# Experimental Study on Permeability Anisotropy of Unsaturated Compacted Loess

Authors: Yan Zhou Hao; Lei Cheng; Wen Fang Xiao
Journal: Advances in Civil Engineering
 (2022)

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## Abstract

This study investigates the permeability characteristics of unsaturated compacted loess by focusing on the anisotropy parallel and perpendicular to the compaction. Three tests are conducted on compacted loess: permeability test, soil-water characteristic curve test, and scanning electron microscope (SEM) test. Samples are maintained and tested at different dry densities under optimal moisture conditions. Test results showed that the horizontal saturated permeability coefficient of compacted loess was larger than in the vertical direction, showing obvious anisotropy. Based on the saturated permeability coefficient, the permeability coefficient of unsaturated compacted loess can be predicted according to the soil-water characteristic curve fitted using the van Genuchten model combined with the Childs and Collis-Geroge model. The relational formula was established between the unsaturated permeability anisotropy ratio and the matrix suction through introducing a pore connectivity-tortuosity parameter, which represents the relationship between unsaturated permeability anisotropy ratio and matrix suction. The difference of pore characteristics between horizontal and vertical directions of compacted loess is the main reason for the permeability anisotropy.


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## Body

## 1. Introduction

The gully is a unique landform common to loess areas that limits city development and expansion. Some cities in China, including Yan’an, Lanzhou, and others, have begun large-scale hill-cutting, gully filling, and artificial land-building engineering in order to facilitate city expansion. In addition, highway, railway, and airport construction in loess areas requires filling to make up for the shortage of construction land. Undisturbed loess commonly has a macroporous structure and is undercompacted and collapsible, which has adverse consequences for foundation construction. Compaction is the primary method employed to improve the mechanical properties of compacted loess and prepare loess-filled construction sites. Permeability is an important property of loess. Water infiltration weakens compacted loess; therefore, examining the permeability of compacted loess is of great significance to large-scale filling foundations, roadbeds, and slopes in loess areas.Soil permeability under an in situ stress state can reflect water seepage in soil. There are more scholars who have performed a lot of research on loess. Li [1] studied the relationship between permeability and porosity in loess. The permeability coefficient is affected by dry density [2, 3], dry-wet cycle [4, 5], freeze-thaw cycles [6], confining pressure [4], structure [7, 8], and osmotic pressure [9]. The permeability coefficient function of remolded unsaturated loess was established under varying humidity and density [10].Research on unsaturated soil permeability has yielded fruitful results. The seepage theory of unsaturated soils has been widely recognized in the field of geotechnical engineering [11]. Unsaturated soil permeability coefficient is an important parameter for studying water migration and distribution in soils. Methods for determining the permeability coefficient of unsaturated soils include the steady-state method [12] and the transient method [13, 14]. Because of the complexity and time-consuming nature of testing the permeability coefficient of unsaturated soils, the soil-water characteristic curve was commonly used to indirectly determine k(θ) [11, 15]. Some scholars used a linear model [16], van Genuchten-Mualem model [17], two-parameter power function model [18], empirical formula [19, 20], unsaturated hydraulic conductivity measurement system [9, 21], gaseous and liquid water migration model [22], or fractal geometry model [23] to study variations in permeability coefficient with matrix suction, saturation, volumetric water content, and effective saturation.Research on permeability anisotropy primarily focused on clay, which focused on causes of permeability anisotropy [24], influencing factors [25], and permeability anisotropy models [26]. The permeability anisotropy ratio of clay increased with decreasing void ratio. With increasing consolidation stress, clay microparticles tend to be horizontal and permeability anisotropy increases [4, 27]. Research on the permeability anisotropy of compacted loess, especially unsaturated compacted loess, is quite limited literature.Examining the permeability anisotropy of compacted loess under the condition of water infiltration will have significant impacts on the distribution of water in filling foundations, embankments, filling slopes, water pipelines, and other engineering projects. This study describes an experimental study in which loess specimens with different dry densities are collected from different vertical and parallel compaction planes. Then, the saturated permeability coefficientksv in the direction of vertical compaction surface and ksh in the direction of parallel compaction surface are determined using saturated permeability tests. The unsaturated permeability coefficients are calculated using the soil-water characteristic curves of unsaturated compacted loess with different dry densities. The equation between the unsaturated permeability anisotropy ratio and matrix suction is established by introducing the pore connectivity-tortuosity parameter. The microstructural characteristics of compacted loess were analyzed using scanning electron microscope (SEM) images to reveal the micromechanisms of permeability anisotropy of compacted loess in vertical and horizontal directions.


## 2. Test Scheme

### 2.1. Samples

Soil samples used in this study wereQ3 Malan loess collected from a foundation pit in Xi’an, China. Malan loess is yellowish brown, relatively weak, and wet. The physical properties of loess samples were determined following the Chinese National Standards (SAC 2019), which are shown in Table 1.Table 1
Main indicator of the physical properties of loess.
Relative densityGSLiquid limitWL (%)Plastic limitWP (%)Plasticity indexIpParticle composition (%)>0.075 mm0.075–0.01 mm0.01–0.005 mm<0.005 mm2.7230.818.612.23.7252.1815.4428.66According to laboratory compaction tests following the Chinese National Standards [28], the optimal soil sample moisture content was 18.9%, and the maximum dry density was 1.73 g/cm3. Soil samples from the soil layer were naturally air-dried and then pulverized using a rubber hammer, which only separated the cemented particles but did not damage the loess particles. The pulverized loess was sieved through a 2 mm mesh in order to prepare soil samples with a water content of 18.9%, which were sealed with plastic film for more than 48 hours to produce the desired water distribution and ensure the water content remains unchanged (Table 1). Samples were prepared using a specifically designed sample press. Wet soil was weighed based on the dry density and moisture content and was vertically compacted into five layers. Samples were 150 mm in diameter and 112 mm tall (Figure 1). The dry densities were 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3. The error was controlled to be ≤0.02 g/cm3.Figure 1
Samples of compacted loess and sampling direction.Soil samples were collected in the direction of vertical compaction surface (vertical samples) and parallel compaction surface (horizontal samples) (Figure1). The permeability test samples were cut out using a soil cutting plate, and the samples were 39.1 mm in diameter and 80 mm high (Figure 1). Next, four vertical and four horizontal samples were put into a vacuum saturation device for saturation treatment until the saturation was greater than 95%. Samples for the soil-water characteristic test were cut out of the compacted loess using a cutting ring with an inner diameter of 70 mm and a height of 19 mm. The dry densities of the four samples were 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3, respectively. Next, samples were put into a humidifying cylinder for sealing and moisturization. The samples for the scanning electron microscope (SEM) test were cut into 5 mm × 5 mm x 10 mm blocks with dry densities of 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3. Four vertical and horizontal samples were used in the scanning electron microscope test.


