then, it converges with regional NE-trending deep faults to absorb heat conducted from deep parts to form deep geothermal reservoirs. The deep geothermal reservoirs were estimated to be 185–225°C using the silica-enthalpy mixing model. The geothermal water is mixed with cold water or seawater while rising along faults. The temperature of shallow geothermal reservoirs was estimated to be 71–145°C using SiO2 geothermometers.

 geothermal water environmental isotope geochemical geothermometer seawater recharge genesis of geothermal resources 1 Introduction

Geothermal resources are new green energy resources that integrate heat, water, and minerals. They are rich and cause low-level environmental pollution compared to fossil energy resources. However, geothermal water with high salinity and high concentrations of As, Hg, F, and H2S also poses risks of environmental pollution (Giggenbach, 1988; Ozgener and Kocer, 2004; Armienta et al., 2014). In the southeast coastal areas of China, which are in great demand for energy resources, the development and utilization of geothermal energy is an important measure for promoting sustainable urban development (Lin, 2007; Lin et al., 2016; Lin et al., 2020). The hydrothermal systems in southeast coastal areas of China circulate as follows. Faults develop in the low-permeability granite basement, and the atmospheric precipitation is heated through deep circulation in these faults and then rises to the Earth surface (Han and Zhuang, 1988; Hu and Xiong, 1990; Xiong et al., 1990; Liao, 2012; Gan, 2017; Gan et al., 2020). However, geothermal water in some coastal areas in Southeast China shows noticeable salinization and is rich in heavy isotopes, indicating the recharge by seawater mixing (Gao et al., 2009; Wang, 2018). Any changes in interactions between groundwater and seawater—the primary recharge factors of geothermal systems in coastal areas—will directly affect the quantity and quality of geothermal resources in coastal areas. The increase in mixed seawater may lead to a significant increase in the salinization and a decrease in the temperature of the geothermal water. By contrast, the decrease in the mixed seawater may lead to the depletion of geothermal resources. In this case, the exploitation of large amounts of geothermal water may cause the high salinization of geothermal water and seawater intrusion. The depletion and water quality deterioration of geothermal resources induced by the exploration of geothermal reservoirs in the southeast coastal areas of China can be effectively prevented by studying the formation conditions of seawater-recharged hot water systems and the genetic patterns of geothermal water and deeply understanding the formation and evolutionary patterns of low-medium temperature convective geothermal systems in these areas.

Southeast coastal areas are among the geothermal active areas with the most considerable potential for the development and utilization of geothermal resources in South China. These areas have widely distributed Mesozoic volcanic rocks and granites (Xiong et al., 1991; Zhang et al., 2018; Lin, 2022), abundant regional geothermal resources, and a ternary heat accumulation pattern consisting of the radioactive heat production by acidic rocks, heat transfer by faults, and heat retention by cap rocks (Li et al., 2020). Geothermal anomalous areas in southeast coastal areas are all located in low-lying areas such as intermountain basins, stream valleys, and plains. As indicated by the characteristics of the geothermal field in the geothermal anomalous areas, as well as the features of pores in strata, rock joints, and tectonic fractures (Qiu, 2018), the geothermal fields in the Southeast coastal areas lie at the intersections of NNW- and NE/NEE-trending faults (Han and Zhuang, 1988; Fan et al., 1993; Zhang et al., 2020). Among them, the NE -trending faults are major regional geothermal-controlling structures, while NEE- and EW-trending tensional faults serve as major regional water-conducting structures (Ma et al., 2021). As calculated using no-steam loss quartz thermometers, the hot springs in Zhangzhou-Xiamen areas have geothermal reservoir temperatures of 106–149°C and circulation depths of approximately 3400–5100 m (Lin et al., 2020). The recharge and salinization of geothermal water in coastal areas have always been controversial. The chemical and isotopic studies show that, in the Zhangzhou area, which is adjacent to the study area, the atmospheric precipitation mixes with seawater in the deep parts of geothermal fields, leading to a significant increase in the salinity of geothermal water and accordingly the formation of saline water (Pang, 1987). Existing studies are mainly focused on the genesis of geothermal resources from the regional structures and hydrochemical isotopic characteristics of geothermal fields and the estimation of geothermal reservoir temperature. However, few studies have been conducted on the genesis of geothermal sources and the recharge, runoff, and discharge conditions of geothermal fluids. Most especially, the contribution of seawater recharge to the formation of geothermal resources is yet to be ascertained. This study revealed the recharge mechanisms of geothermal water circulation and the genetic patterns of geothermal resources and will assist in effectively preventing and controlling the resource and environment problems such as geothermal water salinization, seawater intrusion, and the decrease in the geothermal water caused by geothermal water exploration and utilization.

 2 Regional Geological Background

The study area lies in the coastal area in southeastern Fujian Province. It has a subtropical monsoon climate, with an average annual temperature of 20.8°C, an extreme maximum temperature of 38.4°C, and average annual rainfall of 1347.8 mm. Xiamen City lies at the eastern margin of the Cathaysia block of the South China Plate and in the zone where the southeastern margin of the Eurasian Plate interacts with the Pacific Plate (Wang et al., 1993). Because of the intensive and frequent Yanshanian magmatic activities, polyphasic rock masses were formed and widely distributed in the study area. Moreover, the Late Jurassic magmatic activities occurred on the largest scale among the Yanshanian magmatic activities. As a result, highly radioactive acidic Late-Jurassic and Early-Cretaceous granites are widely developed in the study area (Wang et al., 1996). Because of the large-scale Yanshanian magmatic activities, the deep Zhenghe-Dapu Fault Zone and the coastal deep Dongshan Island—Nan’ao Island Fault Zone extend from hundreds of kilometers to more than 1000 km in the NE and NNE directions. They have a long history of multi-stage orogenic activities and are increasingly active in areas closer to the coast (Wang, 1985). The movement of the Philippine Plate in the NW direction caused these deep faults to slide leftward or suffer compression and torsion, leading to the formation of a set of tensional or transtensional faults in the NW direction (Figure 1).

