The Simao Basin (the southern half of the Lanping-Simao Basin) is located in the Yunnan-Tibet Geothermal Belt. It is a typical red-bed basin that exhibits a strong tectonic activity (Figures 1A,B). Various types of springs of different sizes exist in the basin. Hot spring is an important part of subsurface fluid and is exposed along fault zone. Therefore, hot spring carries a lot of deep information during migration. The hydrochemical characteristics of hot springs are used to obtain information about geothermal reservoirs and thermal groundwater circulation and may provide insight into potential geothermal resources. In addition, hydrochemical components of spring water are effective indicators of earthquakes, because seismic activity can change the state of underground stress and strain, affect the hydrodynamic conditions and the degree of water-rock reaction in the hot spring, and further change the fluid composition and isotope characteristics of hot spring. Some studies on springs in the Simao Basin have focused on potassium exploration through salty and saline springs, the exploration and utilization of geothermal resources, and the origin and evolution of the springs were also examined (Zhang et al., 2013; Bo et al., 2015; Zhang et al., 2018; Zhang L. et al., 2019). However few reports have studied the earthquake-related composition of groundwater characteristics and changes in the basin. The study area is located in the Simao-Pu’er seismic zone, which is one of the most important strong earthquake disaster areas in the Yunnan province (Cheng, 2017). Examination of the hydrochemistry and changes of springs is of great helpful for understanding the breeding process of strong earthquakes in this district.

FIGURE 1. Topographic map of the study area (A) and schematic tectonics and spring sites in the Simao Basin (B); modified from Zhang Y. et al., 2020). Abbreviations: F1, Lancangjiang fault; F2, Wuliangshan fault; F3, Ailaoshan fault; F4, Mohei fault.

Earthquake-related groundwater chemical composition changes have been widely used in the search for seismic precursors. Tsunogai and Wakita, 1995 observed increased Cl and SO42- concentrations in groundwater prior to the Kobe earthquake in Japan. Claesson et al. (2004) observed a rapid increase in multicomponent constituents and a decrease in the Na/Ca content of groundwater due to a seismic event (M = 5.8) in northern Iceland. Changes in the concentrations of Ca2+ and HCO3 were observed before and after the Wenchuan earthquake (Ms = 8.0), the Lushan earthquake (Ms = 7.0), and the Kangding earthquake (Ms = 6.3) in China (Chen et al., 2015; Li et al., 2019). Seismic hydrochemical changes may be linked to changes in the permeability structure, the mixture of deep and shallow fluids, and/or fluid-rock interactions caused by tectonic activity (Claesson et al., 2004; Zhang X. et al., 2019).

In this study, new hydrochemical data was obtained from the hot springs of Simao Basin. We investigated the hydrochemical characteristics of these thermal springs from 2018 to 2020. During the study period, the 2018 Mojiang M5.9 earthquake occurred in the study area and caused significant hydrochemical changes. Earthquake-related hydrochemical changes were studied and the possible mechanisms in the geothermal area were explained.