### 2.2. Testing Techniques

#### 2.2.1. Permeability Test and Result Analysis

The permeability test for saturated compacted loess used a SLB-1 triaxial permeameter apparatus (Figure2). Samples were saturated using vacuum pumping and then put into the sample chamber to test the saturated permeability coefficient ks of the compacted loess samples with different dry densities. The test results of saturated permeability coefficients in vertical directions (ksv) and horizontal direction (ksh) are shown in Table 2.Figure 2
SLB-1 triaxial permeameter apparatus.Table 2
Permeability coefficient of saturated compacted loess.
ρd  = 1.40 g/cm3ρd  = 1.50 g/cm3ρd  = 1.60 g/cm3ρd  = 1.70 g/cm3ksv/10−6cm/sksh/10−6cm/sksv/10−6cm/sksh/10−6cm/sksv/10−6cm/sksh/10−6cm/sksv/10−6cm/sksh/10−6cm/s87.769109.03024.2135.8489.62516.0833.2056.251The vertical and horizontal permeability coefficients of saturated compacted loess significantly decreased with the increase in dry density. That was because the dry density was smaller, the soil was dominated by macropores, the pore connectivity was better, and the permeability coefficient of saturated compacted loess was greater. On the contrary, the dry density was larger, the soil was dominated by micropores, the pore connectivity was poor, and the permeability coefficient of compacted loess was smaller (Table2). The horizontal saturated permeability coefficient of compacted loess was larger than in the vertical direction, showing obvious anisotropy. Flake and needle particles were rotated to be parallel with the compaction surface after vertical compaction. The directionality of the particles, such as flake and needle, weakened the porosity and connectivity of the pores perpendicular to the compaction surface. On the contrary, the porosity and connectivity of pores parallel to the compaction surface were improved. In addition, there are flaky clay minerals in the compacted loess. During the compaction process, the flaky clay minerals continuously rotate and finally parallel to the compacted surface. The increasing area of clay mineral particles blocked the connectivity of vertical pores, which ultimately led to a reduction in the vertical permeability coefficient [4].


#### 2.2.2. Soil-Water Characteristic Curve Test

The soil-water characteristic curve test on unsaturated compacted loess used a soil-water characteristic curve pressure plate apparatus (Figure3) and a high air entry ceramic plate (5 Bar). The high air entry ceramic plate has small pores of relatively uniform size. The plate acted as a membrane between air and water (Figure 4). Once the plate was saturated with water, air could not pass through the plate due to the ability of the contractile skin to resist airflow. The ability of the ceramic plate to withstand the airflow resulted from the surface tension of water, Ts, which acted like a thin membrane plugging the small pores of radius, Rs, on the surface of the ceramic plate. The difference between the air pressure above the contractile skin and the water pressure below the contractile skin was defined as matric suction. The maximum matric suction maintained across the surface of the plate is the air entry value, ug−uwd [11]. Each sample was tested at air pressures of 10 kPa, 20 kPa, 40 kPa, 80 kPa, 100 kPa, 140 kPa, and 180 kPa. Samples were saturated using vacuum with water. Then, the sample was put into the soil sample chamber, and air pressure was applied to the soil sample to measure the amount of water discharged from the sample. Measurements were recorded every 24 h for each air pressure level.Figure 3
Soil-water characteristic curve pressure plate apparatus.Figure 4
Operating principle of a high air entry plate as described by Kelvin’s capillary model [11].


#### 2.2.3. SEM Test

The samples for the scanning electron microscope (SEM) test were cut along the direction of vertical compaction surface and horizontal compaction surface for 5 mm in length, 5 mm in width, and 10 mm in height with the dry densities of 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3 (Figure 5). The samples were broken to be 5 mm in height and form a relatively flat and fresh section. The loose particles were blown off the surface. The surface was coated with a metal film. Then, the sample was put into the SEM to take 500-fold magnification SEM images.Figure 5
Samples of the scanning electron microscope test.


## 2.1. Samples

Soil samples used in this study wereQ3 Malan loess collected from a foundation pit in Xi’an, China. Malan loess is yellowish brown, relatively weak, and wet. The physical properties of loess samples were determined following the Chinese National Standards (SAC 2019), which are shown in Table 1.Table 1
Main indicator of the physical properties of loess.
Relative densityGSLiquid limitWL (%)Plastic limitWP (%)Plasticity indexIpParticle composition (%)>0.075 mm0.075–0.01 mm0.01–0.005 mm<0.005 mm2.7230.818.612.23.7252.1815.4428.66According to laboratory compaction tests following the Chinese National Standards [28], the optimal soil sample moisture content was 18.9%, and the maximum dry density was 1.73 g/cm3. Soil samples from the soil layer were naturally air-dried and then pulverized using a rubber hammer, which only separated the cemented particles but did not damage the loess particles. The pulverized loess was sieved through a 2 mm mesh in order to prepare soil samples with a water content of 18.9%, which were sealed with plastic film for more than 48 hours to produce the desired water distribution and ensure the water content remains unchanged (Table 1). Samples were prepared using a specifically designed sample press. Wet soil was weighed based on the dry density and moisture content and was vertically compacted into five layers. Samples were 150 mm in diameter and 112 mm tall (Figure 1). The dry densities were 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3. The error was controlled to be ≤0.02 g/cm3.Figure 1
Samples of compacted loess and sampling direction.Soil samples were collected in the direction of vertical compaction surface (vertical samples) and parallel compaction surface (horizontal samples) (Figure1). The permeability test samples were cut out using a soil cutting plate, and the samples were 39.1 mm in diameter and 80 mm high (Figure 1). Next, four vertical and four horizontal samples were put into a vacuum saturation device for saturation treatment until the saturation was greater than 95%. Samples for the soil-water characteristic test were cut out of the compacted loess using a cutting ring with an inner diameter of 70 mm and a height of 19 mm. The dry densities of the four samples were 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3, respectively. Next, samples were put into a humidifying cylinder for sealing and moisturization. The samples for the scanning electron microscope (SEM) test were cut into 5 mm × 5 mm x 10 mm blocks with dry densities of 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3. Four vertical and horizontal samples were used in the scanning electron microscope test.


