川西理塘毛垭温泉群的成因及深部地热过程

doi:10.3969/j.issn.0253-4967.2023.03.006

地震地质 ›› 2023, Vol. 45 ›› Issue (3): 689-709.DOI: 10.3969/j.issn.0253-4967.2023.03.006

川西理塘毛垭温泉群的成因及深部地热过程

申华梁¹⁾(), 杨耀²^,³⁾^,^*(), 周志华⁴⁾, 芮雪莲²⁾, 廖晓峰²⁾, 赵德杨²⁾, 梁明剑²⁾, 陈梦蝶²⁾, 官致君²⁾, 任宏微⁵⁾

¹⁾ 中国地质调查局成都地质调查中心, 成都 610081
²⁾ 四川省地震局, 成都 610041
³⁾ 成都理工大学地球科学学院, 成都 610059
⁴⁾ 中国地震台网中心, 北京 100045
⁵⁾ 应急管理部国家自然灾害防治研究院, 北京 100085

收稿日期:2022-12-30 修回日期:2023-03-12 出版日期:2023-06-20 发布日期:2023-07-18
通讯作者: * 杨耀, 男, 1987年生, 工程师, 主要从事构造地球化学、流体地球化学研究, E-mail: yangyao_cdut@163.com。
作者简介:
申华梁, 男, 1986年生, 2015年于成都理工大学获得矿物学、岩石学、矿床学专业硕士学位, 工程师, 主要从事石油地质、数学地质、遥感地质及水文地质等研究, E-mail: 124283663@qq.com。
基金资助:
中国地震局地震科技星火计划项目(XH23048C); 国家自然科学基金(41877205); 四川省自然科学基金(2022NSFSC0210); 中国地质调查局地质调查项目(DD20230105)

GENESIS AND DEEP GEOTHERMAL PROCESS OF MAOYA HOT SPRINGS IN LITANG, WESTERN SICHUAN

SHEN Hua-liang¹⁾(), YANG Yao²^,³⁾^,^*(), ZHOU Zhi-hua⁴⁾, RUI Xue-lian²⁾, LIAO Xiao-feng²⁾, ZHAO De-yang²⁾, LIANG Ming-jian²⁾, CHEN Meng-die²⁾, GUAN Zhi-jun²⁾, REN Hong-wei⁵⁾

¹⁾ Chengdu Geological Survey Center, China Geological Survey, Chengdu 610081, China
²⁾ Sichuan Earthquake Agency, Chengdu 610041, China
³⁾ College of Earth Sciences, Chengdu University of Technology, Chengdu 610059, China
⁴⁾ China Earthquake Networks Center, Beijing 100045, China
⁵⁾ National Institute of Natural Hazards, Ministry of Emergency Management of China, Beijing 100085, China

Received:2022-12-30 Revised:2023-03-12 Online:2023-06-20 Published:2023-07-18

摘要/Abstract

摘要：

毛垭温泉目前的成因模式及深部地热过程的研究程度较低。文中以理塘毛垭温泉群和周边的冒火温泉为研究对象,对其进行水化学组分和氢、氧同位素分析。研究结果表明,毛垭温泉群和冒火温泉的水化类型均为Na-HCO₃型。温泉水在深循环过程中,深部水、岩、气的相互作用使得热储层中的长石发生水解,是形成Na-HCO₃型地热水的主要原因。氢、氧同位素的测量结果表明温泉水均起源于大气降水。毛垭温泉群与冒火温泉相比,具有更高浓度的离子组分,且表现出轻微的氧同位素漂移现象,表明毛垭温泉的循环深度更深,经历了更强烈的水-岩作用,此外,Cl^-的深部来源比例更高。通过SiO₂温标和硅焓混合模型估算得到毛垭温泉群的浅部热储温度为75~103℃,深部热储温度为235℃,冷水混合比例为87%~94%。基于深部热储温度计算得到毛垭温泉的最终循环深度接近5km。深部地热水受静水压力和水热对流作用,沿理塘断裂带向上运移,在此过程中,受构造裂隙的影响,地热水与冷水发生第1次混合,混合水的温度约为100℃。地热水循环至近地表时,与盆地内的冷水进行第2次混合,最终出露地表,形成中低温温泉群。

