河北典型压采区含水层水力层析扫描成像

柴宏利; 刘飞; 甄品娜; 郭晓帅; 刘聪丽; 郭雁辉

doi:10.19509/j.cnki.dzkq.tb20240709

河北典型压采区含水层水力层析扫描成像

doi: 10.19509/j.cnki.dzkq.tb20240709

柴宏利^{a, b,},
刘飞^{a, b, ,},
甄品娜^{a, b},
郭晓帅^{a, b},
刘聪丽^{a, b},
郭雁辉^{a, b}

a.
河北工程大学：水利水电学院
b.
河北工程大学：河北省智慧水利重点实验室，河北邯郸 056038

基金项目: 国家自然科学基金面上项目（42471039）；河北省优秀青年科学基金项目（D2022402013）

详细信息

作者简介:
柴宏利：E-mail：15232626194@163.com

通讯作者:
E-mail：liufei@hebeu.edu.cn

中图分类号: P641.73
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- 文章访问数: 546
- PDF下载量: 21
- 被引次数: 0
出版历程
- 收稿日期: 2024-11-19
- 录用日期: 2025-02-24
- 修回日期: 2025-01-10
- 网络出版日期: 2025-02-24

Hydraulic tomography of typical large-scale aquifers in groundwater exploitation reduction areas of Hebei Province

CHAI Hongli^{a, b
,},
LIU Fei^{a, b
, ,},
ZHEN Pinna^{a, b},
GUO Xiaoshuai^{a, b},
LIU Congli^{a, b},
GUO Yanhui^{a, b}

a.
School of Water Conservancy and Hydroelectric Power, Hebei University of Engineering
b.
Hebei Key Laboratory of Intelligent Water Conservancy, Hebei University of Engineering, Handan Hebei 056038, China

More Information

Author Bio:
E-mail：15232626194@163.com

Corresponding author: E-mail：liufei@hebeu.edu.cn

摘要

摘要:
运用水力层析方法刻画大尺度含水层非均质性的主要困难是寻找能够显著影响区域地下水动态的刺激源，而人为控制下的地下水开采量变化无疑是一个可行的选择。选择河北地下水超采治理试点区之一的邯郸东部平原作为研究对象，利用压采所引起的地下水位响应数据开展了二维承压含水层水力层析扫描成像，探讨了不同先验信息以及观测井布局对水力参数反演效果的影响。结果表明，水力层析法能够有效刻画大尺度含水层非均质性特征，准确的地质分区信息可以明显改善参数的估计效果；相关尺度和方差对参数反演效果影响不显著；为提高含水层参数估计精度，需要充分考虑已有的先验地质信息，并结合已有水井信息，在水文地质条件明显变化区域附近补充完善地下水观测井网络。基于水力层析理念的大尺度含水层非均质性刻画方法，通过智慧式收集河北地下水压采大背景下现有井的地下水开采量和观测数据，以较低的成本刻画大尺度含水层非均质性，省去了额外的打井和抽水试验时间人力成本，具有显著的经济和社会效益。
- 水力层析 /
- 先验地质信息 /
- 大尺度含水层非均质性 /
- 含水层参数 /
- 地下水压采
Abstract: Objective
One of the main challenges in characterizing the heterogeneity of large-scale aquifers using hydraulic tomography is to find effective excitation sources that can significantly affect regional groundwater dynamics. Therefore, human-induced variations in groundwater exploitation amount may be a feasible option.
Methods
The Handan Eastern Plain, one of the pilot areas for groundwater overexploitation control in Hebei Province, was selected as the study area. Hydraulic tomography was applied to a two-dimensional confined aquifer through groundwater level responses caused by exploitation reduction, and the effects of prior geological information and observation well configuration on hydraulic parameter inversion accuracy were further discussed.
Results
The results showed that hydraulic tomography could effectively characterize the heterogeneity of large-scale aquifers, and accurate information of geological zones could significantly improve parameter estimations. Correlation scales and variances had no significant effect on the inversion results. To improve the precision of aquifer parameter estimation, it was necessary to give full consideration to the prior geological information and existing well data, and incorporate new groundwater observation wells into the existing monitoring network in areas with significant changes in hydrogeological conditions.
Conclusion
This novel method, which characterizes the heterogeneity of large-scale aquifers based on hydraulic tomography, intelligently collects groundwater exploitation and observation data from existing wells in Hebei Province against the backdrop of groundwater exploitation reduction. Therefore, this method saves time and labor costs of additional well drilling and pumping tests, and provides remarkable economic and social benefits for mapping large-scale aquifer heterogeneity.
- hydraulic tomography /
- prior geological information /
- large-scale aquifer heterogeneity /
- aquifer parameter /
- groundwater exploitation reduction

