山东省肥城断块岩溶水系统地下水水化学特征及演化分析

张文强; 滕跃; 唐飞; 王金晓; 许庆宇; 张海林

doi:10.11932/karst20230515

山东省肥城断块岩溶水系统地下水水化学特征及演化分析

doi: 10.11932/karst20230515

张文强^{1, 2,},
滕跃^{1, 2, ,},
唐飞³,
王金晓^{1, 2},
许庆宇^{1, 2},
张海林^{1, 2}

1.
山东省地质矿产勘查开发局八〇一水文地质工程地质大队, 济南山东 250014
2.
山东省地下水环境保护与修复工程技术研究中心, 济南山东 250014
3.
山东省地质矿产勘查开发局第五地质大队, 泰安山东 271000

基金项目: 山东省地质勘查项目“山东省1∶5万孝里、石横幅水文地质调查”（鲁勘字（2021）46号）

详细信息

作者简介:
张文强（1992－），男，硕士研究生，工程师，研究方向为水文地质环境地质。E-mail：1024700957@qq.com

通讯作者:
滕跃（1994－），女，硕士研究生，工程师，研究方向为岩溶水化学。E-mail：1609381771@qq.com

中图分类号: P641.3
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- 文章访问数: 250
- HTML浏览量: 83
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- 被引次数: 0
出版历程
- 收稿日期: 2023-04-20
- 录用日期: 2023-07-20
- 修回日期: 2023-07-19
- 网络出版日期: 2023-10-20
- 刊出日期: 2023-10-01

Groundwater hydrochemical characteristics and evolution of the karst water system in the Feicheng fault block in Shandong Province

ZHANG Wenqiang^{1, 2
,},
TENG Yue^{1, 2
, ,},
TANG Fei³,
WANG Jinxiao^{1, 2},
XU Qingyu^{1, 2},
ZHANG Hailin^{1, 2}

1.
801 Institute of Hydrogeology and Engineering Geology, Shandong Provincial Bureau of Geology & Mineral Resources, Jinan, Shandong 250014, China
2.
Shandong Engineering Research Center for Environmental Protection and Remediation on Groundwater, Jinan, Shandong 250014, China
3.
NO.5 Geological Brigade of Shandong Provincial Exploration Bureau of Geology and Mineral Resources, Taian, Shandong 271000, China

