滇中红层膏盐溶蚀特征及其对水质的影响

黄胜东; 赵龙; 黄贵任; 陈积普; 王宇

doi:10.11932/karst20220409

滇中红层膏盐溶蚀特征及其对水质的影响

1.
云南地质工程勘察设计研究院有限公司(一水), 云南昆明 650041

2.
昆明理工大学建筑工程学院, 云南昆明 650500

基金项目: “十四五”国家地下水环境质量考核项目：国家及省级污染防治专项资金(JSKTC-20210102) （合同编号：4532300HT202100029）

详细信息

作者简介: 黄胜东（1978－），男，高级工程师，主要从事水工环地质勘查研究。E-mail： 470605182@qq.com

通讯作者: 陈积普（1981－），男，博士，讲师，主要从事工程地质方面的教学与科研工作。E-mail： cip836@163.com

中图分类号: P642.25

收稿日期: 2022-02-25

刊出日期: 2022-08-25

Dissolution characteristics of gypsum salt in the red beds of central Yunnan Province and their effects on groundwater quality: A case study of Xiejiahe valley in Chuxiong City

1.
Yunnan Research Institute for Geological Engineering Survey and Design Co., Ltd, Kunming, Yunnan 650041, China

2.
School of Architectural Engineering, Kunming University of Science and Technology, Kunming, Yunnan 650500, China

More Information

Corresponding author: CHEN Jipu, cip836@163.com

Received Date: 25 February 2022

Publish Date: 25 August 2022

摘要

摘要:
滇中红层多含有石膏、岩盐等可溶盐矿物，在可溶盐富集地段，地下水往往表现为咸水或微咸水而不适宜饮用。文章以楚雄市谢家河河谷为例，基于钻探、物探、测井、水质分析等综合勘察资料，研究红层膏盐在地下水循环中的溶蚀特征并分析膏盐溶蚀对水质的影响。结果表明：膏盐溶蚀形式主要为散点状膏盐的溶蚀孔洞和裂隙状石膏的溶蚀裂隙，溶蚀强度主要受控于含水介质孔隙发育程度和地下水循环速度；浅层地下水循环速度快，虽可溶盐溶蚀强烈，但对地下水水质影响较弱，水质超标面较小；深层地下水循环速度慢，可溶盐溶蚀后富集于深层承压含水层中，导致地下水水质超标面大；断裂及其影响带导水造成深层承压水向浅层地下水越流，导致浅层地下水水质变差。
- 滇中红层 /
- 膏盐 /
- 溶蚀特征 /
- 地下水循环 /
- 断层 /
- 水质
Abstract:
Red beds in central Yunnan Province are mainly deposited of continental red clastic rocks. Soluble salts in the red beds are enriched in some sections, generating undrinkable salt water or brackish water. Besides, during water resources exploitation, the improper design and construction of water supply drilling will often lead to serial pollution of groundwater or the formation of inferior wells, affecting the project benefit and safety of water supply.

To explore dissolution characteristics of gypsum salt in the red beds of central Yunnan and their effect on groundwater quality, a representative area of Xiejiahe Valley in Lucheng Town of Chuxiong City was selected in this study. Comprehensive survey methods such as geological survey, mapping and drilling were used to analyze lithology, geological structures, aquifers, groundwater types, classification and distribution and dissolution characteristics of gypsum salt in the study area. Based on indicators of sulfur isotope (δ³⁴S), ${\rm{SO}}_4^{2 - }$ concentration and TDS of groundwater, the groundwater quality was studied and the effect of gypsum salt dissolution on groundwater was analyzed.