Geological sketch of Xiamen and the distribution of sampling points.

The study area shows sporadic hydrogeological units, most of which are independent or semi-independent. The groundwater in these hydrogeological units is mainly recharged by atmospheric precipitation and discharges into the sea through short runoff. It can be divided into water in loose-rock porous rocks, water in mesh fractures of weathered zones, and water in bedrock fractures. The former two types of water are primarily distributed in shallow alluvial-diluvial and weathered eluvial strata. The water in bedrock fractures mainly occurs in joints and tectonic cracks in Yanshanian granites and Jurassic volcanic rocks.

 3 Sample Collecting and Testing

Thirteen water samples were collected from geothermal wells with depths of 48.6–500.8 m in the study area. Thirty-four water samples were collected from cold groundwater along the runoff direction of groundwater in the hydrological units of geothermal wells, including 26 samples of water in loose porous rocks (corresponding well depth: 3–25 m) and eight samples of water in bedrock fractures (corresponding well depth: 31–120 m). In addition, eight surface water samples were collected from rivers in the main recharge and discharge areas of groundwater and four samples were collected from seawater (Figure 1). The water temperature, pH, and electrical conductivity were measured on-site using the portable Eureka Manta2 water quality recorder. Water samples were stored in clean polyethylene bottles after being filtered using Millipore membrane filters with a pore size of 0.45 μm. Then, they were tested for anions, cations, and hydrogen and oxygen isotopes at the Key Laboratory of Groundwater Science and Engineering, Ministry of Natural Resources. Cations and anions SO4 2- and Br− were tested using the ICP-OES spectrometer (iCAP-6300) and the Dionex ICS-1500 ion chromatography system, respectively, with testing accuracy of 1% and charge-balance error of 5% or less. Anion Cl− was tested using the titrimetric method, and SiO2 was tested using UV-2550 spectrophotometer according to the silicon molybdenum yellow spectrophotometry. Using the method of wavelength-scanned optical cavity ring-down spectroscopy, hydrogen and oxygen isotopes were detected at a temperature of 22°C and relative humidity of 40% with the Picarro L2130-i isotope analyzer. The detection accuracy was 0.2‰ for δ18O and 2‰ for δ2H. The testing results are shown in Table 1.

List of hydrochemical characteristics of groundwater in Xiamen.

