Genesis of high-sulfate geothermal water in the Namcha Barwa syntaxis, eastern Xizang
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摘要:
藏东南迦巴瓦构造结广泛发育高硫酸盐地热水，开发利用潜力巨大，但硫酸盐来源和形成机理缺乏研究。以南迦巴瓦构造结的温泉水和钻孔水为研究对象，通过水化学组分特征初步揭示离子来源，借助锶和硫酸盐硫、氧同位素综合分析地热水硫酸盐的来源，并利用氘氧同位素探明地热水补给来源，最终查明深部热储的水岩平衡状态和热储温度，归纳总结南迦巴瓦构造结高硫酸盐地热水形成机理。结果表明：（1）地热水属于弱酸及弱碱-碱性水，溶解性总固体含量为130～
3265 mg/L，水化学类型包括HCO3•SO4—Ca•Na、SO4—Ca及SO4•HCO3—Ca•Na型；（2）水化学和锶同位素结果表明片麻岩硅酸盐矿物和蒸发岩硫酸盐矿物溶解是影响水化学组分的关键，${}^{34}{\mathrm{S}}_{{\mathrm{SO}}_4} $-${}^{18}{\mathrm{O}}_{{\mathrm{SO}}_4} $同位素表明${\mathrm{SO}}_4^{2-} $存在大气降水、土壤硫酸盐、黄铁矿和石膏多源供给；（3）氢氧同位素揭示温泉热水补给来源为大气降水，补给高程为2646 ～3045 m；（4）二氧化硅地热温标和硅焓模型计算得到深部热储温度为232～275 °C，浅部热储温度约为180 °C，冷水混入比例为74%～82%。研究揭示该区大气降水沿断裂破碎带或基岩裂隙等导水通道向深部运移，沿途溶滤土壤硫酸盐、变质岩及局部膏盐层，在深部被加热后升流，最终于近地表混入下渗冷水后出露成泉。研究初步建立了高硫酸盐地热水的成因模式，可为南迦巴瓦构造结地热资源开发利用提供科学依据。Abstract:In the Namcha Barwa syntaxis of eastern, high-sulfate geothermal water is extensively developed, presenting significant potential for exploitation and utilization. However, the sources and formation mechanisms of these sulfates remain poorly understood. This study focused on the hot spring and borehole water in the Namcha Barwa syntaxis, aiming to identify the sources of ions in geothermal water. The study first examines the hydrochemical components, followed by comprehensive analyses of strontium, sulfate sulfur, and oxygen isotopes to determine the sources of sulfate in geothermal water In addition, this study investigated the water-rock equilibrium and temperature of deep thermal reservoirs and summarized the genesis of high-sulfate geothermal waters in the Namcha Barwa syntaxis. The geothermal water is characterized as weakly acidic to weakly alkaline-alkaline water, with total dissolved solids ranging from 130 mg/L to
3265 mg/L. The hydrochemical types include HCO3•SO4—Ca•Na, SO4—Ca, and SO4•HCO3—Ca•Na. Water chemistry and strontium isotope results indicate that the dissolution of silicate minerals in gneiss and sulfate in evaporites are key factors influencing the water chemistry components. The ${}^{34}{\mathrm{S}}_{{\mathrm{SO}}_4} $-${}^{18}{\mathrm{O}}_{{\mathrm{SO}}_4} $isotopes suggest multiple ${\mathrm{SO}}_4^{2-} $ sources, including atmospheric precipitation, soil sulfate, pyrite, and gypsum. Hydrogen and oxygen isotopes reveal that the hot spring thermal water is recharged by atmospheric precipitation, with a recharge elevation of2646 m to3045 m. Calculations using the silica geothermometer and the silica enthalpy model estimate the deep reservoir temperatures to be approximately 232 °C to 275 °C, with shallow reservoir temperatures around 180 °C and a cold water mixing ratio of 74% to 82%. The study reveals that atmospheric precipitation in this area migrates into deep reservoirs along water-conducting pathways such as fault fracture zones or bedrock fissures. It leaches soil sulfate, metamorphic rocks, and localized salt layers along the way. Once heated at deep reservoirs, it flows upward and ultimately emerges as springs after mixing with infiltrating cold water near the surface. This study establishes a genesis model for high-sulfate geothermal water, providing a scientific basis for developing and utilizing geothermal resources in the Namcha Barwa syntaxis. -
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图 3 地热水Cl−与（a）Na++K+、（b）Ca2+、（c）Mg2+、（d）
${\bf{HCO}}_{\boldsymbol{3}}^{\boldsymbol{-}} $ 、（e）${\bf{SO}}_{\boldsymbol{4}}^{{\boldsymbol{2-}}} $ 、（f）SiO2、（g）Li+、（h）B、（i）F−相关性图Figure 3.
