# Geological Hazards in Loess Induced by Agricultural Irrigation in Arid and Semiarid Regions of China

Authors: Yuan-jun Xu; Jia-ding Wang; Tian-feng Gu; Jia-xu Kong
Journal: Advances in Civil Engineering
 (2020)

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## Abstract

The development of agriculture in the arid and semiarid regions of China mainly depends on agricultural irrigation. Until 2016, water required for agricultural irrigation has accounted for more than 90% of the total water consumption. But traditionally extensive broad irrigation causes frequent loess geological hazards in irrigation area and it threatens security of local life and property. In this paper, we selected the Heifangtai irrigation district in Yongjing County, Gansu Province, where frequent instabilities occur, as the study area. We used laboratory tests and numerical simulation to examine the mechanism of loess landslides owing to the irrigation hydrological cycle. Irrigation changes the local natural hydrogeological conditions because of the loose and macroporous structure of loess. The numerous pores and fissures constitute preferential migration pathways of irrigation water; thus, irrigation can increase the groundwater level and hydraulic gradient. Broad irrigation is the main inducing factor of geological hazards (including landslides, collapses, and soil salinization) in arid and semiarid regions, and the development of fissures and sinkholes increases the risk of landslides. New water-saving irrigation methods need to replace the traditional irrigation methods and improve the utilization of water resources. A monitoring and warning system in susceptible areas should be established to ensure the sustainability of local agriculture.


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## Body

## 1. Introduction

China needs to feed a quarter of the world’s population using 7% of the available agricultural land. However, 49% of the agricultural land in China is in arid and semiarid regions, with temperate continental climate [1, 2]. Annual precipitation is less than 400 mm and gradually decreases from east to west. There are only few inland rivers and most of them are seasonal. The growth of crops depends on ample water and solar radiation, but high temperature, less rainfall, and extreme weather have pernicious effect on agricultural production [3]. Because of the population increase in China, the normalization of agricultural irrigation was realized in most agricultural areas of China [4, 5]; however, traditional broad irrigation is still the main irrigation method in west China. This irrigation method drastically increases agricultural production and changes the water balance of the irrigated district, which also causes the underground water level in the irrigated district to rise. Therefore, geologic hazards induced by broad irrigation increase in frequency [6–9], and this restricts the development of new-type urbanization and regional society economy, even impedes economic development of Silk Road Economic Belt.The change of the local hydrogeological conditions caused by long-term broad irrigation is the main induced factor of geological disasters. The local geological environment favours landslides. Therefore, it is necessary to study the mechanism of loess irrigation infiltration to analyze the geological hazards of loess irrigation. Water migration pathways greatly affect the seepage of irrigation water. Beven and German [10] first proposed the theory of soil superiority flow; the influence of preferential migration pathway on the infiltration and diffusion of surface water was studied through experimental validation and theoretical analysis. German and Beven [11] presented a method for evaluating the effect of micropores on infiltration capacity by using the concept of the soil–water potential. Theoretical and numerical models were used to study the inflow infiltration mode, controlling factors, the spatial distribution, and water migration patterns of preferential migration runoff [12]. Xu et al. [13] argued that the infiltration of broad irrigation water through preferential migration pathways increased the groundwater level and it was the main reason for fast mass slides in remote areas. Loess landslides induced by irrigation are attributed to the water seepage in slopes that increases the sliding force and decreases the sliding resistance [14]. Hutchinson [15] proposed that soil landslides are induced by irrigation because of structural deterioration and increase in pore pressure and liquefaction. Sassa [16] further pointed out that more than 85% saturation is sufficient to produce excess pore water pressure, leading to landslides. Wang and Hui [17–19] argued that irrigation infiltration increases the pore water pressure but also decreases the permeability; thus, pore water pressure does not dissipate and landslides occur. Wang [20, 21] proposed that creep and liquefaction in saturated loess are responsible for landslides. Previous research was mainly on water infiltration and soil behavior [22, 23] and the relation between groundwater level and landslides [24]. However, the effect of irrigation on slope hydrology is a long-term process; the current method is mainly on-site monitoring, which needs a long time. This paper uses numerical analysis and indoor unsaturated test to explore the mechanism of loess landslide in irrigation area.The paper mainly studies the landslides in loess induced by irrigation in arid and semiarid regions by using laboratory tests and numerical simulation. The research area is Heifangtai platform, which is known as the natural laboratory of landslides. Methods to control landslides induced by irrigation were also proposed. The test results and conclusions derived in this study will provide scientific guidance for the prevention and warning of the loess geological disasters induced by agricultural irrigation in arid and semiarid regions of China.


