Sources of Heat and Control Factors in Geothermal Field
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摘要: 地热能越来越受到重视，但地热田的形成机制和热量的来源仍存在争议，多数学者认为岩浆囊可以为地热田直接供热.以二维热传导正演模拟为手段得出，盖层是形成地热田的必要条件；在浅部存在高热传导层时，地温剖面会出现镜像倒影形态，温度在垂向上分为高梯度段、低梯度段和低温段，侵位较浅（< 10 km）的岩浆囊散热和进入热平衡时间小于20~50万a.结合大量地热田温度资料分析认为，地热田的热量不是因为存在异常热源（如岩浆囊），而是来源于正常的基底热流.当深部热量传递到地表时，由于近地表物质的热传导能力的差异引起温度场发生变化，即地热田之下存在高热传导层快速地将基底热量传递到浅层而形成异常高温.Abstract: Geothermal energy is attracting increasing attention. However, the formation mechanism and the source of heat in geothermal fields are still in dispute. Most scholars believe that the magma pocket can provide direct heating for geothermal fields. In this paper, by means of 2D forward modeling of heat conduction, it is found that the caprock is a necessary condition for forming geothermal fields. When there is a high heat conduction layer in the shallow part, the geothermal profile will display a mirror reflection shape, and the temperature will be divided into high gradient section, low gradient section and low temperature section. The heat dissipation and thermal equilibrium time of the shallow magma pocket (< 10 km) are less than 200 000-500 000 years. Based on the analysis of the temperature data of a large number of geothermal fields, it is concluded that the heat in geothermal fields is from normal basal heat flow instead of the presence of abnormal heat sources, such as magma pocke. When the deep heat is transferred to surface, the temperature field changes due to the difference in the heat conduction ability of the near-surface material:the high heat conduction layer under the geothermal field will rapidly transfer the base heat to the shallow layer and form the abnormal high temperature.
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Key words:
- temperature field /
- heat conduction /
- magma chamber /
- Yangbajing /
- Tengchong /
- geothermal gradient /
- environmental geology
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图 2 中国陆区不同深度地温分布平面图
Fig. 2. Temperature distribution plan in different depths in mainland China
图 3 西藏羊八井盆地水热活动深部机制示意图
据姚足金(1986).1.等温线(℃)；2.地热流体环流线；3.岩浆流体流向；4.花岗岩γ6；5.片麻岩；6.第四系松散堆积；7.主要断层；8.主要钻孔位置；9.纵波波速(km/s)；10.磁大地电流(Ωm)；11.气体氦；12.低速层、低阻体
Fig. 3. Schematic map showing deep mechanism of hydrothermal activity in Yangbajing basin
图 4 沧县隆起容1井井温随深度变化曲线
a.容1井平面位置图；b.容1井实测井温曲线
Fig. 4. Well temperature curve with depth of Rong 1 in Cangxian uplift
图 5 法国苏尔茨地区实测地温分布
Fig. 5. Measured gradient curve of ground temperature from Soults, France
图 6 盖层厚度影响模拟剖面图
a.考虑热盖层的地质模型；b.考虑热盖层的影响后的地温场模拟结果
Fig. 6. Simulation results of the influence of caprock
图 8 古隆起理想模型及地温场分布剖面图
a.模型；b.围岩k2=2.0 W/(m·℃)；c.围岩k2=1.5 W/(m·℃)；d.围岩k2=1.0 W/(m·℃)；e.围岩k2=0.6 W/(m·℃)
Fig. 8. Calculation model of geothermal and its calculation results
图 7 羊八井地区地温场分布模拟剖面(a)及其剖面浅部A, B两点地温随时间变化曲线(b)
Fig. 7. Geothermal field simulation profile (a) of Yangbajing and temperature versus time curve of point A and B of Yangbajing profile (b)
图 9 岩体侵入停止后不同时间的温度分布剖面图
a.0 Ma；b.0.001 Ma；c.0.05 Ma；d.0.2 Ma；e.0.4 Ma；f.0.6 Ma
Fig. 9. Temperature distribution in different times after the intrusion of rock mass
图 10 青藏铁路沿线高温地热显示区分布
据胡先才(2010).1.发电为主的开发热田；2.已勘查评价热田；3.综合利用开发热田；4.有待进一步工作高温热田；5.第四纪沉积盆地；6.活动构造线；7.断裂
Fig. 10. Distribution of high temperature geothermal area along Qinghai-Tibet railway
图 11 伦坡拉盆地部分钻井测温-井深关系
Fig. 11. Relationship between temperature and depth in several wells in Lunpola basin
图 12 青藏高原构造分区和沉积盆地分布
Fig. 12. Distribution of Tectonic division and sedimentary basin in Qinghai-Tibet plateau
表 1 青藏高原地温梯度结果统计
Table 1. Results of geothermal gradient in Qinghai-Tibet plateau
序号 地区 地温梯度(℃/100 m) 1 羌塘盆地 2.73 2 羌塘盆地赤布张错多全区平均值 3 3 羌塘盆地拉雄错、董怀桑、隆鄂尼、野牛沟及安多及雀莫错等地区 1.5 4 北羌塘坳陷东部雀莫错剖面 2.7 5 措勤盆地 3.4~4.0 6 比如盆地 3.5~4.5 7 伦坡拉盆地 4.5~6.0 8 岗巴地区 6.5 9 藏南普莫雍湖 13~32 10 藏南羊卓雍湖 13~32 11 拉萨河谷 3.8 12 羊八井热田 1.9~5.9 13 拉多岗地热区 6.5~12.5 14 羊应乡热田 16~53 15 昌都盆地 5.0~6.0 16 松潘-阿坝地区 2.7 17 柴达木盆地 2.0~3.3 注：据陈红汉等(2013). 
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