关键词: 毛垭温泉群, 地热水, 水文地球化学, 热储温度, 理塘断裂带

Abstract:

Maoya hot spring, as a famous earthquake monitoring site, is seldomly studied in terms of its genesis and deep geothermal process. In this paper, we investigated the chemical and isotopic composition of thermal water in Maoya and Maohuo in Litang to elucidate the hydrochemical characteristics and genesis of the geothermal waters.
The study results show that Maoya hot springs and Maohuo hot spring are of the Na-HCO₃ type as a result of dissolution processes involving feldspars from the reservoir rocks due to the water-CO₂-rock interaction during the deep circulation of the geothermal waters. According to the diagram of Cl^- and Na⁺ concentrations of the geothermal water samples, Cl^- in Maoya hot spring originates from the mixing of granodiorite and basalt aqueous solutions in the process of water rock interaction, while Cl^- in Maohuo hot spring mainly originates from granodiorite aqueous solutions. The stable isotope δD and δ¹⁸O composition of geothermal waters indicates that they are recharged by meteoric precipitation. The Maoya hot springs have the characteristics of higher concentration of ion components and slightly oxygen drifting compared with the Maohuo hot spring, indicating that they have a deeper circulation depth and experience a stronger water-rock interaction. In addition, the ratio of Cl^-that comes from deep source in Maoya hot springs is higher than that in Maohuo hot spring.
The high temperature geothermal water formed by deep circulation of meteoric water is mixed by the shallow cold water during the ascending process. We employed SiO₂ geothermometer and Si-enthalpy model to estimate the temperature of shallow reservoir after mixing with cold water and the temperature of deep reservoir and the mixing ratio of cold water, respectively. The results suggest that the temperature of shallow reservoir in Maoya thermal field is in the range of 75~103℃ and the temperature of deep reservoir in Maoya thermal field is about 235℃ and the mixing ratio of cold water ranges from 87% to 94%. Based on the temperature of deep reservoir, we calculated the depth of the geothermal cycle in Maoya area, which is close to 5km.
The heat source triggering the formation of this geothermal system mainly originates from mantle and partial melting body of the crust. In addition, Cenozoic granitoid magmatic residual heat and upper crust radioactive heat can also provide additional heat sources. During the process of surface cold water circulation from shallow to deep, on the one hand, it forms deep geothermal water through normal geothermal gradients, and on the other hand, the mantle fluid upwelling below the Litang Basin and partial melting in the middle crust further heat the groundwater to form a high-temperature deep reservoir. The deep geothermal water is transported to the surface along the Litang Fault under the effect of hydrostatic pressure and hydrothermal convection. During ascending process, the first mixing of groundwater with superficial cold water occurred due to the presence of structural cracks in the crust, and the temperature of the mixing water is about 100℃. When the geothermal water migrates to the near surface, it mixes with the pore water and bedrock fissure water in the basin for the second time, and the mixing proportion of cold water increases(about 90%). Finally, it emerges to the surface, forming a group of medium-low temperature hot springs.

Key words: Maoya hot springs, geothermal water, hydrogeochemistry, reservoir temperature, Litang fault zone

申华梁, 杨耀, 周志华, 芮雪莲, 廖晓峰, 赵德杨, 梁明剑, 陈梦蝶, 官致君, 任宏微. 川西理塘毛垭温泉群的成因及深部地热过程[J]. 地震地质, 2023, 45(3): 689-709.

SHEN Hua-liang, YANG Yao, ZHOU Zhi-hua, RUI Xue-lian, LIAO Xiao-feng, ZHAO De-yang, LIANG Ming-jian, CHEN Meng-die, GUAN Zhi-jun, REN Hong-wei. GENESIS AND DEEP GEOTHERMAL PROCESS OF MAOYA HOT SPRINGS IN LITANG, WESTERN SICHUAN[J]. SEISMOLOGY AND GEOLOGY, 2023, 45(3): 689-709.