摘要

摘要: 地下水是肥城地区最主要的供水水源，近年来受到工农业生产、煤矿开采、闭坑、矿井排水等人类活动影响，肥城地区地下水动力场及化学场都发生了变化，为查明地下水的环境质量状况，文章在研究水文地质调查和样品采集分析基础上，综合运用数理统计方法、水化学方法（Piper三线图、Gibbs模型、矿物饱和指数、离子比例分析）等，探讨肥城断块地下水水化学特征及演化规律。结果表明：（1）研究区地下水均呈弱碱性，$ {\mathrm{C}\mathrm{a}}^{2+} $、$ {\mathrm{M}\mathrm{g}}^{2+} $、$ {{\mathrm{H}\mathrm{C}\mathrm{O}}_{3}}^{-} $和$ {\mathrm{S}\mathrm{O}}_{4}^{2-} $为主要离子，主要来源于方解石、白云石及石膏溶解；矿物饱和指数表明方解石和白云石绝大多数处于饱和状态，石膏和岩盐矿物呈溶解未饱和状态。（2）区内岩溶水化学类型主要为$ {\mathrm{H}\mathrm{C}\mathrm{O}}_{3}-\mathrm{C}\mathrm{a}\left(\mathrm{M}\mathrm{g}\right) $型，其次为$ {\mathrm{H}\mathrm{C}\mathrm{O}}_{3}·{\mathrm{S}\mathrm{O}}_{4}-\mathrm{C}\mathrm{a} $型和$ {\mathrm{H}\mathrm{C}\mathrm{O}}_{3}·\mathrm{C}\mathrm{l}-\mathrm{C}\mathrm{a} $型。孔隙水主要为$ {\mathrm{S}\mathrm{O}}_{4}·{\mathrm{H}\mathrm{C}\mathrm{O}}_{3}-\mathrm{C}\mathrm{a} $型、局部出现$ {\mathrm{S}\mathrm{O}}_{4}{·\mathrm{N}\mathrm{O}}_{3}-\mathrm{C}\mathrm{a} $型。河流水化学类型相对复杂，包括$ {\mathrm{S}\mathrm{O}}_{4}·{\mathrm{H}\mathrm{C}\mathrm{O}}_{3}-\mathrm{C}\mathrm{a}·\mathrm{N}\mathrm{a} $型、$ \mathrm{C}\mathrm{l}·{\mathrm{S}\mathrm{O}}_{4}-\mathrm{C}\mathrm{a}·\mathrm{N}\mathrm{a} $型等。（3）区内地下水中$ {\mathrm{C}\mathrm{l}}^{-} $、$ {\mathrm{S}\mathrm{O}}_{4}^{2-} $和$ {\mathrm{N}\mathrm{O}}_{3}^{-} $含量相比1999年、2013年显著升高。裂隙水及岩溶水水质整体较好，局部呈点状变差，孔隙水及河水水质普遍较差，影响区域地下水水质的主要因素有化肥施用、禽畜养殖、生活污水下渗以及煤矿排水等。
- 岩溶水系统 /
- 地下水 /
- 水化学特征 /
- 演化规律 /
- 肥城断块
Abstract: The Feicheng area is one of the important industrial bases in Shandong Province with the early development of coal mine, power generation and chemical industry. Besides, vegetable farming is widely distributed. Karst groundwater is the main source of water supply and the only source of drinking water in this area. In recent years, due to human activities such as industrial and agricultural exploitation of groundwater, and reduction of water emissions from coal mine closures, the groundwater dynamic and chemical fields in this area have undergone changes. The current status of groundwater environmental quality needs to be determined. On the basis of hydro-geological survey, this study collected 59 groundwater samples and 6 river water samples in the dry season of 2022, and comprehensively used mathematical statistical methods, hydrochemical methods (Piper three-line diagram, Gibbs model, mineral saturation index, ion proportion analysis) to explore the hydrochemical characteristics and evolution rules of groundwater in the Feicheng fault block.The results show that, (1) The average pH of groundwater in the study area is 7.34–7.47, all of which are weakly alkaline, and Ca²⁺, Mg²⁺, ${\rm{HCO}}_3^{-}$ and ${\rm{SO}}_4^{2-}$ are the main ions in the water. The hydrochemical composition is mainly controlled by water rock interaction, while the influence of atmospheric precipitation and evaporation concentration is relatively small. The water-rock interaction of calcite and dolomite plays a major role in controlling the chemical composition of karst water and fissure water, and the dissolution of evaporite plays an important role in the chemical composition of pore water. The mineral saturation index shows that most of calcite and dolomite is in a saturated state, while gypsum and halite minerals are in a dissolved but unsaturated state.(2) Karst hydrochemical types in the area are mainly HCO₃-Ca (Mg) type, accounting for 47.9%, followed by HCO₃·SO₄-Ca type and HCO₃·Cl-Ca type, 16.7% and 20.8%, respectively. Pore water is mainly of SO₄·HCO₃-Ca type and HCO₃·Cl·SO₄-Ca type, with SO₄·NO₃-Ca type appearing locally in the area of Wangguadian town. The chemical types of river water are relatively complex, including SO₄·HCO₃-Ca·Na type, Cl·SO₄-Ca·Na type, etc.(3) From the perspective of component content, the average TDS content of pore water, karst water, and fissure water is 1,207.13 mg·L⁻¹, 670.96 mg·L⁻¹, 514.5 mg·L⁻¹, respectively. The coefficient of variation of Ca²⁺ and Mg²⁺ in groundwater is relatively small, indicating that they are relatively stable ions. The average values of ${\rm{SO}}_4^{2-}$, Cl⁻ and ${\rm{NO}}_3^{-}$ in pore water are 288.29 mg·L⁻¹, 155.86 mg·L⁻¹, 195.41 mg·L⁻¹, respectively, with high content and small coefficient of variation, indicating that they are mainly influenced by external inputs from human activities. The content of ${\rm{SO}}_4^{2-}$, Cl⁻ and ${\rm{NO}}_3^{-}$ in karst water is relatively low, but the coefficient of variation is large, with uneven concentration distribution, and occurrence of enrichment in local areas. The average ${\rm{SO}}_4^{2-}$ in the Huihe river reaches 345.83 mg·L⁻¹, which is much higher than that of the surrounding groundwater and has a small coefficient of variation, indicating that its source is mainly from external inputs and may be related to the drainage of surrounding coal mines.(4) Some sources of Ca²⁺ are related to the dissolution of gypsum minerals and the infiltration of pollutants containing Cl⁻ and ${\rm{NO}}_3^{-}$, and the nitrate pollutants mixed into aquifers may promote the dissolution of carbonate rocks. The cation exchange is weak in groundwater, but strong in river water.(5) From a time-scale perspective, the groundwater quality in the study area has shown a decreasing trend compared to the quality in 1999 and 2013, with significant increases in the content of Cl⁻, ${\rm{SO}}_4^{2-}$, and ${\rm{NO}}_3^{-}$ in groundwater over the years. From the perspective of groundwater types and spatial distribution, the chemical characteristics of groundwater in the Feicheng area are significantly influenced by human activities. Both the concentrations of nitrogen and chlorine are generally low in the fissure water of magmatic rocks, and hence the water quality is relatively the best. The overall quality of karst water is good, and the rise of the water level in the closed pit mine in Feicheng has not caused cross-layer pollution to the surrounding karst water. However, there are local occurrences of "high nitrogen" or "high chlorine" in Wangzhuang, Taoyuan, Shiheng, Dayang, and other places, which may be affected by pollution sources such as agricultural fertilization, livestock breeding, and domestic sewageinfiltration. Both the concentrations of nitrogen and chlorine are high in most of the pore water, and hence the water quality is generally poor, with ${\rm{NO}}_3^{-}$, as the main ion exceeding the permitted level, which may be related to the application of chemical fertilizer for large-scale agricultural vegetable farming in the study area, and the infiltration of surface nitrate and other pollutants into the groundwater with rainwater. The nitrogen concentration in both Kangwang river and the Huihe river is generally low, while those of chlorine and sulfur are high, reflecting the significant impact of urban sewage discharge and coal mine drainage on these two rivers.
- karst water system /
- groundwater /
- hydrochemical characteristics /
- evolution law /
- the Feicheng fault block