Geological Setting

The Simao Basin is located in southwest Yunnan, China and belongs to the southern section of the Sanjiang fold system, which is narrow in the north and wide in the south in the shape of a broom (Figures 1A,B; Yunnan Bureau of Geology and Mineral Resources, 1986). Several huge NW–SE and nearly S–N trending faults control the formation and tectonic evolution of the basin. The Lancangjiang deep fault (F1) in a roughly S–N direction and the Ailaoshan deep fault (F3) in a NW–SE direction are the western and eastern margins of the basin, respectively. A series of NW–SE trending faults are present in the basin, including the Wuliangshan fault (F2) and the Mohei fault (F4) (Figure 1; Qu et al., 1998). Most parts of the Simao Basin are underlain by thick Mesozoic and Cenozoic red beds, which mainly contain sandstones and mudstones. Proterozoic metamorphic rocks are only exposed in the margin of the basin. The Upper and Middle Paleozoic limestones outcrop in the central block uplifts and the marginal belt uplifts in the basin (Yunnan Bureau of Geology and Mineral Resources, 1990). According to seismic records, many moderate and strong crustal earthquakes have occurred in the basin in recent years, including the 2007 Ning’er earthquake (Ms 6.4), the 2014 Jinggu earthquake (Ms 6.6, Ms 5.8, and Ms 5.9), and the 2018 Mojiang earthquake (Ms 5.9) ( On September 8, 2018, an Ms 5.9 earthquake occurred at Mojiang, with an epicenter location of 23.28°N, 101.53°E and a focal depth of 11 km. The focal mechanism indicates that the seismogenic, strike-slip fault strikes northeast and dips to the southeast. The strike is between azimuths of 26° and 44°, the dip is between 52° and 71°, and the rake is between 2° and –17° (Zhang Y. et al., 2019). The Simao Basin is situated in the southern Yunnan-Tibet geothermal zone, which shows strong geothermal activity. The active crustal movement creates favourable conditions for the formation of high-temperature geothermal fields (Zhou et al., 2017), which have a terrestrial heat flow of 63.2 MW/m2 (Xu et al., 1992). The area hosts more than 100 springs. Several types of springs (including hot springs, saline springs and salty springs) exist in the basin (Zhang L. et al., 2019). The temperature and the flow of spring water vary in the dry season and the rainy season, but the water chemistry of springs is stable. Most of the springs emerge in carbonate rocks and water-rich red beds. The distribution of the banded geothermal wells is controlled by the tectonic activities that formed deeper fracture zones, which can provide channels for the enrichment and migration of geothermal fluids.

Materials and Methods

Hot springs were geochemically investigated in the Simao Basin from 2018 to 2020, and 38 hydrothermal water samples were obtained (sampling locations shown in Figure 1B and Supplementary Table S1). A lot of hydrochemical data was collected from previous studies that investigated these thermal spring samples in the 1980s and 2017 (Tong and Zhang, 1994; Zhang X. et al., 2019). The field investigations include on-site measurements of pH, temperature, electrical conductivity (EC), which were measured with a portable multi-parameter water quality analyzer (produced by WTW, Germany). The precision of these factors were 0.01, 0.1°C, and 1 μS cm−1, respectively. Each water sample was filtered on-site with 0.2 μm membranes and was stored in two 250 ml polyethylene bottles. The concentration of major cations (Na+, K+, Ca2+ and Mg2+) and anions (F, Cl, NO2, Br, NO3and SO42−) were determined by performing ion chromatography (883 Basic IC plus, Metrohm, Switzerland; detection limit: 0.01 mgL−1) at the Deep-earth fluids Laboratory, Yunnan Earthquake Administration, China. Low concentrations of Li+, Rb+, Cs+, Sr2+ were determined with a Thermo Fisher X series II ICP-MS at the Institute of Crustal Dynamics, China Earthquake Administration, Beijing, China. SiO2 (aq), HCO3, and CO32− were detected according to the China National Standard Examination Methods for Drinking Natural Mineral Water (GB/T 8538-2008). SiO2 (aq) was measured by a visible spectrophotometer, and HCO3 and CO32− was measured by the volumetric method (HCl titration).

Results and Discussion


The physicochemical parameters and the geochemical data of hot springs in the Simao Basin have been listed in Supplementary Table S1 and Supplementary Table S2. The 21 hot springs had temperatures ranging from 30°C to 102°C. The pH values and total dissolved solids (TDS) were 5.60–8.26 and 237–10,444 mg/L, respectively. The saline spring samples (No. 3, 4, and 5) had relatively higher TDS values (5,351–10,444 mg/L) than others. The data of ions (K+, Na+, Ca2+, Mg2+, Cl, SO42− and HCO3) was provided from previous studies that investigated the thermal springs from the 1980s to 2020. As shown in Figure 2, Piper and Schoeller’s diagrams illustrate the concentrations of major and minor ions in springs. In the Piper diagram, the 21 water samples have been roughly divided into three groups. Saline spring waters are of Na–Cl type. Samples containing HCO3 as the predominant anion (HCO3 > SO42− > Cl or HCO3 > Cl > SO42−) include Na-HCO3, Ca-HCO3, Ca-Na-HCO3, Na-Ca-HCO3, Na-HCO3-SO4, Na-HCO3-Cl, Na-Ca-HCO3-SO4, and Na-HCO3-Cl-SO4. Samples containing SO42− as the predominant anion (SO42− > HCO3 > Cl or SO42− > Cl > HCO3) include Ca-SO4, Na-Ca-SO4, Ca-Na-SO4, Na-SO4-HCO3, and Na-Ca-SO4-HCO3. Other ions (Li+, NH4+, Rb+, Cs+, Sr2+, F, NO2, Br, NO3) were present in relatively low concentrations. In data points 14–21, the components F and Sr2+ had relatively higher concentrations. This is because F and Sr2+ were more easily enriched into weak alkaline water, with a pH range of 7.0–8.5 (Cai et al., 2001; Xing et al., 2012).

