Characteristics and Genesis of an Exceptionally Large Sinter Group in the Duolong Metallogenic Belt, Northern Xizang
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摘要: 藏北多龙矿集区新发现25×104 m2超大规模泉华群，开展新发现泉华群热泉水水化学特征和钙华成因机制研究，可为多龙矿集区地热资源可持续开发和地质遗迹保护提供参考依据。文章在野外地质调查基础上，对泉华群及周边热泉、河水、泉水等水体进行水化学分析，并对钙华开展δ13C和δ18O同位素取样测试。结果显示：垂向分为上、下两级阶地，热泉水温19.2~37.9 ℃，属低温热水类型。泉华群热泉TDS值为
1625 ~1870 mg/L，水化学类型为HCO3·SO4-Na·Ca型，水中富含 Li、B、As，具深部热水属性，且与流域内其他水体水化学特征差异显著。Na-K-Mg三角图解表明热泉水水–岩相互作用尚未达到平衡状态，石英与玉髓呈饱和或近饱和状态，经3种SiO2地温计计算，热储温度为91.85~121.58 ℃。δ13C和δ18O同位素表明阶地Ⅰ（下级年代较新）的钙华受浅表冷水影响更强。整体上沿容日阿藏布发育的NE和NW向断裂成为连接姐尼拉索-拉嘎拉断裂的沟通导热断裂，为地热流体上涌并与大气淡水混入提供通道。在CO2脱气与蒸发浓缩作用下，经多期泉华沉积、封堵与突破，最终形成现今大规模连片泉华群地貌。Abstract:A giant hot spring sinter covering an area of 25×104 m2 was newly discovered in the Duolong ore concentration area, northern Xizang Research on the hydrochemical characteristics of thermal springs and the genetic mechanism of travertine in this newly identified sinter can provide a reference for the sustainable development of geothermal resources and the protection of geological relics in the Duolong area, and also supply data support for studies on hydrothermal systems and tectonic evolution at different stages on the Qinghai-Xizang Plateau. Based on field geological surveys, this study performed hydrochemical analysis on water bodies including thermal springs, rivers, and springs within and around the sinter group, with a total of 10 hydrochemical sampling sites. δ13C and δ18O isotopic analyses were carried out on travertine samples, collecting 16 sets of isotopic data. The results showed as follows. (1) The newly discovered sinter group in the Duolong ore concentration area covers 25×104 m2 and is vertically divided into upper and lower terraces. The water temperature ranges from 19.2 to 37.9 ℃, belonging to low-temperature thermal water. Various spring vents developed on Terrace Ⅰ and Terrace Ⅱ directly record the morphological features of springs at different evolutionary stages, representing three types corresponding to the early (continuous upwelling), middle (declining), and late (blocked and extinct) stages of hot spring activity. (2) Thermal springs of the sinter group have moderate cation and anion contents, with total dissolved solids (TDS) ranging from 1625 to 1870 mg/L. The hydrochemical type is HCO3·SO4-Na·Ca, with relatively high concentrations of Li, B, and As, indicating a deep high-temperature thermal water origin. The hydrochemical characteristics are distinctly different from those of other thermal springs, rivers, springs, and lakes in the Rongriazangbo Basin. (3) The Na-K-Mg triangular diagram shows that all thermal waters, including those from the sinter group, fall in the unbalanced domain, indicating that water-rock interactions have not reached equilibrium. Quartz and chalcedony in the thermal waters are saturated or near-saturated, suggesting that they are the dominant silica phases in the geothermal reservoir. The reservoir temperatures estimated by the quartz geothermometer with steam loss, quartz geothermometer without steam loss, and revised SiO2 geothermometer are 99.06−119.50 ℃, 97.76−121.58 ℃, and 91.85−117.71 ℃, respectively. (4) For travertine from TerraceⅡ, δ13C ranges from 5.69‰ to 8.83‰ with a mean of 7.54‰, and δ18O ranges from -13.58‰ to -8.50‰ with a mean of -11.76‰. For travertine from TerraceⅠ, δ13C ranges from 4.80‰ to 7.01‰ with a mean of 6.10‰, and δ18O ranges from -17.34‰ to -14.00‰ with a mean of -15.15‰. This indicates that travertine in TerraceⅠ was more strongly affected by shallow cold water during its formation. (5) NE- and NW-trending faults along the Rongriazangbo act as conductive geothermal faults connecting the Jienilasuo-Lagala deep fault, providing pathways for the upwelling of thermal water and the mixing of meteoric freshwater. During geological history, deep thermal water continuously ascended along these faults. Driven by CO2 degassing and evaporative concentration, calcium carbonate precipitated continuously and blocked spring vents, forming drumlin-like spring mounds. The accumulated pressure forced thermal water to break through weak zones and form new springs. Multi-stage superimposition and lateral connection eventually formed the large-scale sinter group observed today.-