No. Type Well depth T pH TDS K+ Na+ Ca2+ Mg2+ Cl− SO4 2- HCO3 − CO3 2- Br− SiO2 δ2H δ18O
m (°C) (ppm) (ppm) (ppm) (ppm) (ppm) (ppm) (ppm) (ppm) (ppm) (ppm) (ppm) (‰) (‰)
G01 Cold Groundwater 3.0 26.2 7.02 550 46.3 33.3 96.8 11.1 34 70.3 285 0 <0.10 34.5 −33 −5.4
G02 Cold Groundwater 10.0 24.5 6.4 433 7.06 52 50.1 17.4 61.3 35.2 121 0 <0.10 29 −41 −6.5
G03 Cold Groundwater 44.0 25.4 6.78 248 4.68 14.3 59.6 4.15 17.5 31.5 170 0 <0.10 23.3 −33 −5.1
G04 Cold Groundwater 24.0 25.9 5.88 179 12.9 27.7 11.5 2.48 38.4 20.7 17.7 0 <0.10 28.3 −42 −6.4
G05 Cold Groundwater 11.0 24.6 4.55 222 0.86 27.1 31.3 3.83 40.3 14.1 6.07 0 <0.10 7.81 −38 −5.9
G06 Cold Groundwater 10.0 24.7 7.14 132 1.28 10.7 25.7 2.22 8.73 14.6 88.5 0 <0.10 19.6 −33 −4.7
G07 Cold Groundwater 10.0 24.8 5.35 174 3.2 19.6 21.8 4.06 30.5 9.36 18.2 0 <0.10 14.1 −38 −5.9
G08 Cold Groundwater 10.0 25.9 7.41 555 2.01 64.2 113 13.5 89.3 80.2 309 0 <0.10 22.3 −32 −5.2
G09 Cold Groundwater 38.0 26.8 6.72 98.3 3.75 9.33 4.46 0.92 5.24 3.13 30.5 0 <0.10 49.2 −42 −6.5
G10 Cold Groundwater 10.0 25.7 5.5 181 3.22 11.8 29.3 4.1 15.8 1.91 54.6 0 <0.10 20.6 −43 −6.6
G11 Cold Groundwater 25.0 25.9 6.17 71.5 4.44 9.48 4.08 0.3 8.73 2.47 18.3 0 <0.10 17.7 −34 −5.3
G12 Cold Groundwater 25.0 25.4 6.82 422 5.47 45.5 74.7 8.04 64.8 32.8 150 0 <0.10 11.9 −36 −5.6
G13 Cold Groundwater 13.0 25.1 6.28 244 29.3 36.7 18.4 2.44 41.9 48.3 55.5 0 <0.10 19.2 −37 −5.8
G14 Cold Groundwater 10.0 24.8 6.31 324 52.9 41.3 18.3 3.25 47.9 57.4 30.5 0 <0.10 4.42 −39 −5.9
G15 Cold Groundwater 9.5 25.5 5.86 107 6.04 12 7.98 1.09 15.4 4.87 24.3 0 <0.10 26 −37 −5.8
G16 Cold Groundwater 9.5 26.1 5.79 84 3.53 7.36 9.35 1.43 12.6 4.09 6.07 0 <0.10 10.4 −40 −6.1
G18 Cold Groundwater 9.0 25 6.61 399 4.32 33.6 69.8 9.25 51 38.2 101 0 <0.10 19 −35 −5.6
G19 Cold Groundwater 31.0 25.8 6.35 348 6.78 60.7 30.1 7.15 102 17.9 48.8 0 <0.10 40.2 −39 −6.1
G20 Cold Groundwater 11.3 25.9 7.08 306 7.88 36.1 45.9 4.39 46.5 41.9 82.4 0 <0.10 21.6 −34 −5.3
G21 Cold Groundwater 9.5 24.5 7.51 366 15.6 47.6 41.1 9.12 59.4 28.5 97.6 0 <0.10 25.9 −38 −5.9
G22 Cold Groundwater 10.0 25.6 7.67 132 5.74 17 6.02 1.63 16.1 3.52 31.7 0 <0.10 47.6 −42 −6.4
G23 Cold Groundwater 15.0 24.5 5.35 236 1.98 47.1 17.7 3.24 61.8 12.5 7.32 0 <0.10 13.2 −42 −6.5
G24 Cold Groundwater 11.0 25.4 7.59 414 26.6 44.6 51.1 9.45 60.4 35.1 98.9 0 <0.10 22 −40 −6.2
G26 Cold Groundwater 10.0 25.9 6.71 279 10.7 33.5 44 3.48 40.2 33.2 99.5 0 <0.10 11.1 −33 −5.2
G27 Cold Groundwater 8.0 25.7 6.88 708 4.96 86.5 131 14.7 114 87.9 250 0 <0.10 7.77 −36 −5.6
G28 Cold Groundwater 11.2 24.7 6.42 339 18.3 36.3 39.6 11.9 40.9 56.1 104 0 <0.10 20.3 −32 −5.2
G29 Cold Groundwater 14.4 24.8 6.3 344 2.53 47.3 37.5 15.2 64.6 54.6 64.1 0 <0.10 12.3 −39 −6.1
G30 Cold Groundwater 100.0 24.3 7.23 249 1.37 22.5 49 5.3 8.03 8.46 190 0 <0.10 52.1 −42 −6.3
G31 Cold Groundwater 120.0 25 6.9 186 2.39 17.3 29.3 4.06 9.43 6.48 122 0 <0.10 45.4 −43 −6.5
G32 Cold Groundwater 105.0 25.2 7.36 172 0.96 14.5 32.2 3.6 4.89 13.9 122 0 1.73 36.4 −47 −7.3
G33 Cold Groundwater 100.0 23.4 7.51 171 0.85 14.8 32.2 3.49 4.89 14.5 122 0 <0.10 36.4 −46 −7.2
G34 Cold Groundwater 100.0 25.1 7.92 251 0.71 58.6 25.8 0.54 21.7 33.5 140 0 <0.10 37.9 −47 −7
H01 Geothermal water 200.4 56.8 7.34 2300 15.9 619 237 0.71 1210 130 33.6 0 3.94 64.1 −48 −7.3
H02 Geothermal water 140.0 51.7 7.36 1100 8.62 332 53.9 0.23 459 108 104 0 1.17 75.4 −43 −6.4
H03 Geothermal water 48.6 48 8.91 301 1.36 85.2 2.84 0.08 14.7 55.8 73.2 18 <0.10 73.2 −51 −7.7
H04 Geothermal water 110.0 37.6 8.07 326 1.71 86 16.4 0.47 56.6 69 88.5 0 <0.10 49.3 −43 −6.5
H05 Geothermal water 150.6 80 7.11 3640 33.4 828 496 1.3 1950 216 48.8 0 6.4 83.4 −42 −6.2
H06 Geothermal water 151.1 47 6.92 8000 59.9 1830 1060 4.17 4630 297 36.6 0 16.5 84.7 −40 −5.9
H07 Geothermal water 160.0 45.5 7.82 391 2.81 112 14.8 0.26 52.4 73.8 142 0 <0.10 56.3 −43 −6.4
H08 Geothermal water 202.0 38.2 6.94 19300 86.4 4040 2940 185 11100 866 45.8 0 35.3 65.9 −29 −4.2
H09 Geothermal water 150.0 53.6 6.65 17600 127 4320 1870 118 10400 609 84.8 0 38.7 79.1 −29 −4.2
H10 Geothermal water 500.8 88.9 6.86 13800 95.3 3520 1410 129 7550 690 67.1 0 27 107 −32 −4.8
H11 Geothermal water 151.5 47.5 8.68 345 1.43 101 4.4 0.35 16.8 101 55.5 18 <0.10 65.3 −49 −7.5
H12 Geothermal water 51.8 48.5 7.17 443 5.72 99.2 16.2 1.9 11.2 136 110 0 <0.10 114 −47 −7
H13 Geothermal water 151.0 68.3 6.5 21100 201 4650 2810 54.9 12500 447 48.8 0 49.2 98.9 −26 −3.8
S01 Surface Water - 33.1 8.24 279 12.5 36.5 43.1 5.38 40.9 44.8 140 0 <0.10 19.3 −37 −5.7
S02 Surface Water - 34.9 9.41 1100 14 147 99.1 2.78 321 49.6 85.4 0 0.92 27.9 −36 −5.3
S03 Surface Water - 30.7 7.4 121 5.73 11.6 18 2.38 11.9 11 73.2 0 0.12 21 −37 −5.7
S04 Surface Water - 34.7 7.89 330 12.6 64.6 34.8 7.92 88.7 39.6 122 0 <0.10 16.1 −36 −5.5
S05 Surface Water - 34.1 7.8 94.9 4.07 9.08 12 1.38 6.99 8.5 48.8 0 <0.10 20.5 −41 −6.4
S06 Surface Water - 32.6 8.04 147 6.37 15.5 19.8 2.84 17.8 17 61 0 <0.10 20.7 −37 −5.9
S07 Surface Water - 33.4 9.03 359 14.2 48.9 50.8 7.36 70.6 43.2 177 0 <0.10 27.3 −33 −4.9
S08 Surface Water - 33.8 8.73 386 14.2 58.8 47.2 7.07 69.2 45 201 0 <0.10 33.4 −32 −4.8
SW01 Seawater - 28.1 7.86 31300 385 9910 353 1140 17200 2330 138 0 55.7 2.92 - -
SW02 Seawater - 28.8 7.87 32700 386 10100 369 1190 17400 2390 133 0 57.3 2.43 - -
SW03 Seawater - 31.7 8.2 32400 385 10000 351 1170 17800 2480 134 0 59.2 <1.00 - -
SW04 Seawater - 28.5 7.8 29800 352 9330 336 1100 16000 2230 132 0 53.1 3.58 - -
4 Results and Analyse 4.1 Hydrochemical Characteristics

The temperature of the hot water exposed in the study area is 37.6–88.9°C, and that of the cold groundwater in the area is 23.4–26.8°C. The pH of the geothermal water and surface water is 6.50–8.68 and 7.4–9.41, respectively, indicating slightly alkaline water. The pH of the groundwater is 4.55–7.92, suggesting neutral and meta-acidic water.

