盆缘断隆型地热田成因模式

章惠; 汪新伟; 钱恪然; 毛翔; 罗璐; 刘晓红; 王玉星

doi:10.11932/karst20260109

盆缘断隆型地热田成因模式——以阳谷凸起南段为例

doi: 10.11932/karst20260109

章惠^{1, 2,},
汪新伟^{1, 2},
钱恪然³,
毛翔^{1, 2},
罗璐^{1, 2},
刘晓红^{1, 2},
王玉星^{1, 2}

1.
深层地热富集机理与高效开发全国重点实验室, 北京 100083
2.
中国石化集团新星石油有限责任公司, 北京 100083
3.
中国石化油田勘探开发事业部, 北京 100728

基金项目: 中国石油化工股份有限公司科技项目（KLJP25012，KLJP23008）

详细信息

作者简介:
章惠（1987－），女，硕士，高级工程师，主要从事非震地球物理勘探与地热地质相关工作。E-mail：zhanghui714@126.com。

中图分类号: P314
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出版历程
- 收稿日期: 2024-11-27
- 录用日期: 2025-05-06
- 修回日期: 2025-04-27
- 网络出版日期: 2026-05-27
- 刊出日期: 2026-02-25

Genetic model of basin-margin fault-uplift geothermal field: Taking the southern section of the Yanggu Uplift as an example

ZHANG Hui^{1, 2
,},
WANG Xinwei^{1, 2},
QIAN Keran³,
MAO Xiang^{1, 2},
LUO Lu^{1, 2},
LIU Xiaohong^{1, 2},
WANG Yuxing^{1, 2}

1.
State Key Laboratory of Deep Geothermal Resources, Beijing 100083, China
2.
Sinopec Star CO., LTD., Beijing 100083, China
3.
Department of Oilfield Exploration & Development, Sinopec, Beijing 100728, China

