Formation Mechanism of Cold Springs and Hot Springs in Karst Groundwater Systems in North China: A study of Baotu Spring
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摘要: 岩溶地下水和地热水分别是中国北方重要的供水水源和供暖热源，但二者水力联系尚缺乏系统研究；为实现保泉、供水和地热清洁能源开发的三赢，通过含水层/热储层空间分布、同位素测年、水文地球化学场、水动力场、温度场特征及规律分析等方法，揭示了趵突泉泉域岩溶地下水流系统从浅、中循环子系统至深循环子系统，即岩溶地下水至冷泉和热泉的演变过程、驱动机制与响应机理. 在地下水位高程差引起的重力势能差驱动下，岩溶地下水沿济南含水层系统从上游浅循环-开放式地下水动力系统，向中游中循环-半开放式地下水动力系统径流，径流途中在济南市区遇不透水的辉长岩体或石炭纪二叠纪砂岩页岩地层阻截，大部分地下水沿垂向强裂隙岩溶发育通道上涌、穿透第四纪砾岩或辉长岩体裂隙发育带喷出地表形成17~18 ℃的承压上升冷泉. 一小部分地下水从深部穿过或从侧面绕过辉长岩体，沿裂隙岩溶通道继续向下游深循环运移，形成弱开放地热水动力系统；高大地热流传导聚热、深大断裂带/侵入岩体-灰岩接触带带状对流聚热、凸起区高热导率分流聚热、盖层低热导率保温聚热、地下水深循环运移传导-对流聚热等五元聚热驱动14~18 ℃的常温地下水演变为33~95℃的承压热泉（自流地热水）.Abstract: To discriminate the correlation between normal temperature groundwater and geothermal water, by analyzing the characteristics and patterns of spatial distribution of aquifer/thermal reservoir, isotopic dating, hydrogeochemical field, hydrodynamic field and temperature field, the evolution process and driving mechanism of karst groundwater flow system in Baotu spring catchment from shallow to middle and to deep circulation subsystems, i.e., from cold springs to hot springs, are revealed. Driven by the gravitational potential energy difference, the groundwater flows from the open groundwater flow system in the upper reaches to the semi-open groundwater flow system in the middle reaches along the Jinan karst aquifer system.A small part of groundwater passes through from the deep or bypasses the Jinan gabbro mass, and migrates to the downstream along the fissure karst channel, forming a weakly open geothermal water flow system. Such five sources of heat accumulation drive normal temperature groundwater of 14-18℃ to be heated into geothermal water of 33-95 ℃ as the high terrestrial heat flux accumulation, the belt shaped convective thermal accumulation in the deep fault zone or intrusive rock-limestone contact zone, the high thermal conductivity diffluence accumulation in the uplift area, theheat preservation accumulation by low thermal conductivity cap rock, and the conductive-convective thermal accumulation by deep groundwater circulation.
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Key words:
- Cold springs /
- hot springs /
- heat flow accumulation /
- evolution process /
- driving mechanism /
- Baotu spring /
- hydrogeology
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图 1 趵突泉2003—2021年地下水位动态曲线图
Fig. 1. Dynamic hydrograph of Baotu Spring from 2003 to 2021
图 2 趵突泉-五龙潭-黑虎泉-珍珠泉等四大泉群2003—2021年流量动态曲线图
Fig. 2. Flow rate dynamic curves of Baotu, Wulongtan, Heihuand Pearl Springs from 2003 to 2021
图 3 济南单斜岩溶地下水系统水文地质略图
AB线以南为浅循环-开放式和中循环-半开放式地下水动力系统，水温14~18 ℃；AB线以北为深循环-弱开放式地热水动力系统，水温33~95 ℃
Fig. 3. Hydrogeological outline of Jinan monoclinic karst groundwater system
图 4 济南单斜岩溶地下水系统自西向东即东阿→长孝→趵突泉→白泉→百脉泉断块地下水动力剖面图
2018年6月枯水期
Fig. 4. Hydrodynamic profile of Dong'e-Changxiao-Baotu Spring-White Spring-Baimai Spingfault block in Jinan monoclinic karst groundwater system
图 5 浅循环开放式地下水动力系统至深循环弱开放式地热水动力系统-岩溶地下水至趵突泉等冷泉和热泉的三级演变模式及其演变过程与驱动机制