The salinity of the geothermal water tends to increase from the surrounding mountainous areas to the coastal areas in Xiamen. It is 300–443 mg/L for geothermal water exposed in mountainous and piedmont alluvial-diluvial plains (i.e., samples H03, H04, H07, H11, and H12), 1100–3640 mg/L for those exposed to groundwater runoff areas of alluvial-diluvial plains and eroded platforms (i.e., samples H01, H02, and H05), and 8000–21000 mg/L for those exposed in sea-land intersections (i.e., samples H06, H08, H09, H10, and H13).

According to the Piper trilinear diagram of water samples (Figure 2), the cations and anions in the surface water mainly include Ca2+, Na+, and HCO3-. For the cold groundwater, the cations and anions are dominated by Na+, Ca2+, HCO3-, and Cl− and the hydrochemical types mainly include Ca•Na-HCO3 and Ca•Na-HCO3•Cl. For the geothermal water in the hilly mountainous areas and the piedmont alluvial-diluvial plains, the cations and anions mainly include Na+, Ca2+, HCO3-, and SO4 2, and the hydrochemical types are dominated by Ca•Na-HCO3•SO4. For the geothermal water in the coastal areas, the cations and anions are dominated by Na+ and Cl−, respectively, with the water type of Na-Cl, and the hydrochemical types feature abrupt changes.

Piper trilinear diagram of water samples from Xiamen.

Cl− is not liable to form mineral salts nor is absorbed on mineral surfaces in natural water-rock systems. Moreover, it is hardly affected by water-rock interactions even in a high-temperature environment. Therefore, Cl− is frequently used to trace the origins of materials in geothermal water and its systems that are closely correlated with Cl− (Cartwright et al., 2004; Arnórsson and Andrésdóttir, 1995). In the study area, there is a negative correlation between SiO2 and Cl− in cold groundwater and the geothermal water H03, H04, H07, H11, and H12 in the hilly mountainous areas and piedmont alluvial-diluvial plains, while there is no close correlation between SiO2 and Cl− in the nearshore geothermal water (Figure 3). These phenomena indicate that the SiO2 and Cl− concentrations in the cold groundwater and the geothermal water in the hilly mountainous areas and piedmont plains are controlled by water-rock interactions, while the SiO2 and Cl− concentrations in nearshore geothermal water are possibly mainly affected by seawater infiltration (Wang et al., 1986).

Distribution of SiO2 and Cl− concentrations in groundwater in Xiamen.

 4.2 Mixing Ratio of Seawater in Geothermal Water

The Piper trilinear diagram and the isotopic characteristics of groundwater all indicate that the nearshore geothermal water in Xiamen is affected by seawater. Figure 4 illustrates the Cl− and Br− concentrations in the geothermal water. The Br− concentration of the groundwater in the study area is relatively low and is mostly below the detection limit, while that in the nearshore geothermal water is relatively high. The linear relationship between Cl− and Br− concentrations reveals that the salinity of the geothermal water originates from seawater and is controlled by the quantity of mixed seawater. The mixing ratio of seawater in the geothermal water was calculated based on the Cl− concentration in geothermal water (Table 2). Specifically, the Cl− concentration in seawater was taken as 17100 mg/L, which was the average Cl− concentration of seawater samples collected from the local sea in Xiamen City. Meanwhile, the Cl− concentration in geothermal water before seawater mixing was taken as 17.90 mg/L, which was the average Cl− concentration in groundwater in the bedrock mountainous areas. The calculation results show that the geothermal water H3, H4, H7, H11, and H12 exposed in the piedmont areas is not affected by seawater mixing, while the nearshore geothermal water is affected by seawater mixing at different levels. The geothermal water H13 in the Pubian geothermal field shows the highest mixing ratio of seawater, which is up to 73.20%.

Distribution of Cl− and Br− concentrations in groundwater in Xiamen.

Mixing ratio of seawater in geothermal water in Xiamen.

No. Landform type Cl−(mg/L) Mixing ratio of seawater %
H03 Bedrock 14.67 0.00
H11 16.77 0.00
H12 11.18 0.00
H01 Alluvial residual plain 1209 6.97
H02 459.3 2.58
H04 56.58 0.23
H07 52.39 0.20
H05 1947 11.29
H06 Alluvial marine floodplain 4628 26.99
H08 11090 64.82
H09 10374 60.63
H10 7545 44.06
H13 12522 73.20
4.3 Environmental Isotopic Characteristics of Groundwater

In the study area, the δ18O and δ2H values of hot water are −7.7 to −3.8‰ and −51 to −26‰, respectively, and those of cold water are −7.3 to −4.7‰ and −47 to −32‰, respectively.

