粤西北连州盆地构造演化对岩溶作用及岩溶塌陷的控制

樊燏; 黄琨; 段慧毓; 林宇航; 罗明明; 万军伟; 温汉辉; 曲金才; 张龙轩

doi:10.19509/j.cnki.dzkq.tb20230120

粤西北连州盆地构造演化对岩溶作用及岩溶塌陷的控制

doi: 10.19509/j.cnki.dzkq.tb20230120

1.
中国地质大学(武汉)环境学院, 武汉 430078
2.
广东省有色金属地质局九四○队, 广东清远 511500

基金项目:

国家自然科学基金项目 42172276

详细信息

作者简介:
樊燏, E-mail: yufan@cug.edu.cn

通讯作者:
万军伟, E-mail: wanjw@cug.edu.cn

中图分类号: P642.25
计量
- 文章访问数: 342
- PDF下载量: 59
- 被引次数: 0
出版历程
- 收稿日期: 2023-03-07
- 录用日期: 2023-09-01
- 修回日期: 2023-05-28

Control of tectonic evolution on karstification and karst collapse in the Lianzhou Basin, northwestern Guangdong Province

1.
School of Environmental Studies, China University of Geosciences(Wuhan), Wuhan 430078, China
2.
No. 940 Branch of Geology Bureau for Nonferrous Metals of Guangdong Province, Qingyuan Guangdong 511500, China

More Information

Author Bio:
FAN Yu, E-mail: yufan@cug.edu.cn

Corresponding author: WAN Junwei, E-mail: wanjw@cug.edu.cn

摘要

摘要:
目前对连州盆地中生代以来的形成演化及其与岩溶发育规律的响应关系尚缺乏系统性认识。基于最新地质调查、水文地质钻探、溶蚀试验和三维地质建模, 结合已有地质资料, 划分了盆地构造演化阶段并探讨了各阶段岩溶作用。前白垩纪, 在地壳升降运动下沉积较强溶蚀能力碳酸盐岩, 这为岩溶发育奠定了物质基础。印支运动促使垂向叠置地层形成EW向构造, 燕山运动导致其横跨-斜跨叠加NE-SW向构造, 这些地质构造控制碳酸盐岩地质结构和空间展布特征及溶蚀性能, 山脉和水系分布确立, 但岩溶整体不发育。白垩纪-古近纪发育陆内山间断陷汇流湖盆, 地壳缓慢隆升加强了盆地周围岩溶作用, 现保留早期岩溶台面。后期被冲洪积物埋藏-充填-固结成岩, 岩溶基本停止发育, 形成厚覆盖型红层盆地。新近纪以来, 地壳快速抬升导致盆地四周山体不断抬高, 河流深切, 岩溶强烈发育, 塑造多级岩溶台面。盆地内部分白垩系红层被剥蚀或切穿, 岩溶作用复活, 水系经多次变迁和贯通后, 形成第四系浅覆盖型岩溶断陷盆地。构造演化控制岩溶发育规律, 岩溶作用影响盆地内部结构, 土体结构孕育岩溶地面塌陷。研究成果可为认识覆盖型岩溶区岩溶塌陷条件提供科学依据和指导。
- 连州盆地 /
- 构造演化 /
- 地壳活动 /
- 岩溶作用 /
- 岩溶塌陷
Abstract: Objective
There is still a lack of systematic understanding of the evolution process of the Lianzhou Basin since the Mesozoic and its response to karstic development.
Methods
Based on the comprehensive analysis of the latest field geological investigations, hydrogeological drilling, dissolution experiments, and three-dimensional geological modelling, the tectonic evolution stages of the basin can be divided, and the karstification of each stage can be discussed by considering the existing geological data.
Results
Before the Cretaceous, carbonate rocks with strong dissolution were successively deposited under the rise or fall movement of the crust, which laid a material foundation for karstic development. The Indosinian movement caused vertically multilayered strata to form an E-W-trending structure, and the Yanshanian movement made the straddle-oblique superimposed a NE-SW-trending structure. They controlled the geological structures, spatial distribution, and dissolution behaviors of carbonate strata. And the distribution of mountains and river system were established. However, karst generally does not develop. An intracontinental and intermountain faulted confluence lake basin formed from the Cretaceous to the Palaeogene, the slow crustal uplift strengthened the karstification around the basin, and it currently retains the early karst platform. Later, they were buried-filled-consolidated by alluvial deposits; therefore, karst basically stopped developing, generating a thick-covered red strata basin. Since the Neogene, the rapid uplift of the crust has led to the continuous elevation of mountains around the basin, deepening of rivers, and strong development of karst, shaping multilevel karst platforms. When part of the Cretaceous red strata in the basin are denuded or cut through, karstification is reactivated. After many changes and penetrations of water systems, the graben basin formed, with karst strata covered by Quaternary sediments, Tectonic evolution controls karstic development, karstification influences the internal structure of the basin, and soil structure causes karst ground collapse.
Conclusion
This study can provide a scientific basis and guidance for understanding karst collapse conditions in covered karst areas.
- Lianzhou Basin /
- tectonic evolution /
- crustal movement /
- karstification /
- karst collapse
注释:

所有作者声明不存在利益冲突。

HTML全文

图 1 研究区岩溶水文地质概图

Figure 1. Karst hydrogeological map of the study area

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图 2 已发岩溶塌陷特征

Figure 2. Karst collapse characteristics

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图 3 连州盆地云灰岩、灰云岩与灰岩、白云岩溶蚀度R_si(a, c)和化学溶蚀度R_di(b, d)随时间变化曲线

Figure 3. Curves of the dissolution rate (a, c) and chemical dissolution rate (b, d) of dolomitic limestone, calcite dolomite, limestone and dolomite over time in the lianzhou Basin

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图 4 连州市主城区第四系覆盖层三维地质结构模型

Figure 4. Three-dimensional geological structure of Quaternary covered layers in main urban area of Lianzhou City

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图 5 连州市主城区垂向岩溶发育规律

Figure 5. Vertical karst development law in main urban area of Lianzhou City

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图 6 枯、丰水期岩溶地下水位等值线图

Figure 6. Contour map of karst groundwater level in dry(a) and wet(b) seasons

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图 7 连州盆地构造形成演化过程与岩溶作用示意图

T₁d².大冶组二段；T₁d¹.大冶组一段；P₂t.童子岩组; P₁q-m.栖霞-茅口组；C₂h.壶天组；C₁z.梓门桥组；C₁c.测水组；C₁s.石磴子组；C₁l.连县组；D₃r.融县组；下同

Figure 7. Schematic diagram of tectonic evolution formation and karstification in Lianzhou Basin

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图 8 发育的岩溶洞穴野外出露特征

Figure 8. Occurrences of karst caves developed in the wild

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图 9 受NNE向裂隙和近EW向断裂发育的溶洞野外特征

Figure 9. Exposed characteristics of karst caves developed by NNE-trending fissures or EW-trending faults

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图 10 岩溶塌陷灾害点形成条件特征

a.地下水主径流带黏性土软化塑性变形; b.碳酸盐岩与非碳酸盐岩交界带砂性土渗透变形; c.地下水排泄带砂性土渗透变形

Figure 10. Formation condition characteristics of karst collapse disaster points

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表 1 连州盆地碳酸盐岩溶蚀试验结果

Table 1. Corrosion test results of carbonatite rocks in the Lianzhou Basin

地层	岩性描述	矿物组成φ_B/%			比溶蚀度K_v		比化学溶蚀度K_cv
地层	岩性描述	方解石	白云石	酸不溶物	5次试验均值	地层均值	5次试验均值	地层均值
大冶组一段	灰色薄-中厚层状微晶泥质灰岩	79.18	3.84	16.98	0.79	0.79	0.92	0.92
栖霞组-茅口组	深灰色厚层状含燧石微晶灰岩	95.45	3.00	1.55	0.93	0.93	0.93	1.01
壶天组	灰色厚层微晶灰岩	97.51	1.01	1.48	1.00	1.03	0.85	0.98
壶天组	灰白色厚层微晶白云岩	2.22	95.63	2.15	1.06	1.03	1.11	0.98
梓门桥组	灰色厚层微晶灰质白云岩	28.13	69.78	2.09	0.75		0.78
	灰色厚层微晶灰质白云岩	43.92	54.58	1.50	1.13		0.98
	灰色厚层微晶含灰质白云岩	24.10	68.03	7.87	1.30		0.97
	灰色厚层微晶灰质白云岩	24.99	72.43	2.58	1.26	1.04	1.18	0.97
	深灰色中厚层细晶含灰质白云岩	7.67	90.50	1.83	1.06		1.06
	灰黑色厚层细晶灰质白云岩	25.48	71.28	3.24	0.92		0.89
	灰黑色厚层含炭质微晶灰岩	96.45	1.99	1.57	0.88		0.94
石磴子组	灰黑色薄-中层微晶灰岩	71.41	1.55	27.04	1.03		1.06
	灰黑色厚层含炭质细晶灰岩	94.58	2.05	3.37	0.84		0.90
	灰黑色厚层微晶含白云质灰岩	86.88	10.09	3.03	0.94	0.92	1.11	1.02
	深灰色厚层微晶白云岩	4.01	91.39	4.60	0.83		1.01
	灰黑色薄-中层微晶纯灰岩	93.72	3.36	2.92	0.95		1.00
连县组	灰黑色厚层细晶含白云质灰岩	83.01	14.81	2.18	0.99		0.93
	灰色厚层细晶含白云质灰岩	86.36	6.43	7.20	1.05		1.14
	灰黑色厚层细晶含白云质灰岩	80.57	17.79	1.64	1.05	0.99	1.17	1.07
	灰黑色厚层细晶白云岩	4.13	94.89	0.98	0.87		1.00
	浅灰色厚层微晶含灰质白云岩	10.67	86.08	3.25	0.99		1.13
融县组	深灰色厚层细晶白云质灰岩	63.46	32.39	4.15	1.48	1.22	1.04	1.03
	深灰色薄-中厚层细晶灰岩	87.97	7.97	6.78	1.00		0.97
	深灰色厚层微晶豹皮灰岩	89.33	3.89	6.78	1.08		1.04
	深灰色厚层微晶含白云质灰岩	81.89	9.78	8.33	1.32		1.05

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