T. 地下水水温（℃）；A. 地下水年龄（a）；D. 地下水循环深度（m）；H. 地下水补给高程（m）
Fig. 5. Evolution process and mechanism from shallow circulation-open groundwater dynamic system to deep circulation-weakly open geothermal water dynamic system
图 6 济南北岩溶热储地热田地热水起源与演化
据康凤新等（2020）修改
Fig. 6. Origin and evolution of karst geothermal reservoir in North Jinan geothermal field
图 8 趵突泉出流机制——岩体阻滞（a）与地垒聚集（b）复合型富水构造
a. 自南向北岩体阻滞地下水动力剖面；b. 自西南向东北沿石灰岩与辉长岩体/砂岩页岩阻水地层接触带形成的地下水主径流带地下水动力剖面；1. 第四纪粉质黏土；2. 第四纪砾岩；3. 白云质石灰岩；4. 石灰岩；5. 大理岩；6. 白垩纪燕山期辉长岩；7. 泉群；8. 岩溶地下水流向；9. 岩溶发育带；10. 岩溶地下水承压水头
Fig. 8. Baotu Spring outflow mechanism: intrusive rock mass obstructed and horst accumulated groundwater rich structure
图 9 趵突泉1959—2021年水位-泉水流量-开采量-降水量动态图
Hmax、Hmin为历年最高、最低水位
Fig. 9. Hydrodynamics of water level-flowrate-exploitation-precipitation of Baotu Spring from 1959 to 2021
图 10 济南北地热田东段地热水14C校正年龄与距补给区距离关系图
据康凤新等（2020）修改；取样井位见图 6；蓝色取样点表示岩溶地下水，红色表示岩溶地热水
Fig. 10. The relationship between corrected 14C ages of geothermal water and distance from the recharge area, east part of North Jinan geothermal field
图 11 趵突泉（水温17 ℃）与齐热1地热井（井口水温57 ℃）水位动态对比图
Fig. 11. Dynamic hydrograph comparisonbetween Baotu Spring (water temperature 17 ℃) and Qire1 geothermal well (wellhead water temperature 57 ℃)
图 12 济北岩溶热储地热田地热井涌水量与距断裂/灰岩-岩体接触带距离关系曲线
Fig. 12. Relation curve between geothermal well yield and distance from faults/limestone-rock mass contact zones in North Jinan Karst geothermal reservoir
图 13 华北克拉通破坏动力学过程与东部减薄的地壳(33 km)和岩石圈(60~100 km)
据Kusky et al.（2014）；Zhu et al.（2015）；徐小兵（2018）修改
Fig. 13. The destruction of North China Craton and eastern thinned crust (33 km) and lithosphere (60~100 km)
图 14 济南北岩溶热储盖层地温梯度等值线图（a）和剖面图（b）（据康凤新等，2020修改）
Fig. 14. Geotemperature contour and profile of cap rock gradient (modified from Kang et al., 2020)
表 1 趵突泉断块岩溶地下水流系统分级及其特征一览表
Table 1. Classification and characteristics of Baotu Spring karst groundwater flow system
特征 地下水流系统分级 浅循环-开放式岩溶地下水动力系统 中循环-半开放式岩溶地下水动力系统 深循环-弱开放式岩溶地热水动力系统 流域位置 上游 中游 下游 岩溶类型 裸露型 半覆盖-覆盖型 埋藏型 补给源 大气降水入渗补给 大气降水入渗补给，上游地下水侧向径流补给 中上游地下水深循环径流补给 地表高程(m) 1 545~400 400~30 30~19 含水层/热储层顶板标高(m) 600~200 200~20 20~-2 429 地下水水力性质 潜水 半承压-承压水 承压水 地下水/地热水循环深度(m) 100~300 300~800 800~3 500 地下水/地热水补给高程(m) 100~500 200~600 411~1 494 地下水/地热水径流速度 40~190 m/d 100~300 m/d 0.25 m/a 地下水/地热水TDS(mg/L) 300~500 500~700 400~7 300 井口水温(℃) 14~15 15~18 33~95 地下水/地热水年龄(a) 7~15 15~30 12 070~39 640 地下水/地热水天然排泄形式 季节性上层滞下降泉，溢流入河，以外源水形式向中游径流 承压上升泉为主要排泄方式，小部分向下游深循环运移径流 滞留状态 地下水/地热水循环交替强度 强烈 强烈 微弱 水岩作用 弱 中等 强 
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表 2 奥陶纪石灰岩热储顶部与盖层底部接触带地温梯度
Table 2. Geothermal gradient at the interface between the roof of the Ordovician limestone geothermal reservoir and the bottom of the cap rock
孔号 奥陶纪石灰岩热储顶板深度（m） 热储顶部与盖层底部接触带测温段及其地温梯度 石炭-二叠纪砂岩页岩盖层平均地温梯度（℃） 深度范围（m） 长度（m） 温度（℃） 温差（℃） 地温梯度（℃/100 m） YK1* 672.00 610~674 64 36.6~45.5 8.9 13.90 3.724 YK2* 537.20 478~541 63 35.8~39.7 3.9 6.19 3.197 YK3* 528.38 490~525 35 32.2~38.2 6.0 17.10 4.599 注：*钻孔位置见图 14
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