The Quaternary loose sedimentary layer (Qp^al), early Cretaceous Puchanghe formation (K₁p) mudstone intercalated with sandstone, and Gaofengsi formation (K₁g) sandstone intercalated with mudstone compose the main strata in the study area. Groundwater media types include pore water of loose layer, bedrock fissure water and karst water. Bedrock fissure water is composed of weathering fissure water, interlayer fissure water and structural fissure water. Pore water of loose layer and weathered fissure water constitutes a shallow circulation of groundwater with fast circulation speed. The deep circulation system is mainly composed of interlayer fissure water with pressure and slow circulation speed. The Yi-gan fault (F8), mainly containing vein fissure water, runs through the whole study area. Associated structures developed near monitoring wells lead to water diversion in this section of the fault. There are two types of gypsum salt in red beds of the study area: scattered gypsum salt and fissure gypsum. K5, K7 and K9 boreholes reveal the pseudocrystal of gypsum salt in Puchanghe formation. K1, K2, K6, K8 and K19 boreholes reveal fissure gypsum in Gaofensi formation. Sulfur isotope (δ³⁴S) is positively correlated with ${\rm{SO}}_4^{2 - }$ concentration of borehole water samples, indicating that the high concentration of ${\rm{SO}}_4^{2 - }$ in groundwater is derived from dissolution of gypsum filling in the surrounding rock of aquifer. The plane distribution of fissure gypsum shows that gypsum mainly occurs in the Yi-gan fault and its associated tectonic fractures. Dissolution forms of gypsum and salt are mainly dissolution pores and cracks. Dissolution pores are mainly formed by dissolution of scattered gypsum salt, and dissolution cracks are mainly developed above the underground section of 100m depth. The dissolution intensity of gypsum salt is mainly controlled by the development degree of pores in water-bearing media and the groundwater circulation rate of groundwater. The effect of gypsum salt dissolution on groundwater quality in the study area is significant. A fast speed of shallow fissure groundwater circulation results in basic dissolution of gypsum salt, and soluble salt minerals are strongly dissolved, hence weakly influencing groundwater quality, and contributing to a generally high quality of groundwater. Due to the slow circulation of deep confined groundwater, sulphate is enriched in confined aquifer after gypsum salt dissolution. The concentration of ${\rm{SO}}_4^{2 - }$ is high and most of groundwater exceeds permitted levels. Deep confined water in the fault and in the water diversion section of the influence belt of fault is transported to shallow groundwater, which results in the pollution of shallow groundwater and poor water quality in the area.

Dissolution forms of gypsum salt mainly include dissolution holes of scattered gypsumsalt and dissolution cracks of fissured gypsum, and the dissolution intensity is mainly controlled by development degrees of pores in water-bearing media and groundwater circulation rates of groundwater. Because the speed of shallow fissure groundwater circulation is fast, although soluble salt minerals are strongly dissolved, the influence on groundwater quality is still weak and the area of groundwater exceeding permitted levels is small. Conversely, if the circulation speed of deep fissure groundwater is slow, and soluble salt is enriched in deep confined aquifers after dissolution, resulting in low groundwater quality. Water diversion in the fault and in its influence belt causes deep confined water to flow over to shallow groundwater, which leads to the deterioration of shallow groundwater quality.
- the red beds of central Yunnan Province /
- gypsum salt /
- dissolution characteristics /
- groundwater circulation /
- fault /
- water quality

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图 1 云南红层分布及谢家河河谷位置（据文献[11]）

Figure 1.

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图 2 研究区水文地质略图

Figure 2.

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图 3 研究区地下水循环示意图

Figure 3.

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图 4 钻孔K1、K2和K19岩芯中的裂隙状石膏

Figure 4.

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图 5 研究区K₁g²地层裂隙石膏分布示意图

Figure 5.

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图 6 研究区红层中膏盐溶蚀特征

Figure 6.

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图 7 钻孔揭露溶蚀孔洞发育深度

Figure 7.

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图 8 研究区钻孔水质情况对比

Figure 8.

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表 1 研究区水样δ³⁴S值与 ${\rm{SO}}_4^{2 - }$ 浓度

Table 1. δ³⁴S and ${\rm{SO}}_4^{2 - }$ concentrations of water samples in the study area

样品编号	采样位置	δ³⁴S_V-CDT值/‰	/mg·L⁻¹	样品编号	采样位置	δ³⁴S_V-CDT值/‰	/mg·L⁻¹
1	K8孔（118.0~150.6 m）	26.9	1 914.3	9	K13孔（10~90 m）	25.0	2 218.2
2	监测井（93 m段）	26.8	4 578.0	10	K17孔（57~91 m）	13.5	2.1
3	K7孔（61.5~98.3 m）	−1.5	4.8	11	K20钻孔（0~94 m）	/	0
4	K16孔（43.4~73.0 m）	−1.3	6.0	12	K2钻孔（93~150 m）	26.6	3 356.5
5	K6孔（77.6~121.3 m）	26.4	745.7	13	K9钻孔（0~85 m）	/	12.3
6	K1孔（69.0~121.1 m）	30.0	540.2	14	K6北东200 m 院内机井	/	0.5
7	K14孔（48.0~67.0 m）	−8.7	17.7	15	K10钻孔	25.0	123.4
8	K11孔（65.0~76.6 m）	23.8	925.2	16	K19钻孔（12~91 m）	24.3	645.2