The local meteoric water line (LMWL) of Xiamen approximates the global meteoric water line (GMWL; Yurtsever, 1975), with the slope and y-intercept of the former being greater than those of the latter (Chen et al., 2016). The delta values of hydrogen and oxygen isotopes in the surface water, groundwater, and geothermal water in the study area are distributed on both sides of the local atmospheric precipitation line, indicating that the water in the area is mainly recharged by atmospheric precipitation. The seawater in the Xiamen Bay is greatly affected by the Jiulong River with a total annual runoff of 8.22 billion m3 and the surface water and groundwater surrounding Xiamen. Large amounts of surface water and groundwater mix with seawater in the Xiamen Bay, causing the seawater to be rich in negative water isotopes. As shown by the testing data, the seawater in the Xiamen Bay has δ18O values of −2.35 to −1.29 and thus is rich in negative water isotopes compared to open ocean water (Table 3). The hydrogen and oxygen isotopes of geothermal fields show obvious zonation. Geothermal waters H01, H03, H11, and H12, which are distributed in low mountains, hills, and river valleys, have relatively negative water isotopes and low temperatures due to the recharge of water from high altitude areas. The elevation of the mountain is about 1175 m in the study area. In addition, groundwater could be recharged during the glacial period, contributing to the depleted water isotopes. The 14C ages of waters H06 and H13 are greater than 18 ka. The temperature of geothermal water tends to be higher and the isotopes of geothermal water tend to approximate those of seawater near the coast (Cai, 2003; Figure 5). When the seawater has a maximum δ18O value of −1.29, the δ18O values at the freshwater endmember of geothermal water were calculated to be −10.66 to −6.4 (average: −7.7) based on the mixing ratio of seawater. For example, Pubian (H13) is rich in negative water isotopes, with a δ18O value of −10.66. When the seawater has a minimum δ18O of −2.35, the calculated δ18O values at the freshwater endmember of geothermal water were −7.7 to −6.4. The δ18O values at freshwater endmember of geothermal water approximate to those of the precipitation in the study area, indicating that the freshwater endmember of geothermal water was recharged by atmospheric precipitation. In addition, the groundwater in the geothermal water Pubian (H13) has a 14C age of 19.7 ka, indicating that the freshwater endmember of groundwater in the hot spring could be recharged during the glacial period.

δ2H and δ18O of coastal seawater in Xiamen.

Sample Sampling timing δ2H VSMOW (‰) δ18OVSMOW (‰)
1998–11-06 1998–12-06 1998–11-06 1998–12-06
Seawater H −15.9 ± 0.6 −10.2 ± 0.3 −1.94 ± 0.02 −1.29 ± 0.03
L −17.8 ± 0.4 −12 0.6 ± 0.1 −2.35 ± 0.05 −1.53 ± 0.02

“H” denotes high tide and “L” denotes low tide.

Distribution of stable hydrogen and oxygen isotopes in geothermal water in Xiamen.

According to the relationships between Cl− concentration and δ18O values (Figure 6), Cl− is poorly correlated with δ18O for cold groundwater and the geothermal water in mountainous areas in Xiamen. In contrast, there is a significantly positive correlation between Cl− and δ18O for the geothermal water in coastal areas, indicating a marine origin of Cl− in geothermal water. The geothermal water circulation in offshore areas could be affected by the paleo-seawater trapped in the marine sediments or modern seawater. The regional geological tectonism in Xiamen is dominated by crustal uplift, with merely a small number of thin marine sedimentary strata. In this case, paleo-seawater cannot be stored. Therefore, it can be inferred that the geothermal water in coastal areas in Xiamen is mainly recharged by modern seawater.

Relationship between the distribution of Cl− concentration and δ18O.

 5 Discussion 5.1 Water-Rock Equilibrium State

The Na-K-Mg ternary diagram can be used to distinguish different types of water samples based on the equilibrium state of geothermal water (Figure 7). The ternary diagram shows three zones, namely the zones of fully equilibrated water, partially equilibrated water, and immature water. It is applied on the basis that K and Na concentrations can reach equilibrium faster than Mg and K concentrations (Giggenbach, 1988). The geothermal water in the study area is partially equilibrated water, except for H04 and H12, which are immature water. The water-rock interactions in the study area have not yet reached the fully equilibrated state, and dissolution still continues. The geothermal water may originate from a hotter environment and is mixed and diluted by shallow cold water during its deep circulation and rise. As a result, the contents of chemical components in hot water change. The high salinity and Cl− concentration of geothermal water originate from seawater mixing, which brings abundant ions such as Na+ and K+ besides Cl−. Meanwhile, the Na-K-Mg ternary diagram shows that all cold groundwater samples lie near the Mg endmember at the lower right corner. This phenomenon indicates that the temperature of water-rock equilibrium is low and Na and K minerals in hot water do not reach equilibrium. The Na/K ratios of the partially equilibrated waters indicate a possible equilibration temperature range of 140–180°C. This result suggests that the high-temperature geothermal water that undergoes deep circulation is mixed with shallow cold water, thus forming partially equilibrated or immature water.

Na-K-Mg ternary diagram of geothermal water samples in Xiamen.

 5.2 Estimation of Geothermal Reservoir Temperature

Geochemical geothermometers can be used to calculate the temperature of underground geothermal reservoirs based on the concentrations of chemical components in geothermal water. In the geothermal system, the migration of hot water from deep to shallow parts tends to be accompanied by the dissolution and precipitation reactions of various minerals. If a certain mineral concentration shows a relationship with the fluid temperature when it reaches the reaction equilibrium in the solution, the mineral concentration can be used to deduce the temperature of mineral equilibrium (i.e., the ambient temperature) (Craig, 1953; Li et al., 2022). Geothermal geothermometers generally include SiO2, gas, isotopic, and cation geothermometers. The cation geothermometers are related to components such as Na, K, and Mg. This study revealed that a large amount of seawater is mixed into the geothermal water in Xiamen. As a result, the concentrations of key cations in the geothermal water have the same orders of magnitude as those in the cold groundwater, making it difficult to conduct correction using the mixing ratio. In other words, the seawater mixing makes the essential application conditions of cation geothermometers unavailable (Fournier, 1977; Fournier and Potter, 1982). SiO2 geothermometers are devised based on the concentrations of SiO2 minerals in geothermal water since the solubility of SiO2 minerals is the function of temperature. Moreover, pressure and the increase in salts (leading to the change in salinity) have small effects on the solubility of quartz and non-crystalline silica when the geothermal reservoir temperature is less than 300°C (Verma and Santoyo, 1997).