## 2.2. Testing Techniques

### 2.2.1. Permeability Test and Result Analysis

The permeability test for saturated compacted loess used a SLB-1 triaxial permeameter apparatus (Figure2). Samples were saturated using vacuum pumping and then put into the sample chamber to test the saturated permeability coefficient ks of the compacted loess samples with different dry densities. The test results of saturated permeability coefficients in vertical directions (ksv) and horizontal direction (ksh) are shown in Table 2.Figure 2
SLB-1 triaxial permeameter apparatus.Table 2
Permeability coefficient of saturated compacted loess.
ρd  = 1.40 g/cm3ρd  = 1.50 g/cm3ρd  = 1.60 g/cm3ρd  = 1.70 g/cm3ksv/10−6cm/sksh/10−6cm/sksv/10−6cm/sksh/10−6cm/sksv/10−6cm/sksh/10−6cm/sksv/10−6cm/sksh/10−6cm/s87.769109.03024.2135.8489.62516.0833.2056.251The vertical and horizontal permeability coefficients of saturated compacted loess significantly decreased with the increase in dry density. That was because the dry density was smaller, the soil was dominated by macropores, the pore connectivity was better, and the permeability coefficient of saturated compacted loess was greater. On the contrary, the dry density was larger, the soil was dominated by micropores, the pore connectivity was poor, and the permeability coefficient of compacted loess was smaller (Table2). The horizontal saturated permeability coefficient of compacted loess was larger than in the vertical direction, showing obvious anisotropy. Flake and needle particles were rotated to be parallel with the compaction surface after vertical compaction. The directionality of the particles, such as flake and needle, weakened the porosity and connectivity of the pores perpendicular to the compaction surface. On the contrary, the porosity and connectivity of pores parallel to the compaction surface were improved. In addition, there are flaky clay minerals in the compacted loess. During the compaction process, the flaky clay minerals continuously rotate and finally parallel to the compacted surface. The increasing area of clay mineral particles blocked the connectivity of vertical pores, which ultimately led to a reduction in the vertical permeability coefficient [4].


### 2.2.2. Soil-Water Characteristic Curve Test

The soil-water characteristic curve test on unsaturated compacted loess used a soil-water characteristic curve pressure plate apparatus (Figure3) and a high air entry ceramic plate (5 Bar). The high air entry ceramic plate has small pores of relatively uniform size. The plate acted as a membrane between air and water (Figure 4). Once the plate was saturated with water, air could not pass through the plate due to the ability of the contractile skin to resist airflow. The ability of the ceramic plate to withstand the airflow resulted from the surface tension of water, Ts, which acted like a thin membrane plugging the small pores of radius, Rs, on the surface of the ceramic plate. The difference between the air pressure above the contractile skin and the water pressure below the contractile skin was defined as matric suction. The maximum matric suction maintained across the surface of the plate is the air entry value, ug−uwd [11]. Each sample was tested at air pressures of 10 kPa, 20 kPa, 40 kPa, 80 kPa, 100 kPa, 140 kPa, and 180 kPa. Samples were saturated using vacuum with water. Then, the sample was put into the soil sample chamber, and air pressure was applied to the soil sample to measure the amount of water discharged from the sample. Measurements were recorded every 24 h for each air pressure level.Figure 3
Soil-water characteristic curve pressure plate apparatus.Figure 4
Operating principle of a high air entry plate as described by Kelvin’s capillary model [11].


### 2.2.3. SEM Test

The samples for the scanning electron microscope (SEM) test were cut along the direction of vertical compaction surface and horizontal compaction surface for 5 mm in length, 5 mm in width, and 10 mm in height with the dry densities of 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3 (Figure 5). The samples were broken to be 5 mm in height and form a relatively flat and fresh section. The loose particles were blown off the surface. The surface was coated with a metal film. Then, the sample was put into the SEM to take 500-fold magnification SEM images.Figure 5
Samples of the scanning electron microscope test.


## 2.2.1. Permeability Test and Result Analysis

The permeability test for saturated compacted loess used a SLB-1 triaxial permeameter apparatus (Figure2). Samples were saturated using vacuum pumping and then put into the sample chamber to test the saturated permeability coefficient ks of the compacted loess samples with different dry densities. The test results of saturated permeability coefficients in vertical directions (ksv) and horizontal direction (ksh) are shown in Table 2.Figure 2
SLB-1 triaxial permeameter apparatus.Table 2
Permeability coefficient of saturated compacted loess.
ρd  = 1.40 g/cm3ρd  = 1.50 g/cm3ρd  = 1.60 g/cm3ρd  = 1.70 g/cm3ksv/10−6cm/sksh/10−6cm/sksv/10−6cm/sksh/10−6cm/sksv/10−6cm/sksh/10−6cm/sksv/10−6cm/sksh/10−6cm/s87.769109.03024.2135.8489.62516.0833.2056.251The vertical and horizontal permeability coefficients of saturated compacted loess significantly decreased with the increase in dry density. That was because the dry density was smaller, the soil was dominated by macropores, the pore connectivity was better, and the permeability coefficient of saturated compacted loess was greater. On the contrary, the dry density was larger, the soil was dominated by micropores, the pore connectivity was poor, and the permeability coefficient of compacted loess was smaller (Table2). The horizontal saturated permeability coefficient of compacted loess was larger than in the vertical direction, showing obvious anisotropy. Flake and needle particles were rotated to be parallel with the compaction surface after vertical compaction. The directionality of the particles, such as flake and needle, weakened the porosity and connectivity of the pores perpendicular to the compaction surface. On the contrary, the porosity and connectivity of pores parallel to the compaction surface were improved. In addition, there are flaky clay minerals in the compacted loess. During the compaction process, the flaky clay minerals continuously rotate and finally parallel to the compacted surface. The increasing area of clay mineral particles blocked the connectivity of vertical pores, which ultimately led to a reduction in the vertical permeability coefficient [4].


