高温作用下非饱和黄土水热迁移试验研究

赵再昆; 王铁行; 金鑫; 张亮

doi:10.11779/CJGE20221067

高温作用下非饱和黄土水热迁移试验研究 English Version

1.
西安建筑科技大学土木工程学院, 陕西西安 710055
2.
西安工业大学建筑工程学院, 陕西西安 710021

基金项目:

陕西省自然科学基础研究重点项目 2020ZJ-49

陕西省自然科学基础研究计划项目 2021JQ-644

陕西省教育厅科研计划项目 21JK0672

详细信息

作者简介:
赵再昆(1995—)，男，博士研究生，主要从事黄土、冻土工程方面的研究工作。E-mail：zhaozaikun@xauat.edu.cn

中图分类号: TU444
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出版历程
- 收稿日期: 2022-08-28
- 网络出版日期: 2024-01-08
- 刊出日期: 2023-12-31

Experimental study on water and heat migration of unsaturated loess under high temperatures

1.
College of Civil Engineering, Xi'an University of Architecture and Technology, Xi'an 710055, China
2.
School of Civil and Architecture Engineering, Xi'an Technological University, Xi'an 710021, China

摘要

摘要: 黄土的水敏性特点使其强度随含水率降低而大幅增加，高温疏干方法进行黄土加固具有广阔应用前景，研究高温作用下非饱和土水热迁移规律具有重要意义。通过自制高温水热迁移装置，进行不同高温水平下不同初始含水率黄土的水热迁移试验。试验结果表明：高温对水分具有显著驱动作用；当热端温度超过100℃时，试验初期贴近热源土体的水分被快速驱离，是气液相变导致的气态水迁移显著增加所致；含水率分布由峰值曲线逐渐演变为含水率单向增大的缓变曲线；热源温度越高，水分迁移通量越大。建立了高温水热迁移模型，并通过计算验证了模型的可靠性。以体积含水量表示计算所得水分场数据分析了高温和水分含量对水分迁移的综合影响机制，根据黄土高温水分迁移特征在不同体积含水量阶段的差异化表现，将高温水分迁移特征划分为3个区间。Ⅰ低体积含水量区间：水分迁移通量随体积含水量变化曲线呈现峰值曲线，水分主要迁移形式为气态水；Ⅱ中体积含水量区间：随体积含水量增大，气态水迁移通量减小的同时液态水迁移通量增大；Ⅲ高体积含水量区间：温度作用对水分迁移进程不产生影响。
- 高温 /
- 非饱和黄土 /
- 含水率 /
- 水热迁移
Abstract: The strength of loess increases greatly with the decrease of water content. The high-temperature drainage method has broad application prospects for loess reinforcement, so it is significant to study the water and heat transfer of unsaturated soils under high temperatures. A water and heat transfer device allowing the action of high temperatures is developed to test the water and temperature fields of loess with specific initial water content under the action of a high-temperature heat source. The test results show that the high temperature has a significant driving effect on water compared with the normal temperature heat source. When the hot-end temperature exceeds 100℃, the water of soils close to the hot source is rapidly driven away at the beginning of the tests, which is caused by the significant increase of gaseous water migration due to the gas-liquid phase change. The distribution curves of water content gradually evolve from a peak type to a unidirectional increase one of the water content. Water migration fluxes significantly increase with heating source temperature. A high-temperature water and heat transfer model is established, and its accuracy is verified through the trial calculation. The comprehensive influence mechanism of high temperature and water content on water migration is analyzed based on the calculated results. The high-temperature water migration characteristics are divided into three intervals: Ⅰ(low water content interval), the water migration flux curve with water content shows a peak curve, and water migrates mainly in gaseous form. Ⅱ (medium water content interval), as the water content increases, the migration flux of gaseous water decreases while the migration flux of liquid water increases. Ⅲ (high water content interval), the temperature has a rare effect on the water migration. The findings may provide preliminary revelation on the water and heat migration characteristics of high-temperature unsaturated soils.
- high temperature /
- unsaturated loess /
- water content /
- water and heat migration

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图 1 高温水热迁移装置

Figure 1. Schematic diagram of high-temperature resistant water migration devices

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${T_{\text{h}}}$ =110℃作用下 ${w_{\text{i}}}$ =19%试样的温度场随时间变化

Curves of temperature field with time at ${T_{\text{h}}}$ =110℃ and ${w_{\text{i}}}$ =19%

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${w_{\text{i}}}$ =19%的试样在不同 ${T_{\text{h}}}$ 作用24 h后的温度场

Curves of temperature field with ${T_{\text{h}}}$ at $t$ =24 h and ${w_{\text{i}}}$ =19%

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${T_{\text{h}}}$ =110 ℃作用不同时间 $t$ 时 ${w_{\text{i}}}$ =19%试样的水分场

Water fields of sample with ${w_{\text{i}}}$ =19% at ${T_{\text{h}}}$ =110℃ for different time $t$

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${w_{\text{i}}}$ =19%的试样在不同热源 ${T_{\text{h}}}$ 作用 $t$ =24 h后的水分场