## 2. Irrigation and Geological Hazards in Arid and Semiarid Region

With the development of engineering technology, massive hydraulic projects aimed to foster agricultural development of arid regions in the middle and lower reaches of the Yellow River and its tributaries. Traditional agricultural irrigation methods are surface irrigation (border irrigation, furrow irrigation, basin irrigation, and broad irrigation), general irrigation, and microirrigation. Agriculture in the arid and semiarid regions of northwestern China mainly depends on agricultural irrigation owing to topography and climate [25]. However, long-term use of broad irrigation wastes freshwater resources (China Water Resources Bulletin, 2004–2016). Agricultural water accounts for more than 90% of the used water in northwestern China (Table 1 and Figure 1).Table 1
Water supply and water consumption of five provinces and autonomous regions in northwest China in 2016.
Province-level administrationWater supply (×10−1°km3)Water consumption (×10−1°km3)Surface waterGround waterOthersThe total amount of water supplyAgricultureThe total amount of water consumptionShaanxi55.533.32.090.857.690.8Gansu90.524.83.0118.494.7118.4Qinghai21.54.80.126.419.926.4Ningxia59.45.30.264.956.364.9Sinkiang445.9118.60.9565.4533.3565.4Figure 1
Agricultural water consumption of five provinces and autonomous regions in northwest China during 2004 to 2016 (China Water Resources Bulletin, 2004–2016).Long-term surface irrigation increases the supply of groundwater, which changes the local hydrogeological conditions and induces landslides, collapses, and mudflows. Geological hazards in loess area induced by irrigation are mainly distributed in the Shaanxi, Gansu, Ningxia, Qinghai, Henan, and Shanxi Provinces, especially, along the Jinghe, Weihe, and Huangshuihe Rivers and their tributaries. Groups of ribbon-like landslides often stretch to tens of kilometres. Typically, geological hazards in loess induced by broad irrigation occur in the Jingyang south plateau of Shaanxi Province [26, 27] and the Heifangtai tableland of Gansu Province [28, 29]. Mountain forests around cities need sprinkle irrigation that can cause landslides, such as the Yikeyin landslide in Xi’ning Province [30] and Wenmiao landslide in Lanzhou City. Canal seepage is ubiquitous in irrigated areas, causing loess collapse and landslides, e.g., Gaolou landslide in Huaxian, Shaanxi Province [31]. Geological hazards in loess threaten human lives and incur property damages, negatively affecting the local economies.


### 2.1. Irrigation and Agriculture in Heifangtai Tableland

The paper takes Heifangtai irrigation in Liujiaxia reservoir and Yanguoxia reservoir area as typical irrigation area to state the development of agriculture in irrigation area. The Heifangtai tableland is a typical loess landscape with no water and thus economically backward. Since 1963, reservoir resettlement of Liujiaxia, Yanguoxia, and Bapanxia reservoir has been moved to Heifangtai tableland. To provide agricultural and drinking water for the migration, three pumping engineering projects (Figure2) were successively built during July 1966 to June 1969. Lifting irrigation takes place five times a year in the irrigation area. Spring irrigation occurs from March to May, winter irrigation from November to December, and three times irrigation of young crops. Recently, the Heifangtai area is the most important vegetable- and fruit-producing area in the Lanzhou district. There has been a structural adjustment of agricultural production from traditional food crops, such as wheat and maize, to high-yielding crops, such as fruits and vegetables. Therefore, agricultural irrigation has significantly increased, and the irrigation channel system has become denser (Figure 3). Except for spring and winter irrigation, the irrigation of young crops has increased to five times a year and the annual mean irrigation volume of the Fangtai tableland has increased to 5.909 × 104 m3, with frequent broad irrigation (Figure 2(b)). The yearly irrigations are not equally distributed but depend on water need and rainfall. The annual mean irrigation quota per square kilometer is 838.56 m3 according to the latest actual irrigation area (0.705 km2). The maximal evapotranspiration of the farmland is 880 mm (including ground surface evaporating and leaf transpiration) and the supplementary irrigation for crops is 657.6 mm after deducting the maximal evapotranspiration of the farmland. Moreover, the annual mean irrigation volume is 4.98 × 106 m3. In other words, the irrigation of the Heitai tableland exceeds by 20% the water needs of the Heifangtai tableland in schedule except for the irrigation of the Fangtai tableland.Figure 2
Agricultural irrigation in Heifangtai area. (a) Pumping engineering projects. (b) Broad irrigation.
(a)(b)Figure 3
Distribution map of acequia and landslide in Heifangtai tableland of Gansu province.