HTML

图 1 研究区采样点分布图

Figure 1. Distribution of sampling points in the study area

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图 2 研究区水文地质剖面图

Figure 2. Hydrogeological profile of the study area

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图 3 研究区岩溶地下水离子含量分布图（a. ${\rm{NO}}_3^{-}$/ b. TDS）

Figure 3. Distribution of ion content in karst water in the study area（a. ${\rm{NO}}_3^{-}$/ b. TDS）

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图 4 研究区采样点Piper三线图

Figure 4. Piper diagram of sampling points in the study area

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图 5 地下水主要化学组分相关性分析可视化

Figure 5. Visualization of correlation analysis of main chemical components of groundwater

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图 6 Gibbs水化学图

Figure 6. Gibbs hydrochemistry diagram

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图 7 主要离子比例关系图

Figure 7. Ratio relationship of main ions

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图 8 肥城盆地地下水主要离子含量箱图^[28]（a 为1999年，b 为2013年）

Figure 8. Box diagram of main ion contents in groundwater of Feicheng basin^[28]（a. 1999，b. 2013）

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图 9 地下水主要离子含量箱图（a 为岩溶水，b 为孔隙水，2022年）

Figure 9. Box diagram of main ion contents in groundwater (a. karst water/b. pore water, 2022)

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图 10 研究区河流断面水化学离子含量

Figure 10. Hydrochemical ion content of river section in the study area

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表 1 研究区地下水及河水水化学组分统计

Table 1. Statistics of chemical components of groundwater and river water in the study area

水样类型	项目	水化学/mg·L⁻¹							TDS mg·L⁻¹	pH
水样类型	项目	Na⁺	Ca²⁺	Mg²⁺	Cl⁻	${\rm{SO}}_4^{2-}$	${\rm{HCO}}_3^{-}$	${\rm{NO}}_3^{-}$	TDS mg·L⁻¹	pH
松散岩类孔隙水	最大值	174.00	311.00	54.60	223.00	470.00	481.00	303.00	1 380.68	7.43
	最小值	33.20	166.00	25.50	110.00	199.00	286.00	11.50	931.00	7.07
	平均值	61.51	262.14	43.91	155.86	288.29	366.02	195.41	1 207.13	7.34
	标准差	50.40	57.91	9.64	42.96	95.79	73.69	143.19	143.19	0.13
	变异系数	0.82	0.22	0.22	0.28	0.33	0.20	0.12	0.12	0.02
碳酸盐岩类裂隙岩溶水	最大值	137.00	309.00	51.80	206.00	720.00	463.01	237.00	1 347.54	7.74
	最小值	3.84	60.10	9.80	15.10	18.60	116.49	0.22	285.66	7.10
	平均值	29.07	152.69	26.87	72.37	138.64	299.92	83.02	670.96	7.42
	标准差	26.11	52.59	10.00	52.67	121.42	56.95	56.92	250.99	0.16
	变异系数	0.90	0.34	0.37	0.73	0.88	0.19	0.69	0.37	0.02
岩浆岩变质岩类裂隙水	最大值	30.70	160.00	33.90	51.00	169.00	295.47	127.00	611.58	7.60
	最小值	5.18	93.70	11.60	28.40	67.90	194.95	27.80	427.37	7.30
	平均值	15.96	119.18	21.03	35.05	101.95	251.94	71.03	514.50	7.47
	标准差	11.40	28.62	9.37	10.70	45.51	47.49	41.45	76.07	0.12
	变异系数	0.71	0.24	0.45	0.31	0.45	0.19	0.58	0.15	0.02
河水	最大值	153.00	150.00	45.40	249.00	468.00	341.00	23.90	1 140.31	7.79
	最小值	91.90	103.00	28.90	58.40	220.00	127.94	2.89	766.12	7.40
	平均值	122.65	117.67	36.72	143.80	345.83	216.26	14.26	908.73	7.58
	标准差	19.86	17.39	6.26	71.20	113.62	71.47	8.18	127.76	0.15
	变异系数	0.16	0.15	0.17	0.50	0.33	0.33	0.57	0.14	0.02

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