## 2.2.2. Soil-Water Characteristic Curve Test

The soil-water characteristic curve test on unsaturated compacted loess used a soil-water characteristic curve pressure plate apparatus (Figure3) and a high air entry ceramic plate (5 Bar). The high air entry ceramic plate has small pores of relatively uniform size. The plate acted as a membrane between air and water (Figure 4). Once the plate was saturated with water, air could not pass through the plate due to the ability of the contractile skin to resist airflow. The ability of the ceramic plate to withstand the airflow resulted from the surface tension of water, Ts, which acted like a thin membrane plugging the small pores of radius, Rs, on the surface of the ceramic plate. The difference between the air pressure above the contractile skin and the water pressure below the contractile skin was defined as matric suction. The maximum matric suction maintained across the surface of the plate is the air entry value, ug−uwd [11]. Each sample was tested at air pressures of 10 kPa, 20 kPa, 40 kPa, 80 kPa, 100 kPa, 140 kPa, and 180 kPa. Samples were saturated using vacuum with water. Then, the sample was put into the soil sample chamber, and air pressure was applied to the soil sample to measure the amount of water discharged from the sample. Measurements were recorded every 24 h for each air pressure level.Figure 3
Soil-water characteristic curve pressure plate apparatus.Figure 4
Operating principle of a high air entry plate as described by Kelvin’s capillary model [11].


## 2.2.3. SEM Test

The samples for the scanning electron microscope (SEM) test were cut along the direction of vertical compaction surface and horizontal compaction surface for 5 mm in length, 5 mm in width, and 10 mm in height with the dry densities of 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3 (Figure 5). The samples were broken to be 5 mm in height and form a relatively flat and fresh section. The loose particles were blown off the surface. The surface was coated with a metal film. Then, the sample was put into the SEM to take 500-fold magnification SEM images.Figure 5
Samples of the scanning electron microscope test.


## 3. Permeability of Unsaturated Compacted Loess

Water migration in unsaturated soils is significantly different from that in saturated soils. Water migration in unsaturated soils is primarily driven by matrix potential and gravity potential. Water migrates in liquid or gas and is affected by temperature, solute, and other complex conditions, making it difficult to accurately measure the permeability coefficient of unsaturated soil using a direct test. Permeability coefficients of saturated soils and soil-water characteristic curves of unsaturated soils are commonly used to indirectly determine permeability coefficients of unsaturated soils [29].


### 3.1. Soil-Water Characteristic Curve Test Results

The volumetric water content and matrix suction of compacted loess with dry densities of 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3 are shown in Table 3. With an increase in matrix suction, the volumetric water content of soil samples gradually decreased. When the soil dry density was high, the decrease in volumetric water content was smaller for the same change in matrix suction. On the contrary, when the dry density of soil was low, the decrease in volumetric water content was large for the same change in matrix suction (Table 3).Table 3
Soil-water characteristic curve test values for compacted loess.
Matric suctionψ/kPaVolumetric water contentθ/%ρd = 1.40 g/cm3ρd = 1.50 g/cm3ρd = 1.60 g/cm3ρd = 1.70 g/cm3046.7643.6540.4837.401039.3237.5035.1933.922033.2132.1831.8730.764026.0526.4526.3425.946022.1022.4323.1823.428020.2420.9121.3622.1010019.1319.8620.3021.3614017.7718.0918.8119.8718016.9617.2717.8918.79


### 3.2. Determiningk(θ) Using the Van Genuchten Soil-Water Characteristic Curve Model

Due to data complexity, data discreteness, and the time-consuming soil-water characteristic curve test, the test data represent only a part of the soil-water characteristic curve. In order to obtain a complete soil-water characteristic curve, measured matrix suction and volume water content were fit using the van Genuchten model (1). The fitting parameters are shown in Table 4, and the fitting curves are shown in Figure 6.where ψ represents matric suction (kPa); θ represents volumetric moisture content (%); θs represents saturated volumetric moisture content (%); θr represents residual volumetric water content (%); and α and b represent model fitting parameters.The expression of the van Genuchten model [29] is as follows:(1)θ−θrθs−θr=1+αψb1/b−1.Table 4
Fitting parameters of the van Genuchten model.
Dry densityρd`(g/cm3)Fitting parametersθs (%)θr (%)αbR21.4046.7611.84090.08181.73190.9991.5043.6510.83690.07941.62110.9991.6040.489.67090.07431.51780.9981.7037.4013.72450.06341.62020.999Figure 6
Soil-water characteristic curve fit using the van Genuchten model.Van Genuchten model equation correlates well with the fitting curve for the soil-water characteristic curve test data. Compacted loess with different dry densities had different matrix suctions due to different particle and pore structures. Matric suction at various dry densities increased with a decrease in volumetric water content (Figure6). When matric suction increased to 40 kPa, because of the water holding capacity of large and small pores in different dry densities was exactly the same, the soil-water characteristic curves intersect at a point where the volumetric water content was approximately equal. For the same volume of water, when ψ < 40 kPa, the dry density decreased, and the matrix suction increased. When matrix suction was low, pores in smaller dry density soils were larger, and water capacity decreased. When ψ > 40 kPa, the dry density and matrix suction increased due to the increased number of small pores in higher dry density soil. Matrix suction was larger in small pores compared to large pores (Table 4).The soil-water characteristic curve (Figure6) was divided into m equal parts along the volumetric water content axis, and the matrix suction corresponding to each section midpoint was obtained. According to the Childs and Collis-Geroge model [30], the permeability coefficient k(θ) of unsaturated compacted loess is given by(2)kθi=kskscAd∑j=im2j+1−2iua−uwj−2,i=1,2,⋯,m,(3)ksc=Ad∑j=im2j+1−2iua−uwj−2,i=0,(4)Ad=Ts2ρwgθsp2μwN2,where k(θ)i represents permeability coefficient corresponding to volume moisture content θi (cm/s); ks represents saturated permeability coefficient measured by experiment (cm/s); ksc represents calculative saturated permeability coefficient (cm/s); Ad represents an adjustment constant, which is related to the density and surface tension of water; Ts represents water surface tension (kN/m); pw represents water density (kg/m3); g represents gravity acceleration (m/s2); μw represents water absolute viscosity (N·s/m2); θs represents saturated volumetric water content (%); ug−uwd represents matrix suction corresponding to the middle point of j interval (kPa); m represents equivalent fraction between saturated volumetric water content and minimum volumetric water content on the soil-water characteristic curve (m = 10); i represents discontinuous numbering; and j represents counting from i to m.Matrix suction did not show anisotropy, so the horizontal and vertical suctions were equal. Based on the saturated permeability coefficientsks measured in the vertical and horizontal directions based on the permeability test at ug−uw=0kPa (Table 2) combined with the matrix suction ug−uwi, equations (2)–(4), the unsaturated permeability coefficients kv in the vertical direction and kh parallel compaction plane of compacted loess were calculated, respectively (Table 5). In order to study the influence of matrix suction on permeability coefficient of unsaturated compacted loess, the curves between permeability coefficient and matrix suction of unsaturated compacted loess with different dry densities were determined (Figure 7).Table 5
Calculated permeability coefficient of unsaturated compacted loess.
ρd = 1.40 g/cm3ρd = 1.50 g/cm3ρd = 1.60 g/cm3ρd = 1.70 g/cm3ug−uw/kPakv /10−6cm/skh /10−6cm/sug−uw/kPakv/10−6cm/skh/10−6cm/sug−uw/kPakv/10−6cm/skh/10−6cm/sug−uw/kPakv/10−6cm/skh/10−6cm/s00 87.769109.0300 24.2135.84800 9.62516.08300 3.2056.2511.33136.32445.1221.4749.99414.7971.6323.9656.6251.8021.3222.5794.3287.3499.1304.8061.9992.9605.3550.7861.3135.9280.2650.5177.8932.9723.6918.9810.8121.2029.9910.3190.53311.1090.1100.21412.5271.3561.68713.9190.3770.55915.7630.1490.24917.2110.0520.10217.9960.6370.79120.4780.1800.26622.8110.0720.12024.8540.0250.05026.3640.2930.36428.9070.0850.12532.2270.0340.05734.2450.0120.02437.1630.1290.16040.6220.0370.05544.8330.0150.025648.6910.00550.010752.4270.05080.06355.5370.0150.021962.7180.0060.010466.8720.00230.004475.2630.01620.02082.5180.00470.006988.4910.0020.003493.6270.000760.0015114.1450.00310.0038123.2360.000890.0013129.0010.00040.00067133.8210.000150.0003Figure 7
Relationship between permeability coefficient and matrix suction of unsaturated compacted loess: (a)ρd = 1.40 g/cm3, (b) ρd = 1.50 g/cm3, (c) ρd = 1.60 g/cm3, and (d) ρd = 1.70 g/cm3.
(a)(b)(c)(d)The permeability coefficient of unsaturated compacted loess was significantly affected by matrix suction and decreased with an increase in matrix suction. When matrix suction was less than 10 kPa, the relationship between permeability coefficient in the horizontal and vertical directions and the matrix suction sharply decreased. When matrix suction was greater than 10 kPa and less than 40 kPa, the slope of the relationship curve gradually decreased and tended to be gentle. When the matrix suction was greater than 40 kPa, the difference between the vertical and horizontal permeability coefficients was less than 0.01 × 10−6cm/s, and the relationship curve tended to be consistent.