表 1 研究区地热水化学组分
Table 1. Hydrochemical components of geothermal water in the study area
编号 样品类型 温度/°C pH 质量浓度（ρ）/（mg·L−1） TDS Ca2+ Mg2+ Na+ K+ Cl− S1 温泉水 39.3 7.89 1393.64 137.79 23.07 131.23 19.65 80.43 S2 钻孔水 68.8 8.07 818.13 91.03 2.24 114.45 9.19 24.07 S3 温泉水 60.8 8.17 1299.78 99.86 9.56 170.62 20.03 50.05 S4 温泉水 84.1 10.41 1884.89 0.64 0.01 504.03 57.63 397.59 S5 地表水 10.1 8.45 130.06 24.33 1.80 1.40 2.72 3.01 编号 样品类型 质量浓度（ρ）/（mg·L−1） 质量浓度（ρ）/（μg·L−1） ${\mathrm{SO}}_4^{2-} $ ${\mathrm{HCO}}_3^- $ ${\mathrm{CO}}_3^{2-} $ SiO2 F− Li B Sr S1 温泉水 152.63 649.01 2.50 119.47 0.85 280.13 5907.00 883.66 S2 钻孔水 336.84 190.11 2.50 106.22 1.19 42.65 863.00 1521.51 S3 温泉水 338.28 405.03 2.50 116.56 1.49 269.34 5631.00 836.90 S4 温泉水 260.51 111.01 204.80 209.33 5.81 1905.78 12167.00 224.13 S5 地表水 23.57 63.37 2.50 5.84 0.10 2.63 207.00 170.61 编号 样品类型 δ ${}^{34}{\mathrm{S}}_{{\mathrm{SO}}_4} $ /‰δ ${}^{18}{\mathrm{O}}_{{\mathrm{SO}}_4} $ /‰87Sr/86Sr δD/‰ δ18O/‰ 采样高程/m 补给高程/m 水化学类型 S1 温泉水 15.16 3.11 0.71496 −86.03 −12.29 2275 2605 HCO3—Na•Ca S2 钻孔水 9.15 7.15 0.70632 −87.10 −12.88 2452 2646 SO4•HCO3—Ca•Na S3 温泉水 8.66 0.87 0.72327 −75.04 −10.85 2068 2184 SO4•HCO3—Ca•Na S4 温泉水 19.25 4.03 0.71362 −92.77 −10.06 2032 2863 Cl—Na S5 地表水 ─ ─ 0.71054 −77.62 −12.41 2283 ─ HCO3•SO4—Ca 注：“—”代表数据缺失。 
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表 2 热储温度和冷水混合比例估算结果
Table 2. Calculation results of geothermal reservoir and cold water mixing ratio
编号 热储温度/°C 冷水混合比例/% 石英 玉髓 多矿物平衡 硅-焓方程 S1 147 122 155～175 — — S2 141 114 — 232 74 S3 146 120 — 275 82 S4 183 162 154～169 — — 注：“—”表示没有计算。
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表 3 地热水温度、焓和SiO2含量之间对应关系
Table 3. Relationship between temperature, enthalpy, and SiO2 content in geothermal water
温度/°C 焓值/（ 4.1868 J·g−1）SiO2质量浓度/ （mg·L−1） 50 50.0 13.5 75 75.0 26.6 100 100.1 48.0 125 125.4 80.0 150 151.0 125.0 175 177.0 185.0 200 203.6 265.0 225 230.9 365.0 250 259.2 486.0 275 289.0 614.0 300 321.0 692.0
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