层状非均质性影响下河流对地下水的补给过程研究

吴佩鹏; 束龙仓; 李福林; 陈华伟

doi:10.16030/j.cnki.issn.1000-3665.202208065

层状非均质性影响下河流对地下水的补给过程研究

doi: 10.16030/j.cnki.issn.1000-3665.202208065

吴佩鹏^{1, 2,},
束龙仓^3, ,,
李福林⁴,
陈华伟⁴

1.
南京水利科学研究院水文水资源与水利工程科学国家重点实验室，江苏南京　210098
2.
吉林大学新能源与环境学院，吉林长春　130061
3.
河海大学水文水资源学院，江苏南京　210098
4.
山东省水利科学研究院，山东济南　250013

基金项目: “一带一路”水与可持续发展科技基金项目（2020nkms05）；国家自然科学基金项目（42102286）；国家重点研发计划项目（2021YFC3200504）

详细信息

作者简介:
吴佩鹏（1989-），男，博士，讲师，主要从事地下水系统理论研究。E-mail：hydrogeowu@jlu.edu.cn

通讯作者:
束龙仓（1964-），男，博士，教授，博导，主要从事地下水资源评价与管理研究。E-mail：lcshu@hhu.edu.cn

中图分类号: P641.2
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出版历程
- 收稿日期: 2022-08-15
- 修回日期: 2022-10-18
- 网络出版日期: 2023-04-17
- 刊出日期: 2023-05-15

Influence of stratified heterogeneity on the recharge from surface water to groundwater

WU Peipeng^{1, 2
,},
SHU Longcang^{3
, ,},
LI Fulin⁴,
CHEN Huawei⁴

1.
State Key Laboratory of Hydrology-Water Resources and Hydraulic Engineering, Nanjing Hydraulic Research Institute, Nanjing, Jiangsu　210098, China
2.
College of New Energy and Environment, Jilin University, Changchun, Jilin　130061, China
3.
College of Hydrology and Water Resources, Hohai University, Nanjing , Jiangsu　210098, China
4.
Water Resources Research Institute of Shandong Province, Jinan, Shandong　250013, China

摘要

摘要: 河流对地下水的补给过程研究是科学认识水循环规律及地下水资源可持续管理的基础。河床沉积层与其下伏潜水含水层岩性差异是河流下伏含水层的主要结构特征，也是控制河流对地下水补给过程的主要因素。为揭示含水介质分层结构特征影响下河流对地下水的补给过程，基于黄河干流河南段野外试验结果，建立了地表水地下水相互作用概念模型，并以地下水流路径为对象，精细刻画了地表水地下水的相互作用过程。结果表明：（1）河流对地下水的补给量主要受河床沉积层渗透性影响，河床沉积层厚度变化对河流向地下水的补给量影响不大。即：河床低渗透性沉积物的存在是河流向地下水补给量降低的主要原因，当河床沉积层与其下伏含水层厚度比（H_S/H）由0增大为0.125时，河流向地下水补给量的减小幅度达72%。（2）与均质条件相比，河床沉积层渗透性及其厚度变化均明显改变了河水向地下水补给的水流路径及径流时间。随着河床沉积物与下伏含水层渗透系数比K_U/K_L的增大，河水向地下水补给的水流路径穿透深度增大，径流时间延长。（3）河流对地下水的补给量及地下水径流时间对低渗透性河床沉积层渗透系数的敏感性随渗透系数的减小而增大，同时，地下水径流时间对低渗透性河床沉积层的厚度变化较为敏感，且随着厚度的增大，敏感性增强。研究成果可为地下水资源管理及可持续开发提供参考依据。
- 河床沉积物 /
- 层状非均质 /
- 地表水地下水交互 /
- 渗透系数 /
- 数值模拟
Abstract: Knowledge of the recharge from surface water to groundwater is the basement of the scientific understanding of water cycle and the sustainable management of groundwater resources. Meanwhile, the layered heterogeneity is the main structural feature of riverbed sediments (i.e., the lithologic difference between riverbed sediments and the underlying aquifer) and the main factor that controlling the recharge from surface water to groundwater. To reveal the influence mechanism of layered structure of pore media on the recharge from surface water to groundwater, a conceptual model of surface water and groundwater interaction is established based on the field test results of Henan reaches of the Yellow River, and the process of the recharge from surface water to groundwater interaction is described using flow path as the object. The results show that the exchange flux of surface water and groundwater is mainly affected by hydraulic conductivity of riverbed sediments, and the change of the thickness of riverbed sediments has little effect on the exchange flux between surface water and groundwater. That is, the increase of the ratio of the thickness of the sediments to that of the underlying aquifer (H_S/H) from 0 to 0.125 leads to the interaction flux decreased by 72%, indicating that the existence of the low permeability layer is the main reason that decreases the interaction flux between surface water and groundwater. The change of the permeability and the thickness of riverbed sediments has obviously changed the flow path from surface water to groundwater and the travel time. Specifically, the increase in K_U/K_L leads to a lager penetration depth of groundwater flow and lager travel times. The sensitivity of exchange flux between surface water and groundwater and groundwater travel time to the hydraulic conductivity of riverbed sediments increases with the decreasing hydraulic conductivity. At the same time, the groundwater travel time is more sensitive to the change of the thickness of the low permeability riverbed sediments, and the sensitivity increases with the increasing thickness. The research results can provide reference for groundwater resource management and sustainable development.
- riverbed sediment /
- stratified heterogeneity /
- surface water-groundwater interaction /
- hydraulic conductivity /
- numerical modeling