### 3.3. Permeability Anisotropy of Unsaturated Compacted Loess

The influence of pore connectivity and tortuosity on water flow in pores in different directions was different from saturated soils [31]. Matrix suction had a significant effect on unsaturated permeability anisotropy of layered soils [32]. The theoretical relationship between anisotropy and saturation was put forward by Mualem [33]. Saturated permeability anisotropy is closely related to the degree of soil saturation [33]. The permeability coefficient of unsaturated soils indirectly calculated using the soil-water characteristic curve was based on the saturated permeability coefficient. The anisotropy of the unsaturated permeability coefficient perpendicular and parallel to the compaction plane was consistent with the saturated permeability anisotropy, which could not show that unsaturated permeability anisotropy was affected by matrix suction.Pore connectivity-tortuosity parameterL was introduced to study the unsaturated permeability coefficient of isotropic soils [33].(5)k=CksSeL,C=∫0Seψx−1dx∫01ψx−1dx2,Se=θ−θrθs−θr,where k represents permeability coefficient (cm/s); Se represents effective degree of saturation (%); L represents pore connectivity-tortuous parameters; ψ represents matric suction (kPa); θ represents volumetric moisture content (%); θs represents saturated volumetric moisture content (%); and θr represents residual volumetric water content (%).Based on the unsaturated permeability coefficient function proposed by Mualem [17], Zhang et al. [34] introduced a pore connectivity-tortuosity parameter L to establish the relationship between unsaturated permeability coefficient, saturated permeability coefficient, and matrix suction (van Genuchten-Mualem equation).(6)k=ks1+αψbL1/b−11−αψb1+αψb1−1/b2,(7)Ahv=kshksv·1+αψbΔLhv⋅1/b−1,where Ahv represents anisotropy coefficient; ΔLhy=Lh−Lv represents pore connectivity-tortuous parameters for horizontal direction, and Lv represents pore connectivity-tortuous parameters for the vertical direction.Pore connectivity-tortuosity parameters were obtained by fitting the measured unsaturated permeability coefficient into equation (6). Fitted parameters were substituted into equation (7) to analyze the anisotropy of unsaturated permeability coefficient; however, the physical meaning, which reflected the pore connectivity and tortuosity of compacted loess, was not clear. The permeability of water in soil was influenced by pore characteristics and was determined by the connectivity-tortuosity of pores under a certain hydraulic gradient. Permeability coefficient was an intuitive expression of pore connectivity-tortuosity. The difference in horizontal and vertical permeability coefficients for saturated compacted loess directly reflected differences in pore connectivity-tortuosity characteristics in the vertical and horizontal directions. The saturated permeability anisotropy ratio not only reflected differences in horizontal and vertical permeability coefficients for saturated compacted loess but also reflected differences in connectivity-tortuosity characteristics of soil pores. If the common pore characteristics reflected in the saturated permeability anisotropy ratio rks were removed, then the difference between the horizontal and vertical pore connectivity-tortuosity characteristics (pore connectivity-tortuosity parameter L) in compacted loess could be obtained. The saturated permeability anisotropy ratio was used to represent pore connectivity-tortuosity parameters, and its physical meaning was clear.According to the definition of permeability anisotropy ratio for saturated compacted loess, unsaturated permeability anisotropy was defined as the ratiork. The permeability anisotropy of unsaturated compacted loess was expressed using the saturated permeability anisotropy ratio, and the pore connectivity-tortuosity parameter was introduced to establish the relationship between the unsaturated permeability anisotropy ratio and effective saturation degree.(8)rk=rks⋅SeL.Equations (1) and (5) are substituted into equation (8):(9)rk=rks⋅1+αψbL⋅1/b−1,where rk represents anisotropic ratio of unsaturated permeability; rks represents anisotropic ratio of saturated permeability; and L represents pore connectivity-tortuous parameters, when rks>1, L = rks-1, and when rks<1, L = -rks-1.For saturated soil, the matrix suction isψ = 0 kPa, and when the soil was isotropic, rks = 1, L = 0, and then, rk = 1.According to equation (9) in combination with data from Tables 1 and 5, the curve between permeability anisotropy ratio and matrix suction of unsaturated compacted loess was calculated (Figure 8):(1)
The permeability anisotropy of unsaturated compacted loess decreased with an increase in matrix suction. The pore connectivity-tortuosity parameter clearly reflects the influence of matrix suction on the permeability anisotropy of unsaturated compacted loess.(2)
Whenρd  = 1.7 g/cm3, the difference in pore structure and particle arrangement in the horizontal and vertical directions during loess compaction increased, and the difference in pore connectivity and tortuous path in the horizontal and vertical directions was more significant, as shown by the larger pore connectivity-tortuous parameter values. The anisotropy ratio of unsaturated permeability was significantly affected by matrix suction, and the curve was steeper. When ρd = 1.4 g/cm3, the difference in pore structure and particle arrangement in the horizontal and vertical directions during the loess compaction process was smaller, and the difference in pore connectivity and tortuous path in the horizontal and vertical directions decreased, as shown by the smaller pore connectivity-tortuous parameter values. The anisotropy ratio of unsaturated permeability was less affected by matrix suction, and the curve was gentle.(3)
Pore connectivity-tortuous parameters not only reflect the influence of matrix suction on permeability anisotropy of unsaturated compacted loess but also reflect the pore structure and arrangement characteristics of compacted loess with different dry densities, which is of great significance to the study of water migration in unsaturated compacted loess.Figure 8
Relationship between permeability anisotropy ratio and matrix suction.