Most geothermal water in the study area is partially equilibrated water, and only Dongtang (H04) and Tangli (H12) are immature water. Moreover, geothermal water H01, H02, H05, H06, H07, H08, H09, H10, and H13 is mixed with seawater at different levels. Seawater can enter the geothermal water in the deep or shallow parts. When seawater mixing occurs in deep parts, water-rock interactions reach the equilibrated state after seawater mixing and thus cation geothermometers are applicable. However, in the case of seawater mixing in shallow parts, water-rock interactions have not reached the equilibrated state after seawater mixing and thus cation geothermometers are inapplicable. It is difficult to determine whether seawater enters the geothermal water in the deep or shallow parts using currently available data. Moreover, partially equilibrated water (H03, H11) highly approaches immature water, possibly leading to large errors in the temperature calculated using cation geothermometers.

SiO2 geothermometers are devised based on the solubility of the SiO2 minerals including quartz, chalcedony, and amorphous non-crystalline silica (Fournier and Rowe, 1966; Fournier and Truesdell, 1973). At a temperature range of 0–250°C, the results calculated using the formulas of quartz geothermometers are very close to the solubility of quartz under the vapor pressure of solutions (Fournier et al., 1980). Therefore, the calculation results of geothermometers are accurate at this temperature range. However, the geothermal reservoir temperature in the study area is generally less than 250°C as revealed by relevant research results. In general, quartz and chalcedony determine the SiO2 concentration at temperatures of > 180°C and < 110°C, respectively, but the minerals that control the SiO2 concentration at a temperature of 110–180°C are still unknown (Arnorsson, 1975). This study selected quartz and chalcedony geothermometers. Quartz geothermometers can be divided into no-steam loss geothermometers and maximum steam loss geothermometers. Since the temperature at geothermal wellheads is significantly lower than the local boiling point, the no-steam loss quartz thermometer and chalcedony geothermometer was used in this study (Fournier, 1977). As revealed by the geothermal temperatures calculated using SiO2 geothermometers, the quartz geothermometer and the chalcedony geothermometer yielded geothermal reservoir temperatures of 101–145°C, and 71–119°C (Table 4).

Estimated temperatures of geothermal reservoirs in Xiamen.

No. Temperature of water Quartz thermometer (°C, no-steam loss) Chalcedony thermometer (°C)
H01 56.8 114 85
H02 51.7 122 94
H03 48.0 121 92
H04 37.6 101 71
H05 80.0 127 100
H06 47.0 128 100
H07 45.5 107 78
H08 38.2 115 86
H09 53.6 125 97
H10 88.9 141 114
H11 47.5 115 86
H12 48.5 145 119
H13 68.3 137 110
5.3 Mixing Model

Given that the geothermal water in the study area is mixed with cold water and seawater in shallow parts, this study used the silica-enthalpy mixing model to determine the mixing ratio of hot water with shallow cold water and to obtain the original temperature of the geothermal reservoirs (Fournier and Truesdell, 1973). In this study, the average temperature of cold water samples was used as the cold water endmember (t = 21°C, SiO2 = 20.64 mg/L). In the silica-enthalpy mixing model, assuming no steam or heat loss, the hot water endmember and the cold water endmember were projected into the silica-enthalpy diagram (Figure 8). Then, the temperature range of deep geothermal reservoirs was determined by the temperatures corresponding to three points of intersection of the line passing the hot water points and the cold water point and the solubility curves of quartz and chalcedony (Alcicek et al., 2018), and the mixing ratio range of cold water is the proportions of the distance between the hot water point and the intersection points along the line. Using the silica-enthalpy illustration method, it can be estimated that deep geothermal reservoirs in Xiamen have enthalpy values of 775–975 kJ/kg and temperatures of 185–225°C and that the mixing ratio of cold water is 63‒91%.

Silica-enthalpy illustration method.

 5.4 Formation Mechanisms of Geothermal Resources

The low-medium temperature geothermal systems in the study area are affected by deep mantle-derived materials to a limited extent, and their He isotopic ratios show typical crustal metamorphic characteristics (Tian et al., 2021). The heat in the study area mainly originates from the heat transfer of EW-trending deep faults and the radioactive heat production of granites. The shallow groundwater or seawater surrounding geothermal anomalous areas infiltrates downward along the fractures of NW-trending structures while continuously absorbing heat (heating, expanding, and specific gravity decreasing). When it infiltrates to heat sources, where the geothermal water is about 185–225°C, the pressure difference formed by the temperature difference between the heat sources and their surrounding areas pushes the geothermal water to rise along tensional fractures and then release thermal energy. Meanwhile, the surrounding low-temperature groundwater continuously infiltrates and recharges the geothermal water. As a result, the shallow geothermal reservoirs in the study area have a temperature of 71–149°C. The temperature difference between the heat sources and their surrounding areas continues pushing the geothermal water to constantly rise, leading to the formation of the convective geothermal systems in igneous rock areas in southeast coastal areas of China (Figure 9).

Diagram showing the genetic model of geothermal resources in igneous rock areas in the southeast coastal areas of China.

 6 Conclusion

The geothermal water exposed in Xiamen has a temperature of 37.60–88.90°C. It is slightly alkaline water, and its hydrochemical types mainly include Ca•Na-HCO3 and Ca•Na-HCO3•Cl. From piedmont areas to the coastal areas, the salinity of the geothermal water constantly increases. Moreover, the geothermal water in the coastal areas has a hydrochemical type of Na-Cl, showing an abrupt change compared with the cold groundwater.

The geothermal water in coastal areas in Xiamen is recharged by seawater mixing to different extents according to the hydrochemical types, isotopic characteristics, and the C1-/Br- ratio of geothermal water. As revealed by the calculation results using the Cl− mixing model, 10 of 13 geothermal fields in Xiamen are recharged by seawater mixing. The geothermal water in the Pubian geothermal field (H13) shows the highest mixing ratio of seawater, which is up to 73.20%. Furthermore, the freshwater recharge endmember of the deep geothermal water in Xiamen could be recharged during the glacial period.

The geothermal resources in Xiamen mainly have low-medium temperatures. The geothermal fields in piedmont areas are recharged by rainfall infiltration, while those in the coastal areas are recharged by rainfall and seawater mixing. The quartz and chalcedony geothermometers yielded geothermal reservoir temperatures of 101–145°C and 71–119°C, respectively.