### 2.2. Irrigation Water Infiltration

The mode of irrigation water infiltration and effect on groundwater are shown in Figure4. The climate in the Heifangtai loess plateau is arid to semiarid. Consequently, the surface water evaporates, and the plant evapotranspiration is high. Irrigation water infiltration is the main mechanism of groundwater recharge. The traditional extensive irrigation causes nonpoint source recharge, while the fissures induced by canal network form rapid infiltration channels. Furthermore, the agricultural crop structure has been recently adjusted to high-water consumption crops, such as fruits and vegetables, causing the underground water level to rise. Because of the low permeability of loess, the irrigation water moves through preferential migration pathways in loess, such as macroporous structures, vertical fractures, and subsurface erosion sinkholes to recharge the groundwater. When the irrigation water infiltrates quickly, the strong action owing to the potential and kinetic energy of the preferential flow expands the original preferential migration pathways and groundwater discharges as springs or runoff in slopes. With the rising of the groundwater level because of the fast recharge of irrigation water through loess fissures or sinkholes, the groundwater hydrodynamic field rapidly increases in slopes but the water level sharply drops after the discharge passes. The intense subsurface erosion makes holes inside the slopes, causing the upper slope to slump; therefore, series of landslides form along the loess plateau.Figure 4
Irrigation water infiltration mode.


### 2.3. Groundwater Level Rise Induced by Irrigation

The conceptual hydrogeological model for the Heifangtai tableland is that of a block between rivers (Figure5). In addition to irrigation, rainfall is the other groundwater recharge source. The mean annual precipitation is only 282.6 mm and the drought index is 5.6. The loess thicknesses in the Heifangtai area is about 20 m to 25 m [32]. Groundwater recharges as springs or seepages at the top of silty clay layers along the edges of the tableland. Because of the permeability differences between the conglomerate and silty clay layers, the groundwater moves in the conglomerate beds without any water pressure build-up [33]. Sporadic phreatic water occurs in the Cretaceous bedrock fissures. Based on numerical modelling of groundwater, the groundwater level is below the aquifer bottom in the east and west prior to irrigation and aquifer is unwatering. Large-scale irrigation started in 1968 and the groundwater level increased to 0.27 m/a, and at the center of the tableland was 0.57 m/a before 1990. After 1990, the rate gradually slowed to about 0.25 m/a, and the cumulative rise was 20 m up to 2010. It is predicted that the cumulative rise will reach 25 m in 2020 [33].Figure 5
The hydrogeological model for the Heifangtai tableland.


### 2.4. Geological Hazards Induced by Irrigation in the Heifangtai Tableland

The Heifangtai tableland has more than 40 years of irrigation by pumping and traditional broad irrigation, which induces various geological hazards including loess landslides groups and collapse of entire tableland. According to incomplete statistics, about 120 landslides have occurred (Figure6). Consequently, irrigation canals, farmland, roads, and other facilities have been damaged as well as loss of electricity or water, traffic disruption, and heavy casualties have occurred. Landslides have resulted in about 39 deaths, 100 injuries and the relocation of 950 families, five schools, and 13 businesses. According to the official statistics, 200 km2 of farmland have been abandoned with direct economic losses of more than 2 × 108 RMB and unaccounted indirect economic losses. The maximum loess collapse is up to 5.96 m. Furthermore, the numerous collapse fissures, depressions, funnel-shaped sinkholes, and subsurface erosion along the edges of tableland incurred more than 2 km2 farmland loss. Water conservation structures are often seriously damaged, including residence in the villages of Xinyuan, Zhuwang, Chenjia, and Fangtai. Consequently, the local population had to relocate and build new houses every few years. Every family has refurbishment for twice a year, even five or six a year, intensifying the economic burden on residents and the local social contradictions.Figure 6
Loess landslide statistics of Heifangtai tableland from 1980 to now.