### 3.4. Rationality Verification of Defined Pore Connectivity-Torture Parameter

Zhang et al. [34] used equations (6) and (7) to analyze the influence of matrix suction on the anisotropy coefficient of three types of soils: Cass sandy loam, Fort Collins clay loam [35], and Xi’an Q3 undisturbed loess [36]. In this study, the unsaturated permeability anisotropy of the above three soils was analyzed using equation (9). Results were compared with the results of Zhang et al. [34], in order to verify the rationality of the proposed pore connectivity-tortuosity parameter and equation (9) (Figure 9).Figure 9
Relationship between measured and calculated unsaturated permeability anisotropy ratio and matrix suction for three types of soils. (a) Cass sandy loam [35], (b) Fort Collins clay loam [35], and (c) Xi’an Q3 undisturbed loess [36].
(a)(b)(c)Compared with the results of equation (7), the unsaturated permeability anisotropy for the three soil types calculated using equation (9) was in good agreement with the test data (Figure 9). The relative error between the test data and the calculated data using equation (7) was 16.4%–23.2%, and the relative error between the test data and the calculated data using equation (9) was 4.1%–8.7%. Thus, the pore connectivity-tortuosity parameters defined in this contribution can reasonably describe the variation in permeability anisotropy of unsaturated soils with matrix suction.


## 3.1. Soil-Water Characteristic Curve Test Results

The volumetric water content and matrix suction of compacted loess with dry densities of 1.40 g/cm3, 1.50 g/cm3, 1.60 g/cm3, and 1.70 g/cm3 are shown in Table 3. With an increase in matrix suction, the volumetric water content of soil samples gradually decreased. When the soil dry density was high, the decrease in volumetric water content was smaller for the same change in matrix suction. On the contrary, when the dry density of soil was low, the decrease in volumetric water content was large for the same change in matrix suction (Table 3).Table 3
Soil-water characteristic curve test values for compacted loess.
Matric suctionψ/kPaVolumetric water contentθ/%ρd = 1.40 g/cm3ρd = 1.50 g/cm3ρd = 1.60 g/cm3ρd = 1.70 g/cm3046.7643.6540.4837.401039.3237.5035.1933.922033.2132.1831.8730.764026.0526.4526.3425.946022.1022.4323.1823.428020.2420.9121.3622.1010019.1319.8620.3021.3614017.7718.0918.8119.8718016.9617.2717.8918.79


