摘要
为研究多层土边坡内入渗雨水方向演变规律建立均质和多层土质边坡模型依据VG模型的多土层边坡含水率与基质吸力的控制方程结合饱和区成形研究了入渗雨水方向的时空演变特征及影响因素以及水流方向与有效应力的联系.分析表明:水平方向的基质吸力差决定了水流方向基质吸力沿水平方向的变化率决定了水流水平方向增速饱和区成形是垂直流产生的必要条件降雨停止坡面浅层 0 ~1.3m 内迅速产生下坡向水流深层下坡向水流产生滞后渗透性差异大的土层交界面上极易产生剧烈的水平渗流上坡向水流的产生伴随着有效应力降低.
In order to study the law of water flow migration in multi-layer soil slope, the homogeneous soil slope model and the multi-layer soil slope model were established. The temporal and spatial characteristics and influencing factors of water flow migration were explored, with the development of saturated-zone taken into account, based on the governing equation of moisture content and matrix suction in multi-layer soil slope derived from the VG model. The relationship between water flow migration and effective stress was also studied. It is found that the difference in the matrix suction in the horizontal direction decides the change of water flow migration mode and the rate of change of matrix suction along the horizontal direction determines the rate increment of water flow horizontal direction. The formation of the saturated-zone is a necessary condition for forming the vertical water flow. After the rainfall stops, the down-slope water flow is rapidly generated only in the shallow layer of 0~1.3 m, with the forming of down-slope water flow in deep area lagging behind. The horizontal water flow at the interface of two layers of soil with large differences in permeability changes sharply, and the forming of up-slope water flow is always accompanied with the decrease of effective stress.
作者
王述红
何坚
刘欢
WANG Shu-hong;HE Jian;LIU Huan(School of Resources & Civil Engineering, Northeastern University, Shenyang 110819, China)
出处
《东北大学学报（自然科学版）》
EI
CAS
CSCD
北大核心
2019年第8期1172-1177,1204,共7页
Journal of Northeastern University(Natural Science)
基金
国家自然科学基金资助项目(U1602232,51474050)
中央高校基本科研业务费专项资金资助项目(N170108029)
辽宁省自然科学基金资助项目(20170540304,20170520341)
东北大学“双一流”建设项目(2018)
关键词
降雨入渗
非饱和土
水流运移
基质吸力
多土层边坡
rainfall infiltration
unsaturated soil
water migration
matrix suction
multi-layer soil slope