FIGURE 2. Piper diagram (A) and Schoeller diagram (B) of the geothermal waters. Process (black circles) indicating the changes before and after the Mojiang earthquake.

To understand the origin and the evolution of major ions in thermal groundwater, the relationships between major ions of the spring water were analyzed, i.e. HCO3 vs. Na+, Na+ vs. Cl, SO42− vs. Ca2+, HCO32− vs. Ca2+, (Ca2+ + Mg2+) vs. (HCO3 + SO42-) and SO42- vs. Cl, (Figure 3). Except for the data points 3, 4, 5, 8, 9, and 12, most of the data points were plotted close to the 1:1 line in Figure 3A. This indicated that the quality of Na was affected by the dissolution of Na-feldspar. Samples 8 and 9 are present on the lower-right side of the 1:1 line, which implies that HCO3 has another source. Figure 3D illustrated that carbonate minerals (calcite and dolomite) were also a source of HCO3. The Triassic carbonate strata in the Simao Basin are located under the Jurassic red bed. The spring water flows through carbonate formations and can dissolve calcite and dolomite. Saline spring waters of data points 3, 4, 5, and 12 have a higher concentration of Na+ ions and a lower concentration of HCO3 ions, with an average molar Na+/HCO3 ratio of 15. This indicates that the dissolution of Na-feldspar is not the main source of these ions (Figure 3A). Spring samples of data points 3, 4 and 5 are located in Jinggu County, which is a region with large halite deposits (Yunnan Bureau of Geology and Mineral Resources, 1986). As shown in Figure 3B, saline spring samples of data points 3, 4, 5, and 12 contained a high concentration of Cl and Na+ ions, which were present on the dissolution line of NaCl. This indicates that halite is the main source of Na. Except for data points 6, 7, 8, and 9 in the Triassic carbonate rocks, most water falls near the 1:1 line (gypsum dissolution line), suggesting that the dissolution of gypsum and anhydrite is the main source of Ca2+ and SO42− (Figure 3C). In Lanping- Simao Basin, anhydrite is distributed in the thin interlayer of the salt series, and gypsum is distributed in the mud conglomerate layer on the surface (Qu et al., 1998). The ionic ratios of (Ca2+ + Mg2+) vs. (HCO3 + SO42-) in Figure 3E show that the dissolution of dolomite, calcite, gypsum, and anhydrite is responsible for the production of Ca2+, Mg2+, SO42-, and HCO3. A correlation between Cl and SO42− can be inferred from Figure 3F. The positive chloride-sulfate relation probably reflects the mixing of geothermal water and cold water (Arnórsson, 1985). Atmospheric oxygen in the cold water oxidizes H2S to SO42- at shallow depths (Daniele et al., 2020), which increases the SO42- concentration of the geothermal water, (e.g., sampling points 10, 11, 18, 19, 20, and 21). In addition, the lithology suggests that the dissolution of the pyrite-bearing formation rocks near the Ailaoshan fault may increase the SO42- content in the groundwater (Luo, 2007). Therefore, the chemical characteristics of geothermal water in the Simao Basin show that the main ions in the hot spring water mainly come from the dissolution of minerals during the circulation of surface water. The water chemistry types are controlled by stratum lithology.