HTML全文

图 1 实际观测井和开采井分布、边界条件和地质分区（a）及2018—2023年研究区深层承压水开采量变化（b）

Figure 1. Distribution of observation and production wells, boundary conditions, and geological zones (a) and changes in deep confined groundwater exploitation amount from 2018 to 2023 in the study area (b)

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图 2 导水系数T(a)和储水系数S(b)参考场（黑色粗实线代表地质分区界线）

Figure 2. Reference fields of transmissivity T (a) and storage coefficient S (b)

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图 3 模型正演30口观测井收集的水头响应（1～30为观测井编号，观测井位见图1a）

Figure 3. Hydraulic head responses collected from 30 observation wells in model forward simulation

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图 4 情景A(a～d)、情景B(e～h)和情景C(i～l)导水系数T、储水系数S估计参数场、估计值与真实值散点图

T为导水系数；S为储水系数；$ {{R}}^{\text{2}} $为相关系数；$ {{L}}_{\text{1}} $为绝对误差；$ {{L}}_{\text{2}} $为均方差；下同

Figure 4. Estimated parameter fields and scatter plots of estimated and true values of transmissivity T and storage coefficient S under scenario A (a-d), scenario B (e-h), and scenario C (i-l)

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图 5 4种方案实际流速分量与模拟流速分量散点图

a，b. 方案一HT方法估计的参数场（有先验地质信息）；c，d. 方案二HT方法估计的参数场（无先验地质信息）；e，f. 方案三参数场为4个地质分区均值；g，h. 方案四参数场为区域Ⅰ参数均值。V_X，V_Y分别为地下水流速在X，Y方向上的分量

Figure 5. Scatter plots of observed and simulated flow velocity under four different scenarios

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图 6 不同相关尺度和方差参数反演结果

a～c. X方向相关尺度不变，改变Y方向相关尺度；d～f. Y方向相关尺度不变，改变X方向相关尺度；g～i. lnT，lnS方差值

Figure 6. Inversion results of different correlation scales and variance parameters

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图 7 观测井布局设计

a.实际水井分布位置；b.网格大小为20 km×20 km；c.网格大小为15 km×15 km；d.网格大小为10 km×10 km

Figure 7. Design of observation well configurations

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图 8 不同网格分辨率和观测井布局条件下导水系数T(a～c)和储水系数S(d～f)估计值与真实值散点图

a, d. 新增观测井10口，网格大小为20 km×20 km；b, e. 新增观测井30口，网格大小为15 km×15 km；c, f. 新增观测井40口，网格大小为10 km×10 km

Figure 8. Scatter plots of estimated and true values of transmissivity T (a-c) and storage coefficient S (d-f) under different grid resolutions and observation well configurations

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表 1 非稳定流模型抽水事件（开采井位见图1a）

Table 1. Pumping events in transient flow model

抽水事件	开采井编号	开采强度/ (m³·d⁻¹)	开采时间/d	开采状态
1	P1，P3，P4，P9，P12， P13，P15，P22，P27	−10000	[0，1 000)	正常开采
		−6000	[1 001，2 000)	减采
		0	[2 001，3 000]	停采
2	P2，P5，P8，P10，P16， P17，P20，P23，P25	−10000	[0，1 000)	正常开采
		0	[1 001，2 000)	停采
		−6000	[2 001，3 000]	减采
3	P6，P7，P11，P14，P18， P19，P21，P24，P26	0	[0，1 000)	停采
		−10000	[1 001，2 000)	正常开采
		−6000	[2 001，3 000]	减采

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表 2 不同观测井布局情况下参数估计效果评价指标比较

Table 2. Comparison of performance indicators for parameter estimation under different observation well configurations

增加观测井数量/口		0	10	30	40
总观测井数量/口		30（真实）	40	60	70
lnT	R²	0.77	0.79	0.82	0.85
	L₁	0.172	0.164	0.149	0.144
	L₂	0.053	0.047	0.038	0.034
	斜率	0.82	0.85	0.88	0.90
	截距	0.97	0.76	0.65	0.49
lnS	R²	0.75	0.78	0.81	0.83
	L₁	0.185	0.160	0.155	0.150
	L₂	0.057	0.047	0.043	0.039
	斜率	0.75	0.77	0.81	0.82
	截距	−1.37	−1.14	−1.03	−1.02

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