The NE-trending faults in Xiamen have significant impacts in deep parts and constitute channels that allow deep heat to rise. The NW- and near-EW-trending faults are mainly tensional and constitute the recharge, runoff, and discharge circulation channels of geothermal water. Atmospheric precipitation infiltrates downward along the NW- and near-EW-trending faults to the NE-trending faults, and groundwater temperature reaches 185–225°C subject to deep heat transfer. The temperature difference results in the pressure difference, which causes the geothermal water to rise along tensional fractures and the surrounding cold water to continuously infiltrate and recharge the geothermal water. As a result, the mixing ratio of cold water is up to 63‒91%, and the shallow geothermal reservoirs in Xiamen have temperatures of 71–145°C.

 Data Availability Statement

The original contributions presented in the study are included in the article/Supplementary files, further inquiries can be directed to the corresponding author.

 Author Contributions

All authors listed have made a substantial, direct, and intellectual contribution to the work and approved it for publication. CL: Conceptualization, Writing-original draft, Visualization, Funding acquisition. YL: Methodology, Resources, Project administration. SC: Investigation, Data curation. JL: Formal analysis, Writing-review and editing, Supervision.

 Funding

This work was supported by China Geological Survey project (DD20190303).

 Conflict of Interest

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

 Publisher’s Note

All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.