## 3.2. Determiningk(θ) Using the Van Genuchten Soil-Water Characteristic Curve Model

Due to data complexity, data discreteness, and the time-consuming soil-water characteristic curve test, the test data represent only a part of the soil-water characteristic curve. In order to obtain a complete soil-water characteristic curve, measured matrix suction and volume water content were fit using the van Genuchten model (1). The fitting parameters are shown in Table 4, and the fitting curves are shown in Figure 6.where ψ represents matric suction (kPa); θ represents volumetric moisture content (%); θs represents saturated volumetric moisture content (%); θr represents residual volumetric water content (%); and α and b represent model fitting parameters.The expression of the van Genuchten model [29] is as follows:(1)θ−θrθs−θr=1+αψb1/b−1.Table 4
Fitting parameters of the van Genuchten model.
Dry densityρd`(g/cm3)Fitting parametersθs (%)θr (%)αbR21.4046.7611.84090.08181.73190.9991.5043.6510.83690.07941.62110.9991.6040.489.67090.07431.51780.9981.7037.4013.72450.06341.62020.999Figure 6
Soil-water characteristic curve fit using the van Genuchten model.Van Genuchten model equation correlates well with the fitting curve for the soil-water characteristic curve test data. Compacted loess with different dry densities had different matrix suctions due to different particle and pore structures. Matric suction at various dry densities increased with a decrease in volumetric water content (Figure6). When matric suction increased to 40 kPa, because of the water holding capacity of large and small pores in different dry densities was exactly the same, the soil-water characteristic curves intersect at a point where the volumetric water content was approximately equal. For the same volume of water, when ψ < 40 kPa, the dry density decreased, and the matrix suction increased. When matrix suction was low, pores in smaller dry density soils were larger, and water capacity decreased. When ψ > 40 kPa, the dry density and matrix suction increased due to the increased number of small pores in higher dry density soil. Matrix suction was larger in small pores compared to large pores (Table 4).The soil-water characteristic curve (Figure6) was divided into m equal parts along the volumetric water content axis, and the matrix suction corresponding to each section midpoint was obtained. According to the Childs and Collis-Geroge model [30], the permeability coefficient k(θ) of unsaturated compacted loess is given by(2)kθi=kskscAd∑j=im2j+1−2iua−uwj−2,i=1,2,⋯,m,(3)ksc=Ad∑j=im2j+1−2iua−uwj−2,i=0,(4)Ad=Ts2ρwgθsp2μwN2,where k(θ)i represents permeability coefficient corresponding to volume moisture content θi (cm/s); ks represents saturated permeability coefficient measured by experiment (cm/s); ksc represents calculative saturated permeability coefficient (cm/s); Ad represents an adjustment constant, which is related to the density and surface tension of water; Ts represents water surface tension (kN/m); pw represents water density (kg/m3); g represents gravity acceleration (m/s2); μw represents water absolute viscosity (N·s/m2); θs represents saturated volumetric water content (%); ug−uwd represents matrix suction corresponding to the middle point of j interval (kPa); m represents equivalent fraction between saturated volumetric water content and minimum volumetric water content on the soil-water characteristic curve (m = 10); i represents discontinuous numbering; and j represents counting from i to m.Matrix suction did not show anisotropy, so the horizontal and vertical suctions were equal. Based on the saturated permeability coefficientsks measured in the vertical and horizontal directions based on the permeability test at ug−uw=0kPa (Table 2) combined with the matrix suction ug−uwi, equations (2)–(4), the unsaturated permeability coefficients kv in the vertical direction and kh parallel compaction plane of compacted loess were calculated, respectively (Table 5). In order to study the influence of matrix suction on permeability coefficient of unsaturated compacted loess, the curves between permeability coefficient and matrix suction of unsaturated compacted loess with different dry densities were determined (Figure 7).Table 5
Calculated permeability coefficient of unsaturated compacted loess.
ρd = 1.40 g/cm3ρd = 1.50 g/cm3ρd = 1.60 g/cm3ρd = 1.70 g/cm3ug−uw/kPakv /10−6cm/skh /10−6cm/sug−uw/kPakv/10−6cm/skh/10−6cm/sug−uw/kPakv/10−6cm/skh/10−6cm/sug−uw/kPakv/10−6cm/skh/10−6cm/s00 87.769109.0300 24.2135.84800 9.62516.08300 3.2056.2511.33136.32445.1221.4749.99414.7971.6323.9656.6251.8021.3222.5794.3287.3499.1304.8061.9992.9605.3550.7861.3135.9280.2650.5177.8932.9723.6918.9810.8121.2029.9910.3190.53311.1090.1100.21412.5271.3561.68713.9190.3770.55915.7630.1490.24917.2110.0520.10217.9960.6370.79120.4780.1800.26622.8110.0720.12024.8540.0250.05026.3640.2930.36428.9070.0850.12532.2270.0340.05734.2450.0120.02437.1630.1290.16040.6220.0370.05544.8330.0150.025648.6910.00550.010752.4270.05080.06355.5370.0150.021962.7180.0060.010466.8720.00230.004475.2630.01620.02082.5180.00470.006988.4910.0020.003493.6270.000760.0015114.1450.00310.0038123.2360.000890.0013129.0010.00040.00067133.8210.000150.0003Figure 7
Relationship between permeability coefficient and matrix suction of unsaturated compacted loess: (a)ρd = 1.40 g/cm3, (b) ρd = 1.50 g/cm3, (c) ρd = 1.60 g/cm3, and (d) ρd = 1.70 g/cm3.
(a)(b)(c)(d)The permeability coefficient of unsaturated compacted loess was significantly affected by matrix suction and decreased with an increase in matrix suction. When matrix suction was less than 10 kPa, the relationship between permeability coefficient in the horizontal and vertical directions and the matrix suction sharply decreased. When matrix suction was greater than 10 kPa and less than 40 kPa, the slope of the relationship curve gradually decreased and tended to be gentle. When the matrix suction was greater than 40 kPa, the difference between the vertical and horizontal permeability coefficients was less than 0.01 × 10−6cm/s, and the relationship curve tended to be consistent.


## 3.3. Permeability Anisotropy of Unsaturated Compacted Loess

The influence of pore connectivity and tortuosity on water flow in pores in different directions was different from saturated soils [31]. Matrix suction had a significant effect on unsaturated permeability anisotropy of layered soils [32]. The theoretical relationship between anisotropy and saturation was put forward by Mualem [33]. Saturated permeability anisotropy is closely related to the degree of soil saturation [33]. The permeability coefficient of unsaturated soils indirectly calculated using the soil-water characteristic curve was based on the saturated permeability coefficient. The anisotropy of the unsaturated permeability coefficient perpendicular and parallel to the compaction plane was consistent with the saturated permeability anisotropy, which could not show that unsaturated permeability anisotropy was affected by matrix suction.Pore connectivity-tortuosity parameterL was introduced to study the unsaturated permeability coefficient of isotropic soils [33].(5)k=CksSeL,C=∫0Seψx−1dx∫01ψx−1dx2,Se=θ−θrθs−θr,where k represents permeability coefficient (cm/s); Se represents effective degree of saturation (%); L represents pore connectivity-tortuous parameters; ψ represents matric suction (kPa); θ represents volumetric moisture content (%); θs represents saturated volumetric moisture content (%); and θr represents residual volumetric water content (%).Based on the unsaturated permeability coefficient function proposed by Mualem [17], Zhang et al. [34] introduced a pore connectivity-tortuosity parameter L to establish the relationship between unsaturated permeability coefficient, saturated permeability coefficient, and matrix suction (van Genuchten-Mualem equation).(6)k=ks1+αψbL1/b−11−αψb1+αψb1−1/b2,(7)Ahv=kshksv·1+αψbΔLhv⋅1/b−1,where Ahv represents anisotropy coefficient; ΔLhy=Lh−Lv represents pore connectivity-tortuous parameters for horizontal direction, and Lv represents pore connectivity-tortuous parameters for the vertical direction.Pore connectivity-tortuosity parameters were obtained by fitting the measured unsaturated permeability coefficient into equation (6). Fitted parameters were substituted into equation (7) to analyze the anisotropy of unsaturated permeability coefficient; however, the physical meaning, which reflected the pore connectivity and tortuosity of compacted loess, was not clear. The permeability of water in soil was influenced by pore characteristics and was determined by the connectivity-tortuosity of pores under a certain hydraulic gradient. Permeability coefficient was an intuitive expression of pore connectivity-tortuosity. The difference in horizontal and vertical permeability coefficients for saturated compacted loess directly reflected differences in pore connectivity-tortuosity characteristics in the vertical and horizontal directions. The saturated permeability anisotropy ratio not only reflected differences in horizontal and vertical permeability coefficients for saturated compacted loess but also reflected differences in connectivity-tortuosity characteristics of soil pores. If the common pore characteristics reflected in the saturated permeability anisotropy ratio rks were removed, then the difference between the horizontal and vertical pore connectivity-tortuosity characteristics (pore connectivity-tortuosity parameter L) in compacted loess could be obtained. The saturated permeability anisotropy ratio was used to represent pore connectivity-tortuosity parameters, and its physical meaning was clear.According to the definition of permeability anisotropy ratio for saturated compacted loess, unsaturated permeability anisotropy was defined as the ratiork. The permeability anisotropy of unsaturated compacted loess was expressed using the saturated permeability anisotropy ratio, and the pore connectivity-tortuosity parameter was introduced to establish the relationship between the unsaturated permeability anisotropy ratio and effective saturation degree.(8)rk=rks⋅SeL.Equations (1) and (5) are substituted into equation (8):(9)rk=rks⋅1+αψbL⋅1/b−1,where rk represents anisotropic ratio of unsaturated permeability; rks represents anisotropic ratio of saturated permeability; and L represents pore connectivity-tortuous parameters, when rks>1, L = rks-1, and when rks<1, L = -rks-1.For saturated soil, the matrix suction isψ = 0 kPa, and when the soil was isotropic, rks = 1, L = 0, and then, rk = 1.According to equation (9) in combination with data from Tables 1 and 5, the curve between permeability anisotropy ratio and matrix suction of unsaturated compacted loess was calculated (Figure 8):(1)
The permeability anisotropy of unsaturated compacted loess decreased with an increase in matrix suction. The pore connectivity-tortuosity parameter clearly reflects the influence of matrix suction on the permeability anisotropy of unsaturated compacted loess.(2)
Whenρd  = 1.7 g/cm3, the difference in pore structure and particle arrangement in the horizontal and vertical directions during loess compaction increased, and the difference in pore connectivity and tortuous path in the horizontal and vertical directions was more significant, as shown by the larger pore connectivity-tortuous parameter values. The anisotropy ratio of unsaturated permeability was significantly affected by matrix suction, and the curve was steeper. When ρd = 1.4 g/cm3, the difference in pore structure and particle arrangement in the horizontal and vertical directions during the loess compaction process was smaller, and the difference in pore connectivity and tortuous path in the horizontal and vertical directions decreased, as shown by the smaller pore connectivity-tortuous parameter values. The anisotropy ratio of unsaturated permeability was less affected by matrix suction, and the curve was gentle.(3)
Pore connectivity-tortuous parameters not only reflect the influence of matrix suction on permeability anisotropy of unsaturated compacted loess but also reflect the pore structure and arrangement characteristics of compacted loess with different dry densities, which is of great significance to the study of water migration in unsaturated compacted loess.Figure 8
Relationship between permeability anisotropy ratio and matrix suction.