FIGURE 3. Relationship plots of major ions of the spring water in the Simao Basin. (A) HCO3 vs. Na+; (B) Na+ vs. Cl; (C) SO42− vs. Ca2+; (D) HCO32− vs. Ca2+; (E) Ca2+ + Mg2+ vs. HCO3 + SO42−; (F) SO42− vs. Cl.

Earthquake-Induced Chemical Variations

As shown in the Piper diagram (Figure 2), the water chemistry in No.7 and 13 changed during the study period. Anomalies of the water chemistry types in No. 1 and 2 should not be considered, because the epicentral distance of these two anomalous sites is far above the theoretical distance influenced by the quake with magnitude (M) 5. No.7 is located in the near-field of the Mojiang earthquake. The water chemistry in No.7 changed from Na-HCO3-Cl to Na-Ca-HCO3 in June 2018 before the Mojiang M5.9 earthquake on September 8 and from Na-Ca-HCO3 back to Na-HCO3-Cl in 2020. Similarly, the water chemistry in No.13 changed from Na-Ca-Cl-SO4-HCO3 to Na-Ca-HCO3-Cl-SO4 before the Mojiang M5.9 earthquake and from Na-Ca-HCO3-Cl-SO4 back to Na-Ca-Cl-SO4-HCO3 after the earthquake; however, no significant changes were observed in other spring samples (Supplementary Table S1). For these spring samples, the time series of anion and cation ions for these springs were plotted (Figure 4). Based on previous case studies documenting hydrogeochemical response to seismicity, the groundwater chemistry fluctuates due to rainfall and other superficial phenomena. During the entire sampling period, most of the cations and anions varied with the two sigma relative standard deviation (2σ). Before the earthquake, ionic concentration increased slightly (only 10–20% above the background value) and was considered insignificant (Toutain et al., 1997; Li et al., 2021). In the springs, Ca2+ and HCO3 ions exhibited significant changes before the Mojiang M5.9 earthquake; however, other ions stayed relatively stable in the springs. In most springs (blue lines), the concentration of Ca2+ and HCO3 ions increased obviously (about 28–77% above the background value) before the Mojiang M5.9 earthquake; however, it decreased after the earthquake (Figure 4). The data points 6, 8, 9, 18, 19, 20, and 21 (black lines) changed slightly before and after the earthquake. The Na/Ca ratio appeared to be sensitive to changing stresses, which were associated with M > 4 earthquakes (Claesson et al., 2004). In Figure 4, the Na/Ca data decreased before the Mojiang M5.9 earthquake. After the earthquake, the Na/Ca ratio increased slightly and then recovered in 2020.

FIGURE 4. Hydrogeochemical changes of thermal springs from the 1980s to 2020.

Reservoir Temperature and Variations

Reservoir temperature is an important parameter, which is used for classifying the genetic types of geothermal systems. Moreover, it is also used for evaluating the geothermal potential of geothermal fields, which can be estimated with geochemical geothermometers. The concentration of solutes in geothermal fluids is a function of the geothermal reservoir temperature. In theory, all chemical reactions controlled by temperature can be used as geochemical geothermometers (Ellis, 1970; Wang et al., 1993).

Traditionally, the cation ratio geothermometers such as Na-K, Na-K-Ca, and K-Mg geothermometers and SiO2 geothermometers were used to estimate the geothermal reservoir temperature (Fournier, 1981; Giggenbach, 1988; Verma and Santoyo, 1997). As shown in Table 1, the reservoir temperatures were calculated by using Eqs 14.


TABLE 1. The estimated reservoir temperatures of hot springs in the Simao Basin.

As shown in Table 1, the reservoir temperatures calculated by quartz geothermometers were in the range of 32–177°C, and those calculated by cation geothermometers were as follows: 63–260°C (Na-K), 12–91°C (Na-K) and 16-200 (Na-K-Ca), respectively. The Na-K-Mg triangular diagram classified spring waters into three types: fully-equilibrated waters, partially-equilibrated waters and immature waters. These water types were used to determine whether a fluid reached water-rock equilibrium (Giggenbach, 1988). Only fully-equilibrated waters could be used with cation geothermometers. In Figure 5, most data points were in the area of immature water, which was present in the hot springs plot. Sample No. 2, 3, 4, 5, and 12 were located in the partially-equilibrated area of the triangular diagram. This indicates that the wall rock have not reached equilibrium due to the addition of a significant quantity of cold water (shallow groundwater). This implies that cation geothermometers are not suitable for calculating the reservoir temperatures of the study area.

