华北平原古海侵事件导致浅层地下水咸化过程模拟

黄义鸿; 杨杰; 李和学; 刘强; 李俊霞

doi:10.19509/j.cnki.dzkq.tb20230709

华北平原古海侵事件导致浅层地下水咸化过程模拟

doi: 10.19509/j.cnki.dzkq.tb20230709

黄义鸿^1,,
杨杰²,
李和学³,
刘强³,
李俊霞^1, ,

1 .
中国地质大学（武汉）环境学院，武汉 430078
2 .
湖北省地质实验测试中心，武汉 430034
3 .
河北省地矿局第四水文工程地质大队，河北沧州 061000

基金项目: 国家自然科学基金项目（42177067）

详细信息

作者简介:
黄义鸿：E-mail：yar1001826@163.com

通讯作者:
E-mail：jxli@cug.edu.cn

中图分类号: P641
计量
- 文章访问数: 139
- PDF下载量: 8
- 被引次数: 0
出版历程
- 收稿日期: 2023-12-20
- 录用日期: 2024-04-24
- 修回日期: 2024-04-23
- 网络出版日期: 2025-09-01

Numerical simulation of shallow groundwater salinization process induced by paleo-seawater transgression in North China Plain

1 .
School of Environmental Studies, China University of Geosciences(Wuhan), Wuhan 430078, China
2 .
Geological Experimental Testing Center of Hubei Province, Wuhan 430034, China
3 .
The Fourth Hydrological Engineering Geology Brigade of Hebei Geological and Mining Bureau, Cangzhou Hebei 061000, China

More Information

Author Bio:
E-mail：yar1001826@163.com

Corresponding author: E-mail：jxli@cug.edu.cn

摘要

摘要:
为了研究受到晚更新世和全新世海侵、现代海水入侵和蒸发作用共同影响下的地下水咸化过程，以沧州地区2个浅层含水层组作为研究对象，基于一系列古环境演化资料，运用SEAWAT软件建立了二维古水文地质模型，模拟了全新世以来地下水盐分的演化过程。结果表明：当今浅层地下水盐分的分布情况受到全新世海侵和海退事件的影响，来自古海侵的海水呈指状下渗，平均下渗速度达到23 mm/a，古海侵形成的咸水已下渗至地下−140～−160 m处。晚更新世海侵及全新世海侵事件中被捕获并储存的古海水仍然存在于含水层中且未被完全淡化，滨海地区地下水盐分运移过程仍未到达平衡。古海侵形成的地下咸水仍以较低的速率持续下渗，地下水咸化过程也在持续进行，可能会导致更深层地下水水质的进一步恶化。研究成果可为沿海地区水资源管理提供参考。
- 华北平原 /
- 地下水咸化 /
- 海侵 /
- 数值模拟
Abstract: Objective
To investigate the groundwater salinization process influenced by the combined effects of the Late Pleistocene and Holocene transgression, modern seawater intrusion, and evaporation, two shallow aquifer groups were selected as the research objects in the Cangzhou area.
Methods
Based on a series of paleo-environmental evolution data, a two-dimensional palaeo hydrogeological model was established using SEAWAT software to simulate the evolution process of groundwater salinity since the Holocene.
Results
The results suggest that the current distribution of shallow groundwater salinity is impacted by the Holocene transgression/regression. The palaeo seawater infiltrated downward in a finger-like pattern, with an average infiltration rate 23 mm/a. The brine formed by the palaeo transgressions has infiltrated to depths of −140 m to −160 m B.S.L. The palaeo seawater captured and stored during the Late Pleistocene and Holocene transgression events still remains in the aquifer and has not been completely desalinated. The salt transport process in coastal groundwater has yet to reach equilibrium. The palaeo-saltwater formed by ancient transgressions continues to seep downward at a low rate, and the groundwater salinization process is ongoing, which may lead to further deterioration of water quality in deeper aquifers.
Conclusion
The research results can provide a reference for water resources management in coastal areas.
- North China Plain /
- groundwater salinization /
- marine transgression /
- numerical simulation

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图 1 研究区地理位置(a)和采样点空间分布(b)（正交投影区（粉色矩形框内）的采样点投影于剖面A-A'）