图/表 13

图 1 川西理塘地区的地质构造简图(据Zhou et al., 2017修改)

Fig. 1 Geological and tectonic sketch-map of the Litang area and its surroundings(adapted after Zhou et al., 2017).

图 2 川西理塘地区的活动断层分布图

Fig. 2 The map showing the active faults in Litang area and its surroundings.

图 3 理塘毛垭地区的地质图

Fig. 3 Geological map of the Maoya area and surrounding regions.

图 4 研究区温泉和河水采样点分布图

Fig. 4 Map showing the sampling locations of hot springs and river water in the study area.

表 1 研究区水样的水化学分析结果

Table 1 Chemical composition and isotope of the water samples in the study area

样品名称	样品编号	温度 /℃	Na⁺ /mg·L^-1	K⁺ /mg·L^-1	Mg²⁺ /mg·L^-1	Ca²⁺ /mg·L^-1	F^- /mg·L^-1	Cl^- /mg·L^-1	$SO 4 2 -$ /mg·L^-1	$NO 3 -$ /mg·L^-1	$CO 3 2 -$ /mg·L^-1	$HCO 3 -$ /mg·L^-1	SiO₂ /mg·L^-1	PH	TDS /mg·L^-1	EC /μs·cm^-1	δD /‰	δ¹⁸O /‰
毛垭温泉1	LT-1	28.9	611.8	31.7	16.7	46.0	1.9	31.2	23.0	14.5	n/d	2208.8	27.1	7.8	1491	2980	-159.5	-19.0
毛垭温泉2	LT-2	37.7	628.1	25.4	6.6	57.4	5.2	34.2	26.4	6.3	n/d	2214.9	51.3	7.8	1521	3040	-160.0	-18.9
毛垭温泉3	LT-3	36.6	616.9	22.9	6.4	55.6	1.8	30.8	41.0	9.6	n/d	2147.8	49.9	7.8	1461	2920	-160.5	-19.0
毛垭温泉4	LT-4	42.8	633.9	23.8	8.8	34.1	4.0	31.9	30.3	9.8	n/d	2036.4	51.2	8.0	1536	3070	-158.7	-18.2
毛垭温泉5	LT-5	43.3	557.0	19.7	5.2	61.1	3.6	28.6	29.6	8.6	n/d	2001.4	42.5	7.7	1401	2800	-159.4	-19.4
毛垭温泉6	LT-6	40.9	591.0	21.6	5.6	57.8	3.8	30.0	28.6	8.4	n/d	2035.6	46.3	7.8	1456	2910	-161.1	-19.6
冒火温泉	LT-7	79.6	57.2	1.6	0.0	4.1	2.8	7.6	20.5	0.1	n/d	158.6	59.5	8.5	168	336	-161.9	-21.4
河水1	LT-8	19.4	41.8	2.6	8.8	25.6	0.5	2.5	10.7	1.3	n/d	256.3	13.0	8.3	227	453	-133.3	-16.7
河水2	LT-9	16.3	6.3	0.3	3.4	23.0	0.9	1.0	13.3	0.1	n/d	103.3	7.3	8.0	105	209	-124.0	-16.0