## 3.4. Rationality Verification of Defined Pore Connectivity-Torture Parameter

Zhang et al. [34] used equations (6) and (7) to analyze the influence of matrix suction on the anisotropy coefficient of three types of soils: Cass sandy loam, Fort Collins clay loam [35], and Xi’an Q3 undisturbed loess [36]. In this study, the unsaturated permeability anisotropy of the above three soils was analyzed using equation (9). Results were compared with the results of Zhang et al. [34], in order to verify the rationality of the proposed pore connectivity-tortuosity parameter and equation (9) (Figure 9).Figure 9
Relationship between measured and calculated unsaturated permeability anisotropy ratio and matrix suction for three types of soils. (a) Cass sandy loam [35], (b) Fort Collins clay loam [35], and (c) Xi’an Q3 undisturbed loess [36].
(a)(b)(c)Compared with the results of equation (7), the unsaturated permeability anisotropy for the three soil types calculated using equation (9) was in good agreement with the test data (Figure 9). The relative error between the test data and the calculated data using equation (7) was 16.4%–23.2%, and the relative error between the test data and the calculated data using equation (9) was 4.1%–8.7%. Thus, the pore connectivity-tortuosity parameters defined in this contribution can reasonably describe the variation in permeability anisotropy of unsaturated soils with matrix suction.


## 4. Microscopic Mechanism of Permeability Anisotropy

SEM tests were carried out on loess samples with different compacted dry densities to obtain images, which are shown in Figure10.Figure 10
SEM images with different dry densities (500 times) [4]. (a) ρd = 1.70 g/cm3, (b) ρd = 1.60 g/cm3, (c) ρd = 1.50 g/cm3, and (d) ρd = 1.40 g/cm3.
(a)(b)(c)(d)The micropore structures of the compacted surface and vertical compacted surface were significantly different (Figure10). The number of pores perpendicular to the compacted surface was greater than that of the compacted surface, and pore connectivity was better. This was the primary reason why the permeability coefficient of compacted loess was large parallel to the compacted surface was larger compared to the permeability perpendicular to the compacted surface. The number of pores on the compacted surface and perpendicular to the compacted surface gradually increased with a decrease in dry density. However, the difference of pore diameter and number on the compacted surface and perpendicular to the compacted surface decreased with a decrease in dry density, which revealed the reason why smaller dry densities correlate with smaller permeability anisotropy. On the contrary, when the dry density was higher, the permeability anisotropy was greater [4].


## 5. Conclusions

By conducting permeability test and soil-water characteristic curve test on compacted loess of different dry densities, this study investigated the permeability anisotropy of unsaturated compacted loess and drew the following conclusions:(1)
The vertical and horizontal permeability coefficients of saturated compacted loess significantly decreased with the increase in dry density. The horizontal saturated permeability coefficient of compacted loess was larger than that in the vertical direction, showing obvious anisotropy. Flake and needle particles rotated to be parallel with the compaction surface after vertical compaction, which weakened the porosity and connectivity of the pores, led to a reduction in vertical saturated permeability coefficient. The porosity and connectivity of pores parallel to the compaction surface were improved to make the horizontal permeability coefficient larger.(2)
Van Genuchten model equation correlated well with the fitting curve for the soil-water characteristic curve test data. Based on the vertical and horizontal saturated permeability coefficients, the permeability coefficient of unsaturated compacted loess was calculated using the soil-water characteristic curve fitted using the van Genuchten model and Childs and Collis-Geroge model. The permeability anisotropy of unsaturated compacted loess could be expressed by the ratio of unsaturated permeability anisotropy.(3)
The pore connectivity-tortuosity parameter was introduced to establish the equation between the unsaturated permeability anisotropy ratio and matrix suction. The rationality of the equation was verified by comparing test and calculated datasets for unsaturated permeability anisotropy of Cass sandy loam, Fort Collins clay loam, and Xi’anQ3 undisturbed loess. The physical meaning of the introduced pore connectivity-tortuosity parameter was clear and reasonable, and the pore connectivity-tortuosity parameter could express the relationship between the anisotropy ratio of unsaturated permeability and matrix suction.(4)
The microtest showed that the permeability anisotropy of compacted loess with different dry density was mainly caused by the different pore structures in the direction of vertical compaction surface and horizontal compaction surface [37].



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