FIGURE 5. The Na-K-Mg trilinear equilibrium diagram of hydrothermal water of the Simao Basin.

The reservoir temperature in the Simao Basin was calculated by Zhang Y. et al., 2019. Their study indicates that compared to cation geothermometers, quartz geothermometer provides more reasonable estimations of the reservoir temperature of this area (Zhang L. et al., 2019). As mentioned previously, the studied hot spring waters are mixtures of thermal groundwater and shallow cold waters, which cause a high dilution of silica concentration. Therefore, the temperatures calculated with SiO2 geothermometers (Table 1) were lower than the most reliable reservoir temperatures. The silica-enthalpy mixing model equation and the silica-enthalpy diagram can be used to estimate the proportion of thermal groundwater and cold waters. Moreover, they can be used to measure the original temperature of the thermal groundwater component, which can be further considered as the reservoir temperature (Fournier, 1977). The proportion of cold water during mixing was calculated by the following silica-enthalpy Eqs 5, 6 (Fournier et al., 1974).


where Hc is the enthalpy of the near-surface cold water, Hh is the initial enthalpy of deep hot water, and Hs is the enthalpy of mixed hot water. Moreover, Sic is the silica content of near-surface cold water, Sih is the initial silica content of deep hot water, and Sis is the silica content of mixed hot water. X1 and X2 are the calculated cold water mixing ratios of enthalpy and the SiO2 concentration, respectively. The solution of Eqs 5, 6 was calculated by using a diagrammatic method (Figure 6, taking the example of samples 10a-d) because the values of X1, X2, and Hs are unknown. The relationship between X and temperature was plotted to obtain two curves, whose intersection indicated the estimated proportion of cold water and the original temperature of the thermal groundwater component. The silica-enthalpy diagram is another way to estimate the temperature of the deep thermal groundwater, by using a plot of silica concentration vs. the enthalpy of water (Fournier, 1977). A line passed through the characteristic points of cold (point A) and geothermal (point B) waters; the intersection of the line is point C. The quartz solubility curve illustrates the enthalpy of the deep thermal groundwater (Figure 7, taking the example of samples 10a-d).

FIGURE 6. A diagram of temperature relative to the proportion of cold water in hot spring sample 10 (X is the proportion of the cold water).

FIGURE 7. The silica-enthalpy diagram of hot spring sample 10.

Except for the data points 4c, 5c, 7c, 10c, and 12c at abnormal lower temperatures, the reservoir temperatures of the mixing model of the silica-enthalpy equation and diagram were in the range of 121°C and 289°C (Table 2). As shown in Table 2, these values were significantly higher than those of reservoir temperatures, which were determined by the SiO2 geothermometer. The proportions for cold water ranged from 69 to 98%. An intersection point was not obtained at the plots of samples 1c-d, 6c, 8c, 9a-d, 11c, 14a-d, 16a-d, 18a-d, and 19a-d. This indicates that heat was lost before mixing the hot and cold waters. The existence of the low-velocity zones (LVZs) has been revealed by seismic imaging beneath the Simao Basin within the middle-lower crust at a depth of 15–30 km, and is considered to be possible ductile crustal flow (Bai et al., 2010; Bao et al., 2015; Li et al., 2016). The ductile crustal flow may be a dominant heat source of hot springs in the Simao Basin. The hot springs had higher reservoir temperatures (>250°C) and were mainly located at the margin of the Simao basin, that is, sample sites 2, 13, 15, 17, 20, and 21. At this location, the Lancangjiang and Ailaoshan deep faults were well-developed. A fracture is the main channel for hot water circulation, and the deep faults help provide deep heat for the spring waters (Tang et al., 2017). In the study area, the fissures were well-developed in carbonate rocks. However, the metamorphic strata were exposed in the margin of the basin, which seemed to have low permeability. As a result, springs that emerged in the Ailaoshan metamorphic rocks had higher reservoir temperatures.