Key words:
- Northern Xizang Plateau /
- sinter group /
- travertine /
- hydrogeology /
- silica geothermometer
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图 1 研究区区域地质背景简图（a）/大地构造位置图（b）图
K1l—早白垩世郎山组；K1q—早白垩世去申拉组；JM—侏罗纪木嘎岗日群；J3r—晚侏罗世日松组； T3R—晚三叠世日干配错群；P1x—早二叠世下拉组
Figure 1. Simplified map of the regional geological background of the study area (a) / tectonic location map (b)
图 2 泉华群野外露头特征（a-b、d-f）和正交镜照片（c）
Figure 2. Field outcrop characteristics of the sinter group (a−b, d−f) and photomicrograph under cross-polarized light (c)
图 3 容日阿藏布流域温泉发育地质简图（a）和泉华群C-O同位素、泉水全分析样点分布图（b）
Figure 3. Simplified geological map of hot spring development in the Rongri Zangbo river basin (a) and distribution map of C-O isotope and complete water analysis sampling sites of sinter group and spring water (b)
图 4 研究区各类型地下水Piper图
Figure 4. Piper diagram of various types of groundwater in the study area
图 5 研究区热泉水Na-K-Mg三角图
Figure 5. Na-K-Mg ternary diagram of thermal spring water in the study area
图 6 研究区热泉水中主要矿物的饱和指数图
Figure 6. Saturation index diagram of major minerals in thermal spring water in the study area
图 7 泉华群阶地Ⅰ、阶地Ⅱ钙华的δ18O和δ13C关系图
Figure 7. δ18O vs. δ13C plot for the tufa samples of terrace I and II, sinter group
图 8 姐尼拉索-拉嘎拉断裂带水文地质剖面(a)、露头(b)及AMT图(c)
Figure 8. Hydrogeological section (a), outcrop (b) and AMT profile (c) of the Jienilasuo-Lagala fault zone
表 1 容日阿藏布流域及周边代表性温泉水、地表水水化学取样统计表
Table 1. Hydrochemical sampling statistics of representative hot spring water and surface water in the Rongri Zangbo river basin and its surrounding areas
样点 类型 位置 构造位置 出露地
层岩性测试项目(mg/L) pH 温度
℃水化学类型 Na+ K+ Ca2+ Mg2+ Cl− ${\rm{SO}}_4^{2-}$ ${\rm{HCO}}_3^{-}$ SiO2 Li B As TDS A01 温泉 泉华群处温泉 断裂带附近，
NNE断裂K1d 多尼组
石英砂岩244.6 28.1 266.0 50.1 108.7 711.7 626.1 45.8 2.0 7.7 1.6 1768 7.34 37.89 HCO3·SO4-Na·Ca A02 温泉 泉华群处温泉 229.5 22.0 232.5 47.9 119.4 780.9 540.0 67.5 2.0 10.1 1.9 1712 8.30 24.56 HCO3·SO4-Na·Ca A03 温泉 泉华群处温泉 243.3 27.1 369.5 49.3 118.0 793.6 503.4 74.78 2.0 9.0 1.78 1870 8.34 19.22 HCO3·SO4-Na·Ca A04 温泉 泉华群处温泉 239.5 23.1 251.9 50.5 115.6 741.6 387.5 68.3 2.0 10.1 1.7 1625 8.21 27.60 HCO3·SO4-Na·Ca A05 温泉 泉华群南2 km温泉 断裂带附近，
NNE断裂K1d 多尼组
石英砂岩136.9 17.5 279.3 55.9 70.5 676.1 512.0 25.4 1.4 4.7 1.0 1501 7.67 28.17 HCO3·SO4-Na·Ca A06 温泉 泉华群北5 km泉 断裂带内 P1x 下拉组灰岩 46.8 6.3 87.0 33.8 19.5 110.9 370.4 10.8 0.4 1.56 0.8 496 7.97 18.45 HCO3·SO4-Na·Mg A07 温泉 容日阿藏布上游 断裂带附近，
NEE断裂K2ηγ 黑云二
长花岗岩832.0 73.5 63.4 8.2 612.1 203.6 1241.2 90.1 20.0 202.3 26.1 2509 7.46 55.01 Cl·HCO3-Na A08 泉水 文不当桑大泉 断裂带内 P1x 下拉组灰岩 41.3 3.0 69.0 50.3 17.1 56.1 327.1 11.7 0.1 0.05 0.1 358 8.56 13.50 HCO3-Na·Ca A09 河水 容日阿藏布 / 第四系 64.9 7.5 71.6 17.2 38.0 113.9 271.5 13.8 0.8 2.23 0.7 472 8.05 10.22 SO4·HCO3-Na·Ca A10 湖水 别若则错 / 第四系 5291.9 424.0 13.3 715.4 4620.0 6513.0 845.1 7.2 29.9 22.9 9.9 18653 9.02 10.55 Cl·SO4- Mg·Na 
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表 2 研究区热泉水估算热储温度表
Table 2. Estimated reservoir temperatures of thermal springs in the study area
热泉编号 泉口实测温度/ ℃ 估算热储温度/ ℃ 玉髓法a 玉髓法b 有蒸汽损失石英 无蒸汽损失石英 修正SiO2 A01 37.89 67.54 69.09 99.06 97.76 91.85 A02 24.56 87.60 87.81 115.05 116.35 112.01 A03 19.22 93.30 93.10 119.50 121.58 117.71 A04 27.60 88.25 88.41 115.55 116.95 112.66 A05 28.17 40.99 44.10 77.12 72.67 64.96 A06 18.45 9.08 13.70 49.54 41.77 32.32 A07 55.01 104.14 103.13 127.87 131.45 128.52
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