Curves of water field with ${T_{\text{h}}}$ at $t$ =24 h, ${w_{\text{i}}}$ =19%

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${w_{\text{i}}}$ =16%，19%和22%的试样经不同热源 ${T_{\text{h}}}$ 作用 $t$ =14 d后的水分场

Curves of water field with ${T_{\text{h}}}$ and ${w_{\text{i}}}$ at $t$ =14 d

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14 d后不同 ${w_{\text{i}}}$ 试样的水分通量 ${\bar q_m}$ 与热源 ${T_{\text{h}}}$ 的关系

Relationship between mean water flux ${\bar q_m}$ and ${T_{\text{h}}}$ after 14 days at different ${w_{\text{i}}}$

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图 8 高温热源作用14 d后水分场的计算值与实测值

Figure 8. Calculated and measured water fields after 14 days of high-temperature heat source

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图 9 不同高温水平下水分迁移通量与体积含水量的关系(Ⅰ低体积含水量阶段、Ⅱ中体积含水量阶段、Ⅲ高体积含水量阶段）

Figure 9. Variation of vapor and liquid diffusivity with water content and temperature (Ⅰ: low water content stage, Ⅱ: medium water content stage, and Ⅲ: high water content stage)

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表 1 试验材料物理指标

Table 1 Physical parameters of test material

试样孔隙比 $n$	试样干密度 ${\rho _{\text{d}}}$ /(g·cm^-3)	塑限w_P/%	液限w_L/%	塑性指数I_P	土颗粒密度r_s/(g·cm^-3)	含量/%
试样孔隙比 $n$	试样干密度 ${\rho _{\text{d}}}$ /(g·cm^-3)	塑限w_P/%	液限w_L/%	塑性指数I_P	土颗粒密度r_s/(g·cm^-3)	黏粒(＜5 μm)	粉粒(5~50 μm)	砂粒(＞50 μm)
0.936	1.4	19.1	31.6	12.5	2.71	22	66	12

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表 2 考虑高温影响的气、液态水运移参数表达式

Table 2 Transport parameters and change rates of vapor and liquid water at different temperatures

参数	表达式	来源
$\eta$	$\eta = 9.5 + 3 \cdot \theta /{\theta _{{\text{sat}}}} - 8.5 \cdot \exp \left\{ { - {{\left[ {(1 + 2.6/\sqrt {{f_{\text{c}}}} )\theta /{\theta _{{\text{sat}}}}} \right]}^4}} \right\}$	Saito等^[27]
$\gamma$ / ${\text{(N}} \cdot {{\text{m}}^{ - 1}})$	$\gamma = - 16.14 \times {10^{ - 5}}{T^2} - 0.16T + 76.16, {\text{ }}{R^2}{\text{ = 0}}{\text{.958}}$	根据数据文献[31]拟合
${\mu _w}$ / ${{({\rm{ \mathsf{ μ}}} {\rm{Pa}}}} \cdot {{\text{s}}^{ - {\text{1}}}}{\text{)}}$	${\mu _{\text{w}}} = {\mu _{{\text{w0}}}}\exp [{\mu _1}/(R \cdot ({\text{T}} - 139.85))]$	Philip等^[28]
${\rho _{\text{v}{\text{s}}}}$ / ${\text{(kg}} \cdot {{\text{m}}^{ - 3}})$	${\rho }_{\mathrm{vs}}={10}^{-3}{T}^{-1}\mathrm{exp}(31.3716-6014.79{T}^{-1}-7.92495\times {10}^{-3}T), \;\text{0}^ \circ {\rm{C}}<\text{T}\le \text{120}^ \circ {\rm{C}}$ $\begin{array}{l}{\rho }_{\text{vs}}=1.3069\times {10}^{-7}\times {T}^{-1}\mathrm{exp}(25.66651-3429.31154\times \\ {T}^{-1}+7.06\times {10}^{-3}T), \text{ }{R}^{2}=0.968, \text{120}^ \circ {\rm{C}}<\text{T}\le \text{ 300}^ \circ {\rm{C}}\text{ }\end{array}$	Saito等^[27]根据数据文献[31]拟合
${D_{\text{e}}}$ / ${\text{(}}{{\text{m}}^2} \cdot {{\text{s}}^{ - {\text{1}}}})$	${D_{\text{e}}} = (\theta _{\text{v}}^{{\text{7/3}}}/\theta _{{\text{sat}}}^{\text{2}})\theta _{\text{v}}^{} \cdot 2.12 \times {10^{ - 5}}{(T/273.15)^2}$	Milly等^[29]
注：T在参数 $\gamma$ 中为摄氏温度（℃），在 ${\mu _{\text{w}}}$ ， ${\rho _{{\text{vs}}}}$ ，D_e参数中为绝对温度（K）； ${f_{\text{c}}}$ 为土中黏粒的质量分数； ${\mu _{{\text{w0}}}}$ 为水分在25℃时的黏滞系数；R为摩尔气体常数。

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