## 2.1. Irrigation and Agriculture in Heifangtai Tableland

The paper takes Heifangtai irrigation in Liujiaxia reservoir and Yanguoxia reservoir area as typical irrigation area to state the development of agriculture in irrigation area. The Heifangtai tableland is a typical loess landscape with no water and thus economically backward. Since 1963, reservoir resettlement of Liujiaxia, Yanguoxia, and Bapanxia reservoir has been moved to Heifangtai tableland. To provide agricultural and drinking water for the migration, three pumping engineering projects (Figure2) were successively built during July 1966 to June 1969. Lifting irrigation takes place five times a year in the irrigation area. Spring irrigation occurs from March to May, winter irrigation from November to December, and three times irrigation of young crops. Recently, the Heifangtai area is the most important vegetable- and fruit-producing area in the Lanzhou district. There has been a structural adjustment of agricultural production from traditional food crops, such as wheat and maize, to high-yielding crops, such as fruits and vegetables. Therefore, agricultural irrigation has significantly increased, and the irrigation channel system has become denser (Figure 3). Except for spring and winter irrigation, the irrigation of young crops has increased to five times a year and the annual mean irrigation volume of the Fangtai tableland has increased to 5.909 × 104 m3, with frequent broad irrigation (Figure 2(b)). The yearly irrigations are not equally distributed but depend on water need and rainfall. The annual mean irrigation quota per square kilometer is 838.56 m3 according to the latest actual irrigation area (0.705 km2). The maximal evapotranspiration of the farmland is 880 mm (including ground surface evaporating and leaf transpiration) and the supplementary irrigation for crops is 657.6 mm after deducting the maximal evapotranspiration of the farmland. Moreover, the annual mean irrigation volume is 4.98 × 106 m3. In other words, the irrigation of the Heitai tableland exceeds by 20% the water needs of the Heifangtai tableland in schedule except for the irrigation of the Fangtai tableland.Figure 2
Agricultural irrigation in Heifangtai area. (a) Pumping engineering projects. (b) Broad irrigation.
(a)(b)Figure 3
Distribution map of acequia and landslide in Heifangtai tableland of Gansu province.


## 2.2. Irrigation Water Infiltration

The mode of irrigation water infiltration and effect on groundwater are shown in Figure4. The climate in the Heifangtai loess plateau is arid to semiarid. Consequently, the surface water evaporates, and the plant evapotranspiration is high. Irrigation water infiltration is the main mechanism of groundwater recharge. The traditional extensive irrigation causes nonpoint source recharge, while the fissures induced by canal network form rapid infiltration channels. Furthermore, the agricultural crop structure has been recently adjusted to high-water consumption crops, such as fruits and vegetables, causing the underground water level to rise. Because of the low permeability of loess, the irrigation water moves through preferential migration pathways in loess, such as macroporous structures, vertical fractures, and subsurface erosion sinkholes to recharge the groundwater. When the irrigation water infiltrates quickly, the strong action owing to the potential and kinetic energy of the preferential flow expands the original preferential migration pathways and groundwater discharges as springs or runoff in slopes. With the rising of the groundwater level because of the fast recharge of irrigation water through loess fissures or sinkholes, the groundwater hydrodynamic field rapidly increases in slopes but the water level sharply drops after the discharge passes. The intense subsurface erosion makes holes inside the slopes, causing the upper slope to slump; therefore, series of landslides form along the loess plateau.Figure 4
Irrigation water infiltration mode.


## 2.3. Groundwater Level Rise Induced by Irrigation

The conceptual hydrogeological model for the Heifangtai tableland is that of a block between rivers (Figure5). In addition to irrigation, rainfall is the other groundwater recharge source. The mean annual precipitation is only 282.6 mm and the drought index is 5.6. The loess thicknesses in the Heifangtai area is about 20 m to 25 m [32]. Groundwater recharges as springs or seepages at the top of silty clay layers along the edges of the tableland. Because of the permeability differences between the conglomerate and silty clay layers, the groundwater moves in the conglomerate beds without any water pressure build-up [33]. Sporadic phreatic water occurs in the Cretaceous bedrock fissures. Based on numerical modelling of groundwater, the groundwater level is below the aquifer bottom in the east and west prior to irrigation and aquifer is unwatering. Large-scale irrigation started in 1968 and the groundwater level increased to 0.27 m/a, and at the center of the tableland was 0.57 m/a before 1990. After 1990, the rate gradually slowed to about 0.25 m/a, and the cumulative rise was 20 m up to 2010. It is predicted that the cumulative rise will reach 25 m in 2020 [33].Figure 5
The hydrogeological model for the Heifangtai tableland.