 References Alçiçek H. Bülbül A. Brogi A. Liotta D. Ruggieri G. Capezzuoli E. (2018). Origin, Evolution and Geothermometry of the Thermal Waters in the Gölemezli Geothermal Field, Denizli Basin (SW Anatolia, Turkey). J. Volcanol. Geotherm. Res. 349, 1–30. 10.1016/j.jvolgeores.2017.07.021 Armienta M. A. Rodriguez R. Ceniceros N. Cruz O. Aguayo A. Morales P. (2014). Groundwater Quality and Geothermal Energy. The Case of Cerro Prieto Geothermal Field, Mexico. Renewable Energy 63, 236–254. Arnórsson S. Andrésdóttir A. (1995). Processes Controlling the Distribution of Boron and Chlorine in Natural Waters in Iceland. Geochimica Cosmochimica Acta 59 (20), 4125–4146. 10.1016/0016-7037(95)00278-8 Arnorsson S. (1975). Application of the Silica Geothermometer in Low Temperature Hydrothermal Areas in Iceland. Am. J. Sci. 275 (7), 763–784. 10.2475/ajs.275.7.763 Cai M. (2003). The Study of Hydrogen and Oxygen Isotopes of Coastal Groundwater in Xiamen Island. Mar. Sci. 27 (9), 1–6. 10.3969/j.issn.1000-3096.2003.09.001 Cartwright I. Weaver T. R. Fulton S. Nichol C. Reid M. Cheng X. (2004). Hydrogeochemical and Isotopic Constraints on the Origins of Dryland Salinity, Murray Basin, Victoria, Australia. Appl. Geochem. 19 (8), 1233–1254. Chen Y. Du W. Chen J. Xu L. (2016). Composition of Hydrogen and Oxygen Isotopic of Precipitation and Source Apportionment of Water Vapor in Xiamen Area. Acta Sci. Circumstantiae 36 (2), 667–674. 10.13671/j.hjkxxb.2015.046410.5846/stxb201408251674 Craig H. (1953). The Geochemistry of the Stable Carbon Isotopes. Geochimica Cosmochimica Acta 3 (2-3), 53–92. 10.1016/0016-7037(53)90001-5 Dezi W. Qijiang R. Jiansheng Q. Kerong C. Zhaowen X. Jiahu Z. (1996). Characteristics of Volcanic Rocks in the Shoshonite Province, Eastern China, and Their Metallogenesis. Acta Geol. Sin. Ed. 9 (3), 246–259. 10.1111/j.1755-6724.1996.mp9003003.x Fan W. Menzies M. A. Yi H. X. Chen X. Zhou H. (1993). Nature and Processes of the Lower Lithosphere of the Southeast China Coast. Geotect. Metallogenia 17 (1), 27–34. Fournier R. O. (1977). Chemical Geothermometers and Mixing Models for Geothermal Systems. Geothermics 5 (1-4), 41–50. 10.1016/0375-6505(77)90007-4 Fournier R. O. Potter R. W. II (1982). A Revised and Expanded Silica (Quartz) Geothermometer. Geotherm. Resour. Counc. Bull. 11 (10), 3–12. Fournier R. O. Rowe J. J. (1966). Estimation of Underground Temperatures from the Silica Content of Water from Hot Springs and Wet-Steam Wells. Am. J. Sci. 264 (9), 685–697. 10.2475/ajs.264.9.685 Fournier R. O. Thompson J. M. Austin C. F. (1980). Interpretation of Chemical Analyses of Waters Collected from Two Geothermal Wells at Coso, California. J. Geophys. Res. 85 (B5), 2405–2410. 10.1029/JB085iB05p02405 Fournier R. O. Truesdell A. H. (1973). An Empirical NaKCa Geothermometer for Natural Waters. Geochimica Cosmochimica Acta 37 (5), 1255–1275. 10.1016/0016-7037(73)90060-4 Gan H. Lin W. Yan X. Yue G. Zhang W. Wang G. (2020). Analysis of Geothermal Occurrence Characteristics and Origin of the Thermal Anomalies in the Hidden Igneous Rock Area in the Central Guangdong. Acta Geol. Sin. 94 (7), 2096–2106. 10.19762/j.cnki.dizhixuebao.2020215 Gan H. Lin W. Yue G. Wang X. Ma F. Wang G. (2017). Research on the Fault Controlling Mechanism of Geothermal Water in Zhangzhou Basin. J. Groundwater Sci. Eng. 5 (4), 326–335. Gao F. Yang X. Wu A. Fu Y. Chen Y. (2009). Characteristics of Thermal Springs and Genesis of Thermal Underground Waters in Hainan Island. J. Jilin Univ. 39 (2), 281–287. 10.3969/j.issn.1671-5888.2009.02.016 Giggenbach W. F. (1988). Geothermal Solute Equilibria. Derivation of Na-K-Mg-Ca Geoindicators. Geochimica Cosmochimica Acta 52 (12), 2749–2765. 10.1016/0016-7037(88)90143-3 Han Q. Zhuang Q. (1988). On the Source and Pathway of Hot Water in Zhangzhou Basin, Fujian. Sci. J. Earth Sci. 13 (3), 271–277. Hu S. Xiong L. (1990). Reservoir Modelling of Zhangzhou Low Temperature Fracture Zone System, Fujian, China. Geol. Sci. Technol. Inf. 9 (4), 65–71. Li J. Zhang L. Ruan C. Tian G. Sagoe G. Wang X. (2022). Estimates of Reservoir Temperatures for Non-magmatic Convective Geothermal Systems: Insights from the Ranwu and Rekeng Geothermal Fields, Western Sichuan Province, China. J. Hydrology 609 (3), 127668. 10.1016/j.jhydrol.2022.127668 Li T. lin W. Gan H. Yue G. Zhang D. Wang G. (2020). Research on the Genetic Model and Exploration Progress of Hot Dry Rock Resources on the Southeast Coast of China. J. Geomechanics 26 (2), 187–200. 10.12090/j.issn.1006-6616.2020.26.02.018 Liao Z. (2012). Deep-Circulation Hydrothermal Systems without Magmatic Heat Source in Fujian Province. Geoscience 26 (1), 85–98. 10.3969/j.issn.1000-8527.2012.01.009 Lin S. (2007). Characteristics, Exploitation and Utilization of Geothermal Resources in the Xinglinwan Area of Xiamen City. Geol. Fujian 27 (2), 249–253. 10.3969/j.issn.1001-3970.2008.02.021 Lin W. Chen X. Gan H. Yue G. (2020). Geothermal, Geological Characteristics and Exploration Direction of Hot Dry Rocks in the Xiamen Bay-Zhangzhou Basin, Southeastern China. Acta Geol. Sin. 94 (7), 2066–2077. 10.19762/j.cnki.dizhixuebao.2020223 Lin W. Gan H. Wang G. Ma F. (2016). Occurrence Prospect of HDR and Target Site Selection Study in Southeastern of China. Acta Geol. Sin. 90 (8), 2043–2058. 10.3969/j.issn.0001-5717.2016.08.031 Lin W. J. Wang G. L. Gan H. N. Wang A. D. Yue G. F. Long X. T. (2022). Heat Generation and Accumulation for Hot Dry Rock Resources in the Igneous Rock Distribution Areas of Southeastern China. Lithosphere 2021 (5), 2039112. 10.2113/2022/2039112 Ma Z. Ma Y. Zhang P. Si F. Huo Q. Chu L. (2021). Application of Wide Area Electromagnetic Method in Geothermal Exploration of Hongtang Town, Fujian Province. Mineral. Explor. 12 (3), 661–667. 10.3969/j.issn.1674-7801.2021.03.019 Ozgener O. Kocer G. (2004). Geothermal Energy Utilization in Jordanian Deserts. Energy Sources 26 (4), 353–360. 10.1080/00908310490424105 Pang Z. (1987). Zhangzhou Basin Geothermal System--Genesis Model, Energy Pottential and the Occurrence of Thermal Water. Beijing: Institute of Geology and Geophysics, 270. Qiu Z. (2018). Study on Geothermal Resources and its Causes in Xiamen. Beijing: China University of Geosciences. Tian J. Li Y. Zhou X. Pang Z. Li L. Xing L. Z. (2021). Geochemical Characteristics of Hydrothermal Volatiles from Southeast China and Their Implications on the Tectonic Structure Controlling Heat Convection. Front. Earth Sci. 9, 1–13. 10.3389/feart.2021.786051 Verma S. P. Santoyo E. (1997). New Improved Equations for Na/K, Na/Li and SiO2 Geothermometers by Outlier Detection and Rejection. J. Volcanol. Geotherm. Res. 79 (1-2), 9–23. 10.1016/S0377-0273(97)00024-3 Wang D. Zhang R. Shi Y. (1986). General Hydrogeology. Beijing: Geological Publishing House. Wang J. (1985). Distributions and Formation of the Geothermal Field along the Coast, Southeastern China. Seismol. Geol. 7 (1), 49–58. Wang P. Chen Y. Cao B. Pan J. Wang C. (1993). Crust-upper Mantle Structure and Deep Structure Setting of Fujian Province. Geol. Fujian 12 (2), 79–158. Wang X. (2018). Formation Conditions and Hydrogeochemical Characteristicsof the Geothermal Water in Typical Coastal Geothermal Field with Deep Faults. Wuhan: Guangdong Province , China University of Geosciences. Xiong L. Wang J. Pang Z. (1990). Convective and Conductive Heat Flows in Zhangzhou Geothermal Field, Fujian Province, China. Chin. J. Geophys. 33 (6), 702–711. 10.1016/0009-2541(90)90098-R Xiong S. Jin D. Sun K. Zou Z. Fan S. Y. Du B. X. (1991). Some Characteristics of Deep Structure of the Zhangzhou Geothermal Field and It's Neighbourhood in the Fujian Province. Chin. J. Geophys. 34 (1), 55–63. 10.1007/BF02919155 Yurtsever Y. (1975). Worldwide Survey of Stable Isotopes in Precipitation. International Report. Vienna: IAEA. Zhang J. Wang B. Tang X. Dong M. Ai Y. (2018). Temperature Structure and Dynamic Background of Crust and Mantle beneath the High Heat Flow Area of the South China Continental Margin. Chin. J. Geophys. 61 (10), 3917–3932. 10.6038/cjg2018L0448 Zhang Y. Luo J. Feng J. (2020). Characteristics of Geothermal Reservoirs and Utilization of Geothermal Resources in the Southeastern Coastal Areas of China. J. Groundwater Sci. Eng. 8 (2), 134-142. 10.19637/j.cnki.2305-7068.2020.02.005