[en] The method and main results of a study on moisture migration in aerated zone at CIRP's Field Test Site are presented. The facility for the study consists of a tensiometer shaft down to a depth of 9.0 m and 2 neutron-probe access tubes down to a depth of 28.0 m. A set of theirs was used to monitor the moisture migration under natural condition for 2 years, and another set was used to determine unsaturated hydraulic conductivity under the after pounding and water redistribution for 7 months. Soil matrix head and water content profiles were monitored by a tensiometer system (model WM-1) and a neutron soil moisture probe (model IH_iii). The results indicate: (1) the depth essentially effected by rainfall and the depth effected by evaporation are in the upper 1.0 m; (2) the moisture migration may be divided into four zones: the layer in the upper 1.0 mm of the soil is a strong exchange zone, in which the magnitude of water content and the direction and magnitude of hydraulic head gradient vary incessantly, and the migration of liquid water is obvious; the layer in depth from 1.0 to 7.2 m is a weak exchange zone where the direction of hydraulic head gradient is downward except for the depths of more changes in grain size, in which in the depth from 1.0 to 1.6 m the changes in the water content and hydraulic head are comparatively large, and in the depth of 5.0 to 7.2 m their variations are very small, the moisture migration basically appears in a stable state and a weak thermal vapor diffusion was appeared; the layer, ranging from 7.2 to 23.0 m in depth, is a retentive zone, in which changes in soil water content with depth correspond to the variations in loess grain size except for the interface of loess-paleo-soil beds; and the layer in the depth of 23.0 to 28.0 m is capillary water zone; (3) at the depth of 0.4 to 2.4 m the conductivity ranges from 3.6 x 10^-3 to 23.4 cm/d when volumetric water contents are 0.18 to 0.41, fitting relation of unsaturated hydraulic conductivity versus water contents, this relation can be applied to the Malan Loess's upper segment for these water contents; (4) in the layer for the stable moisture migration the cumulative annual recharge calculated by an annual average means and Darcy Equation is less than 1 cm; (5) in mid-dry loess zone thermal vapor diffusion may be another way of groundwater recharge