Figure 1. Geographic location (a) and spatial distribution of sampling points (b) in the study area

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图 2 水文地质剖面(A-A')(a)和钻孔柱状图(b)（剖面图据文献[15-16]修改，柱状图据文献[17-20]修改，剖面A-A'位置见图1b）

Figure 2. Hydrogeological profile (a) and borehole histogram (b)

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图 3 古地理变化图（据文献[23]修改）

Figure 3. Paleogeography evolution

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图 4 海平面变化图^[25]

Figure 4. Sea-level change

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图 5 剖面A-B概念模型

Figure 5. Conceptual model of the profile A-B

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图 6 模型网格剖分(a)和地层结构图(b)

Figure 6. Grid section (a) and stratigraphic structure (b) of model

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图 7 水头值拟合图(a)和氯离子质量浓度拟合图(b, c)（c图中沿剖面A-A' 30 km宽的缓冲区内的采样点正交投影于剖面上得到相对空间位置）

Figure 7. Water head value fitting graph (a) and chloride ion mass concentration fitting graph (b, c)

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图 8 地下水总溶解性固体（TDS）模拟演化过程

Figure 8. Simulation evolution process of total dissolved solids in groundwater

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图 9 原始模型(a)及敏感性分析结果(b～k)

α_L. 纵向弥散度；D_m. 有效分子扩散系数；K_h. 水平渗透系数

Figure 9. Original model (a) and sensitivity analysis results (b-k)

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表 1 气候变化情况^[26]

Table 1. Climate change

年代	降水量/mm	蒸发量/mm	气候条件
早全新世（公元前5500 年之前）	480	1202	冷干向暖湿过渡
中全新世（公元前5500 年−公元前3500 年）	998	2350	暖湿
晚全新世（公元前3500 年−公元前500 年）	764	1800	温暖偏干
近现代（公元前500 年−现代）	573	1692	温凉偏干

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表 2 时间段划分及其描述

Table 2. Division and description of model time periods

时间段	描述	参考来源
公元前10000 – 公元前9000 年	地表的晚更新世海侵咸水开始下渗
公元前9000 – 公元前8000 年	模型引入降水和蒸发项	文献[26]
公元前8000 – 公元前7000 年	海平面线性升高，由−28.5 m升至−17 m	文献[25]
公元前7000 – 公元前6000 年	平均地表高程升至−13.7 m	文献[15，17]
公元前6000 – 公元前5000 年	全新世海侵到达最大界线	文献[28]
公元前5000 – 公元前4000 年	海平面低速升高，由−14 m升至−12.3 m	文献[25]
公元前4000 – 公元前3000 年	地表最大高程升至2.6 m	文献[15]
公元前3000 – 公元前2000 年	海平面升至−8 m	文献[25]
公元前2000 – 公元前1000 年	海岸线退行至现代海岸线附近	文献[28]
公元前1000 – 公元0 年	在公元前100 年前后，大运河疏浚
公元0 – 公元1000 年	气候转为温凉偏干	文献[29]
公元1000 – 公元1960 年	海岸线移动至当今海岸线位置	文献[28]
公元1960 – 公元2021 年	地下水开采，人类活动增加

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表 3 古水文地质模型主要参数

Table 3. Main parameters of the paleohydrogeological model

参数	岩土类型			参考来源
参数	砂	粉土及粉质黏土	黏土	参考来源
水平渗透系数K_h/(m·d⁻¹)	6.1	0.04	2.6×10⁻³	文献[35]
水平与垂直渗透系数比值K_h/K_v	12.5	10	10	文献[26]
储水系数S_s/m⁻¹	4.9×10⁻⁴	1.2×10⁻³	1×10⁻³	文献[36]
给水度S_y	0.06	0.05	0.04	文献[37]
孔隙度$ \theta $	0.3	0.4	0.4	文献[38]
纵向弥散度α_L/m	83	80	70
有效分子扩散系数D_m/(m²·d⁻¹)	5.1×10⁻⁵	5.1×10⁻⁵	5.1×10⁻⁵	文献[39]

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参考文献(46)

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