TABLE 2. Reservoir temperatures based on the silica-enthalpy mixing model and cold water mixing proportions of the hot springs in the Simao Basin.

The sampling points 4c, 5c, 7c, 10c, and 12c, which were located at about 50–150 km away from the epicentre of the M5.9 Mojiang earthquake. After the earthquake, these reservoir temperatures showed a massive decline (Figure 8). In particular, the reservoir temperatures of the sample 10c decreased by about 100°C after the M5.9 Mojiang earthquake; however, the reservoir temperature of the sample 10c recovered in the year 2020 (200–223°C). The variations in reservoir temperature were similar to those observed after the M 8.0 Wenchuan earthquake (Li et al., 2019). The reservoir temperature was approximately 340°C before the Wenchuan earthquake, and it decreased to a relatively stable level after the earthquake (220–260°C).

FIGURE 8. Reservoir temperature variations in some springs from the 1980s to 2020.

The Assumptions of Earthquake-Related Hydrogeochemical Variation

Two assumptions have often been used to explain earthquake-related hydrogeochemical changes (Claesson et al., 2007): 1) hydrogeochemical shifts record accelerated water-rock interactions resulting from an increased reactive surface area caused by fracture of the sampled aquifer; or 2) hydrogeochemical shifts record the mixing of (or switching between) chemically distinct aquifers. This could occur in response to the fracture of a hydrological barrier between aquifers or because of a change in the relative pressures of connected aquifers.

Whenever an earthquake occurs, the pore pressure of rocks is enhanced. Since a seismic wave propagates through the rocks, it causes an extensive fracture of the wall rock (Du et al., 2013). This increases the rock’s surface area, which is in contact with groundwater. Thus, the water-rock interactions become more intensive. In hydrogeochemistry, the saturation index (SI) is commonly used to indicate the chemical states of the mineral phases of groundwater. The saturation state of hot springs in the Simao Basin was calculated based on the chemical compositions and physicochemical parameters of the hydrothermal waters via the PHREEQC program package (Parkhurst and Appelo, 1999). All the samples were undersaturated with gypsum, anhydrite, celestite and halite (SI < 0), showing no obvious changes before and after the Mojiang earthquake. However, the SI values of carbonate minerals (calcite and aragonite) exhibited significant changes before and after the earthquake. Figure 9 illustrates the saturation trends of calcite and aragonite. The SI values of calcite and aragonite in almost all undersaturated sampling points reached saturation before the Mojiang M5.9 earthquake, indicating the enhanced dissolution of carbonate rocks. Thus, the increases in the concentrations of Ca2+ and HCO3 ions were observed during the Mojiang earthquake. The water chemistry of No.7 and No.13 sites changed from Na-HCO3-Cl to Na-Ca-HCO3, and from Na-Ca-Cl-SO4-HCO3 to Na-Ca-HCO3-Cl-SO4, respectively. This also indicates that the dissolution of Ca2+ and HCO3 ions were in progress. After the earthquake, the SI ratios continued to increase and reached oversaturated levels. This implies that precipitation occurred in the hot springs of the Simao Basin, and the concentration of dissolved ions decreased. The SI values decreased and recovered in 2020. This progressive re-equilibration was possible due to water-rock interactions, which explains why the concentration of Ca2+ and HCO3 ions decreased to their pre-seismic levels. Moreover, the water chemistry of No.7 and No.13 sites also recovered. Although the vigorous water-interaction model is used to explain the changes in the chemical components (i.e., major and trace elements) following an earthquake, the model fails to explain the variables that indicate water mixing or interactions with deep fluids (e.g., water isotopes, dissolved gases and reservoir temperature; Binda et al., 2020).

FIGURE 9. Variations in the SIs of calcite and aragonite in the hot springs from the 1980s to 2020.