HTML全文

图 1 试验断面位置图

Figure 1. Location of the test sections

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图 2 竖管试验原理图

Figure 2. Schematic diagram of the standpipe test

下载: 全尺寸图片幻灯片

图 3 黄河下游地表水地下水相互作用数值模拟的概念模型

Figure 3. Conceptual model for numerical simulation of surface water-groundwater interaction in the lower Yellow River

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图 4 河床沉积物的渗透系数、厚度变化条件下地表水地下水转化量变化规律

Figure 4. Effect of the variation of the hydraulic conductivity of riverbed sediments and the variation of the thickness of riverbed sediments on the flux exchange between surface water and groundwater.

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图 5 河床沉积物渗透系数变化条件下地表水地下水转化路径及相应径流时间

Figure 5. Flow paths from surface water to groundwater and the corresponding travel times under the changing hydraulic conductivity of riverbed sediments

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图 6 河床沉积物厚度变化条件下地表水地下水转化路径及径流时间

Figure 6. Flow paths from surface water to groundwater and the corresponding travel times under the condition of changing sediment thickness

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图 7 河床沉积物的渗透系数、厚度变化条件下地表水地下水转化的径流时间变化规律

Figure 7. Effect of the variation of hydraulic conductivity of riverbed sediments, and the variation of sediment thickness on the travel times of groundwater recharged by surface water

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图 8 地表水地下水转化量及地下水径流时间对河床沉积物渗透系数变化的敏感性

Figure 8. Sensitivity of exchange flux between surface water and groundwater and groundwater travel times to the change of riverbed hydraulic conductivities

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图 9 地表水地下水转化量及地下水径流时间对河床沉积物厚度变化的敏感性

Figure 9. Sensitivity of exchange flux between surface water and groundwater and groundwater travel times to the change of thickness of riverbed sediments

下载: 全尺寸图片幻灯片

表 1 不同试验断面不同点位渗透系数竖管试验结果

Table 1. Standpipe test results of hydraulic conductivity at different points in different test sections /（m·d⁻¹）

断面	测点编号1	测点编号2	测点编号3	测点编号4	测点编号5	测点编号6
桃花峪	4.500	2.800	3.400	0.014	6.000	2.400
	4.800	2.700	3.800	0.010	5.800	2.100
	4.000	1.800	3.000	0.012	4.900	2.500
	3.400	2.000	4.000	0.009	6.400	1.800
平均值	4.175	2.325	3.550	0.011	5.775	2.200
花园口	2.400	1.780	2.530	2.180	1.720	0.240
	2.140	1.690	2.320	2.980	0.980	0.190
	1.980	2.010	2.510	2.570	1.540	0.540
	2.070	1.750	1.890	1.690	1.210	0.810
平均值	2.148	1.808	2.313	2.355	1.363	0.445
柳园口	1.570	0.021	0.140	0.001	1.210	0.850
	1.280	0.009	0.009	0.001	1.080	0.940
	1.370	0.021	0.014	0.005	0.970	0.090
	2.150	0.050	0.021	0.008	0.520	0.120
平均值	1.593	0.025	0.046	0.004	0.945	0.500

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