表 1 研究区水样的水化学分析结果

Table 1 Chemical composition and isotope of the water samples in the study area

样品名称	样品编号	温度 /℃	Na⁺ /mg·L^-1	K⁺ /mg·L^-1	Mg²⁺ /mg·L^-1	Ca²⁺ /mg·L^-1	F^- /mg·L^-1	Cl^- /mg·L^-1	$SO 4 2 -$ /mg·L^-1	$NO 3 -$ /mg·L^-1	$CO 3 2 -$ /mg·L^-1	$HCO 3 -$ /mg·L^-1	SiO₂ /mg·L^-1	PH	TDS /mg·L^-1	EC /μs·cm^-1	δD /‰	δ¹⁸O /‰
毛垭温泉1	LT-1	28.9	611.8	31.7	16.7	46.0	1.9	31.2	23.0	14.5	n/d	2208.8	27.1	7.8	1491	2980	-159.5	-19.0
毛垭温泉2	LT-2	37.7	628.1	25.4	6.6	57.4	5.2	34.2	26.4	6.3	n/d	2214.9	51.3	7.8	1521	3040	-160.0	-18.9
毛垭温泉3	LT-3	36.6	616.9	22.9	6.4	55.6	1.8	30.8	41.0	9.6	n/d	2147.8	49.9	7.8	1461	2920	-160.5	-19.0
毛垭温泉4	LT-4	42.8	633.9	23.8	8.8	34.1	4.0	31.9	30.3	9.8	n/d	2036.4	51.2	8.0	1536	3070	-158.7	-18.2
毛垭温泉5	LT-5	43.3	557.0	19.7	5.2	61.1	3.6	28.6	29.6	8.6	n/d	2001.4	42.5	7.7	1401	2800	-159.4	-19.4
毛垭温泉6	LT-6	40.9	591.0	21.6	5.6	57.8	3.8	30.0	28.6	8.4	n/d	2035.6	46.3	7.8	1456	2910	-161.1	-19.6
冒火温泉	LT-7	79.6	57.2	1.6	0.0	4.1	2.8	7.6	20.5	0.1	n/d	158.6	59.5	8.5	168	336	-161.9	-21.4
河水1	LT-8	19.4	41.8	2.6	8.8	25.6	0.5	2.5	10.7	1.3	n/d	256.3	13.0	8.3	227	453	-133.3	-16.7
河水2	LT-9	16.3	6.3	0.3	3.4	23.0	0.9	1.0	13.3	0.1	n/d	103.3	7.3	8.0	105	209	-124.0	-16.0

图 5 研究区水点水化类型的Piper三线图

Fig. 5 Piper diagram of the water samples.

图 6 研究区温泉水的Cl--Na+浓度图解(底图据崔月菊等, 2022)

Fig. 6 Diagram of Cl-and Na+concentrations of the thermal water samples(adapted after CUI Yue-ju et al., 2022).

图 7 研究区水样δD-δ18O关系图

Fig. 7 Plot of the relations between δD and δ18O in the water samples.

图 8 研究区水样的K-Na-Mg三角图

Fig. 8 The triangle diagram of Na-K-Mg of the water samples.

表 2 热水中温度、焓和SiO2浓度间的对应关系(Fournier et al., 1974)

Table 2 Relationship among temperature, enthalpy and SiO2 content(after Fournier et al., 1974)

温度/℃	焓/J·g^-1	$C S i O 2$ /mg·L^-1
50	50	13.5
75	75	26.6
100	100.1	48
125	125.1	80
150	151	125
175	177	185
200	203.6	265
225	230.9	365
250	259.2	486
275	289	614
300	321	692

表 2 热水中温度、焓和SiO2浓度间的对应关系(Fournier et al., 1974)

Table 2 Relationship among temperature, enthalpy and SiO2 content(after Fournier et al., 1974)

温度/℃	焓/J·g^-1	$C S i O 2$ /mg·L^-1
50	50	13.5
75	75	26.6
100	100.1	48
125	125.1	80
150	151	125
175	177	185
200	203.6	265
225	230.9	365
250	259.2	486
275	289	614
300	321	692

图 9 硅焓图解法

Fig. 9 Si-enthalpy model in the study area.

图 10 研究区地热水的热储温度与冷水混入的比例

Fig. 10 Reservoir temperatures and mixing ratio of cold water in the study area.

图 11 理塘地区地热水成因模式示意图(地层的厚度为依据平面地质图推测的厚度)

Fig. 11 The conceptual model of the Litang geothermal system (the thickness of the stratum is estimated based on the geological map).

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川西理塘毛垭温泉群的成因及深部地热过程

GENESIS AND DEEP GEOTHERMAL PROCESS OF MAOYA HOT SPRINGS IN LITANG, WESTERN SICHUAN

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