摘要

摘要: 盆缘断隆型地热田具有基岩热储埋深浅、物性好、成藏晚等特征。其形成机制的研究对丰富盆地内地热田的成因模式、指导地热田的勘探开发有着重要的理论与现实意义。文章以鲁西南隆起阳谷凸起南段为例，采用地热地质综合分析方法，对阳谷凸起南段地热田的“源、储、通、盖”主要因素进行系统研究，剖析地热田的成因模式，并精细评价地热资源量。研究结果表明：阳谷凸起南段受兰聊深断裂和基岩凸起双重影响，大地热流平均值68 mW∙m⁻²，热背景较好；该区发育奥陶系岩溶热储，呈北东向展布，热储顶面埋深1000~1800 m，具有北部和东部浅、南部和西部深的特点；主力热储层为峰峰组、上马家沟组和下马家沟组上段，热储平均厚度98m，平均孔隙度9.2%，井口水温59~70 ℃。地下热水来源于东部梁山和嘉祥地区裸露基岩的大气降水，沿断裂和岩溶不整合面运移加热进入浅部热储，最终在凸起区以热传导为主的热传递方式聚集形成中低温地热田。地热水循环深度为2219~3692 m，水化学类型为SO₄·Cl-Na·Ca和 Cl·SO₄-Na·Ca，TDS为3240~8004 mg∙L⁻¹。利用热储体积法分区带分层系精细评价阳谷凸起南段奥陶系地热资源量，该区地热资源总量28.10×10¹⁸ J，折合标煤0.96×10⁸ t，年开采地热资源量可满足505×10⁴ m²供暖面积，开发前景较好。
- 阳谷凸起南段 /
- 奥陶系 /
- 成因机制 /
- 概念模型 /
- 资源量评价
Abstract: A basin-margin fault-uplift zone usually refers to the high uplift located at the edge of a faulted basin, where deep-seated faults are developed along the basin margin, and the Cenozoic fault distance can exceed thousand meters. With advancements of geothermal exploration, the uplift zone at the basin edge has become a focal point and hotspot for the exploration. Geothermal fields in this area are characterized by shallowly buried depths, favorable reservoir properties, and relatively recent accumulation. Understanding the formation mechanisms of these fields holds important theoretical and practical significance for enriching genetic models of geothermal fields in the basin and guiding their exploration and development. Taking the southern section of the Yanggu Uplift in southwestern Shandong as an example, this study systematically examines the main factors of "source, reservoir, communication, and cover" of the geothermal field based on data from drilling, logging, geophysical prospecting, production testing, and hydrochemical analysis. Using a comprehensive analysis, this study examines the genetic model of the geothermal field, and provides a detailed evaluation of its geothermal resource potential.The results indicate the following: (1) Ordovician karst thermal reservoirs are developed in this area, distributed predominantly in a northeast direction. The top surface of the thermal reservoir is buried at a depth of 1,000 to 1,800 m, becoming shallower toward the north and east and deeper toward the south and west. Taking the Lanliao Fault and secondary faults as boundaries, the study area is divided into three zones: the fault-uplift zone, the fault-terrace zone, and the deep fault zone. In the fault-uplift zone, the top surface of the thermal reservoir is buried at a depth of 1,000 to 1,200 m, with wellhead water temperatures ranging from 59 to 62 ℃. In the fault-terrace zone, the buried depth is 1,200 to1,400 m, and wellhead water temperatures range from 62 to 64 ℃. In the deep fault zone, the buried depth ranges from 1,400 to 1,800 m, with wellhead water temperatures between 64 and 70 ℃. (2) The overall thickness of the Ordovician strata is 600 to 780 m. Vertically, from oldest to youngest, the formations are the Yeli Formation, Liangjiashan Formation, Xiamajiagou Formation, Shangmajiagou Formation, and Fengfeng Formation. The main thermal reservoirs are the Fengfeng Formation, Shangmajiagou Formation, and the upper section of Xiamajiagou Formation, characterized mainly Class I and Class II fractures. The average thickness of the thermal reservoir is 98 m, with an average porosity of 9.2%. Fractures are more developed around the deep fault and at the core and leading edge of the anticline, facilitating the formation of dominant water-rich areas. The permeability coefficient in these zones exceeds 2 m∙d⁻¹. Conversely, the transition zone between the anticline core and the deep fault,where fractures are poorly developed,exhibits permeability coefficient below 0.3 m∙d⁻¹, indicating weak permeability. (3) The southern section of the Yanggu Uplift is affected by the Lanliao deep fault and the bedrock uplift. The average geothermal flow is 68 mW∙m⁻², with the highest values along the Lanliao Fault ranging from 70 to 90 mW∙m⁻², indicating a favorable thermal background. The average geothermal gradient of the cap rock is 2.9 to 4.2 ℃∙hm⁻¹. The high-value area, exceeding 4 ℃∙hm⁻¹, is located in the fault-uplift zone, while the low value area, below 3.0 ℃∙hm⁻¹, is located in the deep fault zone. (4) Based on the analysis of hydrogen and oxygen isotope characteristics of water, the geothermal water in this area comes from atmospheric precipitation, with a recharge elevation ranging from 278 to 620 m. Considering the local geomorphological conditions, it is inferred that the geothermal water mainly derives from the atmospheric precipitation infiltrating the exposed bedrock in the Liangshan and Jiaxiang areas to the east. In the study area, from east to west, the geothermal water migrates along faults and karst unconformity surfaces, heating as it moves into shallow thermal reservoirs. Water ultimately accumulates in uplifted regions, where heat transfer mode is predominantly governed by conduction, resulting in a medium- to low-temperature geothermal field. The circulation depth of geothermal water is 2,219 to 3,692 m. The hydrochemical type evolves from SO₄·Cl-Na·Ca to Cl·SO₄-Na·Ca from east to west. The TDS is 3,240 to 8,004 mg∙L⁻¹. (5) Using the method of thermal reservoir volume, the Ordovician geothermal resources in the southern section of the Yanggu Uplift were comprehensively evaluated based on both horizontal zones and vertical stratifications. The calculation indicate that the total geothermal resources in this area amounts to 28.10×10¹⁸ J, equivalent to 0.96×10⁸ t of standard coal. The annual exploitable geothermal resources can support heating for an area of 505×10⁴ m², indicating promising development prospect.
- southern section of the Yanggu Uplift /
- Ordovician system /
- genetic mechanism /
- conceptual model /
- resource evaluation.

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图 1 阳谷凸起及邻区前新生界地质图和地质剖面图

Figure 1. Pre-cenozoic geological map and geological section of the Yanggu Uplift and its adjacent area

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图 2 阳谷凸起南段奥陶系顶面埋深和盖层地温梯度

Figure 2. Buried depth of the Ordovician top and the geothermal gradient of cap rock in the southern section of the Yanggu Uplift

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图 3 阳谷凸起南段奥陶系热储特征连井对比

Figure 3. Comparison of Ordovician reservoir characteristics in the southern section of the Yanggu Uplift

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图 4 阳谷凸起南段及邻区大地热流分布图（据文献[23]-[25]改）

Figure 4. Distribution map of geothermal flow in the southern section of the Yanggu Uplift and adjacent area (revised according to references 23 to 25)

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图 5 阳谷凸起南段典型钻井深度—温度关系图

Figure 5. Typical drilling depth-temperature relationship in the southern section of the Yanggu Uplift

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图 6 阳谷凸起南段及邻区TDS与离子关系图和氢氧关系图

Figure 6. Relationship between TDS and ions, and the relationship between hydrogen and oxygen in the southern section of the Yanggu Uplift and its adjacent area

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图 7 阳谷凸起南段地热系统成因模式图

Figure 7. Genetic model of geothermal system in the southern section of the Yanggu Uplift

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表 1 阳谷凸起南段典型地热井实际资料

Table 1. Data of typical geothermal wells in the southern section of theYanggu Uplift

