全吸力范围非饱和土水力渗透系数的计算

翟钱; 朱益瑶; 叶为民; 杜延军; 戴国亮; 赵学亮

doi:10.11779/CJGE202204008

全吸力范围非饱和土水力渗透系数的计算 English Version

翟钱^{1, 2,},
朱益瑶^{1, 2},
叶为民³,
杜延军⁴,
戴国亮^{1, 2},
赵学亮^{1, 2}

1.
东南大学混凝土及预应力混凝土结构教育重点实验室, 东南大学桥梁研究中心, 江苏南京 210096
2.
东南大学土木工程学院, 江苏南京 210096
3.
同济大学土木工程学院, 上海 200092
4.
东南大学交通学院, 江苏南京 210096

基金项目:

国家自然科学基金项目 42030714

国家自然科学基金项目 41877248

国家自然科学基金项目 42177133

国家自然科学基金项目 51878160

国家自然科学基金项目 52078128

详细信息

作者简介:
翟钱(1982—)，男，博士，副教授，主要从事非饱和土土力学等方面的教学和科研。E-mail: 101012332@seu.edu.cn

中图分类号: TU411.4;P66;P67
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出版历程
- 收稿日期: 2021-07-04
- 网络出版日期: 2022-09-22
- 刊出日期: 2022-03-31

Estimation of hydraulic conductivity of unsaturated soils under entire suction range

ZHAI Qian^{1, 2,},
ZHU Yi-yao^{1, 2},
YE Wei-min³,
DU Yan-jun⁴,
DAI Guo-liang^{1, 2},
ZHAO Xue-liang^{1, 2}

1.
Key Laboratory of Concrete and Prestressed Concrete Structure of Ministry of Education, Southeast University, Bridge Engineering Research Center of Southeast University, Nanjing 210096, China
2.
School of Civil Engineering, Southeast University, Nanjing 210096, China
3.
School of Civil Engineering, Tongji University, Shanghai 200092, China
4.
Southeast University, Nanjing 210096, China

摘要

摘要: 非饱和土水力渗透系数决定了水分在非饱和土体中迁移的速率，因此非饱和土水力渗透系数是研究水分在非饱和土中迁移规律的关键参数。一般情况，渗流数值计算软件将水力渗透系数方程作为输入参数，水力渗透系数方程的准确性直接影响渗流模拟结果的可靠性。常用的非饱和土水力渗透系数方程大多基于毛细水的相关理论，在低吸力区其计算结果与试验数据吻合度较高，但在高吸力区计算结果与试验数据差异显著。将全吸力范围分为毛细水渗流主导区、膜态水渗流主导区、气态水渗流主导区，并分析了不同形态的水分在非饱和土体中迁移规律的控制机理。全吸力范围的非饱和土水力渗透系数定义为表观渗透系数，其包含毛细水渗透系数、膜态水渗透系数和气态水渗透系数。通过剖析毛细水、薄膜水以及水蒸气在非饱和土体中迁移机理，推导不同形态水分渗透系数的数学表达，最终得出全吸力范围非饱和土的水力渗透系数计算方程。
- 孔径分布 /
- 渗流函数 /
- 毛细水渗流 /
- 膜态水渗流 /
- 气态水渗流
Abstract: The hydraulic conductivity of unsaturated soils controls their water flow. Most numerical softwares adopt the hydraulic conductivity function (HCF) as the input parameter to simulate the water flow in unsaturated soils. The accuracy of the inputted HCF has significant effect on the reliability of the simulated results from the seepage analysis. It is noted that most HCFs are proposed based on the theory of capillary flow. It is observed that in the high suction range, the estimated HCF of unsaturated soils from the capillary flow is much lower than what is obtained from the experimental measurement. In this study, the water flows in unsaturated soils are categorized into three forms, including (i) capillary flow, (ii) film flow and (iii) vapour flow. The mathematical models for the HCF of soils corresponding to those three forms of water flow are proposed. Consequently, the total HCF of unsaturated soils under the entire suction range is proposed.
- pore-size distribution /
- hydraulic conductivity function /
- capillary flow /
- film flow /
- vapour flow

HTML全文

图 1 土体中不同形态水分^{[23, 25]}

Figure 1. Different forms of water in soils^{[23, 25]}

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图 2 阀门模型

Figure 2. Illustration of valve model

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图 3 不同孔径联通产生的有效面积

Figure 3. Illustration of effective area

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图 4 允许水流通过的有效面积的计算

Figure 4. Computation of effective area allowing water to pass through

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图 5 毛细渗透系数计算结果

Figure 5. Computation of capillary conductivity

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图 6 砂质黏土和粉质砂土的土水特征曲线和非饱和渗透系数

Figure 6. Illustration of SWCCs and unsaturated hydraulic conductivities of low-plasticity clay and silty sand

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图 7 不同粒径颗粒连接造成膜态水的不同渗流路径。

Figure 7. Illustration of seepage paths for film water due to different connecting paths between soil particles with different radii

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图 8 综合毛细渗流和膜态水渗流计算非饱和土渗透系数

Figure 8. Computation of hydraulic conductivities of unsaturated soils by considering both capillary flow and film flow

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图 9 非饱和高庙子高岭土在不同温度下渗透系数

Figure 9. Illustration of hydraulic conductivities of unsaturated GMZ bentonite under different temperatures.

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图 10 允许气体通过的有效面积计算

Figure 10. Computation of effective area allowing air to pass through

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图 11 气态水渗流渗透系数的计算

Figure 11. Computation of the hydraulic conductivity of soil due to vapour flow

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图 12 非饱和土体中不同形态水分渗流主导区域

Figure 12. Illustration of different dominated zones in hydraulic conductivity function of unsaturated soils

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表 1 不同学者对αβ建议值

Table 1 Suggested values of αβ by various scholars

参考文献 αβ

Penman^[46] 0.66n

Marshall^[47] β^3/2

Millington ^[48] β^4/3

Millington等^[49] β^10/3/n²

Lai等^[50] β^5/3

Abu-EI-Sha'r等^[51] 0.435n

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