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表 2 石膏充填部位含水层特征与硫酸盐含量动态

Table 2. Aquifer characteristics and sulfate content dynamics of gypsum filling sit

充填位置	充填率	充填段含水情况	孔段硫酸盐含量动态			备注
充填位置	充填率	充填段含水情况	孔段/m	时间/月.日	硫酸盐/mg·L⁻¹	备注
K1(110~121 m)	4.5%	岩芯段裂隙碎裂岩胶结、石膏充填，地下水径流弱	69~95	8.12	540.2
			109~121	8.22	648.0
			50~121	9.20	596.8	孔组抽水后
K2(130~142 m)	3.3%	岩芯段破碎，裂隙发育，部分无充填裂隙含水，地下水径流活动稍强	65~93	8.12	2 480.1
			93~151	8.30	3 356.5
			93~151	11.10	2 225.0	孔组抽水后
K19（69~96 m）	8.6%	岩芯段裂隙泥质胶结、方解石石膏充填，含水贫乏	59~90	10.11	645.2
K19（69~96 m）	8.6%	岩芯段裂隙泥质胶结、方解石石膏充填，含水贫乏	14~90	11.28	738.0

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表 3 研究区钻孔水样TDS和 ${\rm{SO}}_4^{2 - }$ 浓度统计

Table 3. Statistics on TDS and ${\rm{SO}}_4^{2 - }$ concentrations of borehole water samples in the study area

钻孔	取样深度/m	TDS/ mg·L⁻¹	/ mg·L⁻¹	地层描述	钻孔	取样深度/m	TDS/ mg·L⁻¹	/ mg·L⁻¹	地层描述
K1	0~69	1 018.0	460.9	揭露断层破碎带和裂隙状石膏，高丰寺组上段	K9	0~18	228.0	17.5	监测井南西侧山脚，普昌河下段，膏盐假晶
	69~95	1 181.0	540.2		K9	18~84	221.0	12.7	监测井南西侧山脚，普昌河下段，膏盐假晶
	95~121	1 205.0	596.8		K10	0~10	518.0	125.6	F_8-1附近，上部第四系，下部高丰寺风化层
K2	0~67	484.5	96.8	揭露断层破碎带和裂隙状石膏，高丰寺组上段	K10	15~120	492.0	126.7	F_8-1附近，上部第四系，下部高丰寺风化层
	67~93	4 100.5	2 480.1		K11	0~65	187.5	59.6	蔡家冲水库北西角，高丰寺上段，揭露断层
	93~150	5626.5	3 356.5		K11	65~87	1 544.0	951.0	蔡家冲水库北西角，高丰寺上段，揭露断层
K4	5~11	444.0	184.4	上部为第四系，下部高丰寺上段	K13	0~15	196.0	14.9	蔡家冲水库北西角，普昌河下段，揭露断层
K5	0~51	316.5	29.9	上部第四系，下部为普昌河下段，膏盐假晶		15~90	3 275.5	2 218.2
K5	51~80	311.0	44.1	上部第四系，下部为普昌河下段，膏盐假晶		90~129	3 431.0	2 267.0
K6	0~50	205.5	14.2	研究区中段北东侧山坡，高丰寺上段，底部揭露石膏和破碎带	K14	0~22	142.0	6.4	研究区中段断层F_8-2附近，高丰寺上段
	50~78	268.0	80.3			29~67	165.0	6.2
	78~121	1 285.0	811.7			67~120	182.5	17.5
K7	0~61	213.0	0.3	上部第四系，下部为普昌河下段，膏盐假晶	K16	0~73	179.0	6.1	上部为普昌河下段，下部为高丰寺上段
K7	61~104	201.0	6.6	上部第四系，下部为普昌河下段，膏盐假晶	K16	73~97	178.5	5.5	上部为普昌河下段，下部为高丰寺上段
K8	0~30	220.5	17.4	高丰寺上段，断裂带岩体破碎，揭露石膏	K17	0~57	89.0	2.1	河谷下游，上部第四系，下部高丰寺组上段
	30~91	294.5	51.6		K17	57~91	142.0	6.4	河谷下游，上部第四系，下部高丰寺组上段
	91~118	3 016.0	1 685.8		K19	0~12	903.0	336.7	河谷下游F_8-1附近，裂隙状石膏揭露
	118~140	3 057.0	1 914.3		K19	12~90	1 435.0	738.0	河谷下游F_8-1附近，裂隙状石膏揭露

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