井名	井深/ m	水温/ ℃	水量/ (m³∙h⁻¹)	静水位/ m	降深/ m	盖层地温梯度/ (℃∙hm⁻¹)	渗透系数/ (m∙d⁻¹)	导水系数/ (m²∙d⁻¹)
TC1	1546	59	120	37	15	3.7	1.1800	110
TC2	1560	60	122	31	34	4.2	0.5293	63
LD2	1740	64	130	38	7	3.2	2.7394	310
LD3	1708	63	114	43	51	3.0	0.3297	33
LR3	1776	61	128	46	69	3.0	0.2736	23
LX2	1980	65	128	46	34	3.2	0.5553	36
XZ1	2290	70	140	50	25	2.9	0.8260	82

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表 2 阳谷凸起南段及邻区典型地热井岩溶水水化学分析数据

Table 2. Chemical analysis of karst water in typical geothermal wells in the southern section of the Yanggu Uplift and its adjacent areas

构造单元	井点	分析项目/(mg∙L⁻¹)								pH	δ¹⁸O/ ‰	δD/ ‰	水化学类型
构造单元	井点	Na⁺	K⁺	Ca²⁺	Mg²⁺	Cl⁻	${\rm{SO}}_4^{2-}$	${\rm{HCO}}_3^{-}$	TDS	pH	δ¹⁸O/ ‰	δD/ ‰	水化学类型
阳谷凸起	TC1	785.57	38.47	546.55	100.13	890.17	2131.78	131.46	3270.00	7.1	/	/	SO₄·Cl-Na·Ca
	LD3	1000.18	59.58	640.43	123.26	1103.61	2389.49	135.48	4985.00	7.8	/	/	SO₄·Cl-Na·Ca
	LR2	787.79	38.77	531.06	97.36	911.32	2053.36	117.00	3240.00	7.1	−8.94	−69.68	SO₄·Cl-Na·Ca
	LX2	988.23	65.11	637.35	125.12	1079.78	2440.82	133.51	5513.23	7.1	−9.50	−71.70	SO₄·Cl-Na·Ca
	XZ1	1692.00	46.30	862.60	151.30	3105.00	1777.00	284.30	8004.00	6.3	/	/	Cl·SO₄-Na·Ca
菏泽凸起	YS1	256.09	27.41	539.77	127.00	270.87	1906.22	177.09	3239.23	7.4	−9.10	−71.00	SO₄-Ca·Na
	HR1	466.65	36.06	578.20	114.30	449.64	1997.63	215.94	1914.63	6.6	−7.03	−66.63	SO₄-Ca·Na
	DQ1	503.70	33.13	477.30	116.03	452.14	1875.66	234.70	1669.56	7.0	−6.40	−64.85	SO₄-Na·Ca
	HN1	542.86	32.77	445.85	95.52	324.66	2062.89	170.16	1504.45	6.9	−9.39	−63.92	SO₄-Na·Ca
注：阳谷凸起南段地热井为本次研究所测的数据，菏泽凸起地热井为文献搜集数据(来源文献[2]、[3]）。

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表 3 阳谷凸起南段岩溶水地球化学温标计算结果

Table 3. Calculation results of geochemical temperature scale of karst water in the southern section of the Yanggu Uplift

井名	T/℃	T_Na-K/℃	T_K-Mg/℃	$T_{{\mathrm{SiO}}_2} $/℃	循环深度/m
TC1	59.00	142.80	71.73	79.41	2218.86
LD3	63.00	159.20	79.91	86.23	2541.13
LR2	63.00	143.19	72.42	75.11	2246.11
LX2	65.00	168.15	81.92	85.03	2620.14
XZ1	70.00	100.68	71.42	109.15	2206.57

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表 4 阳谷凸起南段奥陶系岩溶热储地热资源评价参数及评价结果

Table 4. Evaluation parameters and results of the Ordovician karst geothermal reservoir of geothermal resources in in the southern section of the Yanggu Uplift

构造单元	面积	层段	有效厚度	孔隙度	平均温度	地热资源总量		可采地热资源总量
构造单元	km²	层段	m	%	℃	地热资源总量/ ×10¹⁸J	折合标准煤/ ×10⁸ t	合计/ ×10¹⁸ J	折合标准煤/ ×10⁸ t
断隆带	78.7	O₂f	15.3	12.2	57	1.33	0.05	0.20	0.01
		O₂sm	53.4	10.1	58	4.69	0.16	0.70	0.02
		O₂xm	24.7	10.4	59	2.22	0.08	0.33	0.01
断阶带	122.5	O₂f	12.9	10.8	59	1.81	0.06	0.27	0.01
		O₂sm	67.2	10.5	60	9.64	0.33	1.45	0.05
		O₂xm	36.2	10.6	61	5.32	0.18	0.80	0.03
深断裂带	23.2	O₂f	23.5	10.2	63	0.68	0.02	0.10	0.00
		O₂sm	48.4	10	65	1.46	0.05	0.22	0.01
		O₂xm	30.1	7.2	68	0.95	0.03	0.14	0.00
总计	224.4	/	/	/	/	28.10	0.96	4.22	0.14
注：O₂f为峰峰组，O₂sm为上马家沟组，O₂xm为下马家沟组。

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