The rupture of hydrological barriers or permeability changes are probable causes of variations in ionic concentrations and reservoir temperature. Seismic waves may enhance the permeability of the affected aquifers through increasing fracture porosity, changing pore pressure, and fracturing aquitards. These seismic effects could result in the mixing of fluids from different aquifers or the upwelling of deep fluids (Binda et al., 2020). Before the occurrence of the Mojiang earthquake (from April to July 2018), the compressive activity was significantly greater around the Jingdong-Simao region (Yang et al., 2019). A compressional setting favored an increase in pore pressure induced in Moderate shocks (De Gregorio et al., 2012). Under the N–S-trending tectonic compression stresses, the local stress concentration may cause a new fracture and induce moderate to strong earthquakes like the Mojiang M5.9 earthquake (Chang et al., 2019). New fractures were created during the Mojiang earthquake, which caused the permeability to increase greatly. The obvious increases in the concentrations of Ca2+ and HCO3 may be attributed to a secondary fluid, which is rich in Ca2+ and HCO3 ions and originates from the underlying carbonate strata. In addition, the variation in ionic concentrations may be correlated to the contribution of deep fluids. Under the Simao-Pu’er seismic zone, strong low-velocity zones are visible, suggesting the existence of an upwelling asthenosphere in the uppermost mantle (Li et al., 2016; Zhang Z. et al., 2020). Deep degassing results indicate that high He isotopes signatures (3He/4He = 5.75–8.36 Ra; mantle-derived He >70%) are present in this region (Zhao et al., 2018). An increased 3He/4He ratios were observed in the hot springs before the occurrence of M > 4 earthquakes in the Simao-Pu’er seismic zone. This implies that much deeper fluid was added to these springs. Moreover, a similar phenomenon that caused changes in the reservoir temperature was the M 8.0 Wenchuan earthquake (Li et al., 2019). Variations in reservoir temperature after the Mojiang earthquake may have been caused by the entrance of cold shallow groundwater into the reservoir, which participated in deep circulation; however, the clogging of fractures prevented the entry of shallow cold groundwater, and the reservoir temperature increased. Thus, we infer that the chemical changes that occurred after the Mojiang earthquake were caused by the mixing of fluids and water-rock interaction.


From 2018 to 2020, the hydrochemical characteristics of 21 thermal springs of the Simao Basin were determined. These water samples were roughly divided into three groups: saline spring waters, HCO3-rich spring waters, and SO42−-rich spring waters. In the study area, the water chemistry types were controlled by stratum lithology. Ca2+ (Mg2+) and HCO3 in the hot spring waters were mainly derived from the dissolution of carbonate minerals, gypsum, and anhydrite in Triassic rocks. The saline springs flowed in the red beds and dissolved a large amount of halite with high Cl and Na+ contents. The Ailaoshan metamorphic rocks contain pyrite, which may increase the SO42- content in the hot spring waters. The reservoir temperatures (121–289°C) of the Simao Basin were determined. It is speculated that the ductile crustal flow could be the dominant heat source of the hot springs of Simao Basin. The hot springs had higher reservoir temperatures (>250°C) and were mainly located at the edges of the basin. Metamorphic rocks exposed in the region had low permeabilities and these springs was close to nearby deep faults that provided deep heat.

During the study period, the 2018 Mojiang M5.9 earthquake occurred in the study area and caused significant hydrochemical changes. The concentrations of Ca2+ and HCO3 ions increased obviously in most springs, just before the occurrence of the Mojiang M5.9 earthquake; however, the concentrations of these ions decreased after the earthquake. The hydrogeochemical variation might be attributed to the vigorous water-rock interactions and the mixing of a second fluid. The reservoir temperature decreased after the earthquake. This may have been caused by the entry of cold shallow groundwater.

Data Availability Statement

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

Author Contributions

QL: Conceptualization, Investigation, Writing—original draft, Visualization. CZ: Methodology, Data curation. YW: Investigation, Discussion. YZ and HR: Investigation.


This study was supported by the project of Science for Earthquake Resilience of China (XH20053Y) and the Special Fund of the Institute of Earthquake Forecasting, China Earthquake Administration (2017IES010205).

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.


We sincerely thank the reviewers and the editor for providing useful comments and suggestions, which greatly improved the quality of this manuscript.

Supplementary Material

The Supplementary Material for this article can be found online at:



This article is autogenerated using RSS feeds and has not been created or edited by OA JF.

Click here for Source link (