## 2.4. Geological Hazards Induced by Irrigation in the Heifangtai Tableland

The Heifangtai tableland has more than 40 years of irrigation by pumping and traditional broad irrigation, which induces various geological hazards including loess landslides groups and collapse of entire tableland. According to incomplete statistics, about 120 landslides have occurred (Figure6). Consequently, irrigation canals, farmland, roads, and other facilities have been damaged as well as loss of electricity or water, traffic disruption, and heavy casualties have occurred. Landslides have resulted in about 39 deaths, 100 injuries and the relocation of 950 families, five schools, and 13 businesses. According to the official statistics, 200 km2 of farmland have been abandoned with direct economic losses of more than 2 × 108 RMB and unaccounted indirect economic losses. The maximum loess collapse is up to 5.96 m. Furthermore, the numerous collapse fissures, depressions, funnel-shaped sinkholes, and subsurface erosion along the edges of tableland incurred more than 2 km2 farmland loss. Water conservation structures are often seriously damaged, including residence in the villages of Xinyuan, Zhuwang, Chenjia, and Fangtai. Consequently, the local population had to relocate and build new houses every few years. Every family has refurbishment for twice a year, even five or six a year, intensifying the economic burden on residents and the local social contradictions.Figure 6
Loess landslide statistics of Heifangtai tableland from 1980 to now.


## 3. Research Methods

### 3.1. Unsaturated Loess Test

The analysis of saturated and unsaturated seepage requires knowing the soil–water characteristic curve and the coefficient of permeability of unsaturated soil. The mechanical behaviour of unsaturated soil and the water characteristics are closely related with the soil–water characteristic curve [34]. Measurements of the soil–water characteristic test is on TRIM (soil–water characteristic fast measurement); the curves and the Hydrus-1D program were used to process moisture absorption data based on the Van Genuchten, Mualem, and suction stress models. The soil–water curve (Figure 7) for moisture absorption and dehumidification and the coefficient of the permeability function curve (HTC) were obtained [35].Figure 7
The soil–water curve for moisture absorption and dehumidification and the coefficient of the permeability function curve (HTC).The unsaturated strength of the Heifangtai loess was obtained by unsaturated triaxial shear tests in a GDS device with controlled matrix suction. Based on the Fredlund’s shear strength model [36, 37], shear strength of unsaturated loess is given by(1)τf=19.0+σ−uatan16.2°+ua−uwtan15.1°,where τf is the shear strength, σ is the principal stress, ua is the pore gas pressure, and uw is the pore water pressure.Figure8 shows the Mohr circles for matrix suction of 50 kPa and 100 kPa. Based on Figure 8, the effective cohesion of loess is 14.5 kPa, effective internal friction angle is 16.8°, and suction friction angle is 15.1°.Figure 8
The Mohr circles of shear strength of unsaturated loess.


### 3.2. Numerical Simulation

The Jiaojiayatou landslide 13 was analysed to understand the slope stability under irrigation. The strata in the slope are Qp3 loess, Qp2 alluvial deposits, and the interface of Cretaceous sandstone and mudstone (Figure 9). The model parameters are shown in Table 2. Based on the engineering geological profile, we built the saturated–unsaturated finite-element model in Figure 10. The model height is 80 m and the width is 135 m at the top and 223 m at the bottom. The bottom is horizontal and constrained on both sides, but the surface is free. The water level is fixed at the left; that is, a waterhead is set on the left to simulate the groundwater level under different irrigation conditions. The bottom is the confining boundary, and the slope surface is the seepage surface boundary.Figure 9
Engineering geological profile of landslide (1: loess; 2: silty clay; 3: sand and gravel; and 4: sandy mudstone interbedding).Table 2
Material parameters of the model [1, 2].
TitleWeightρ/kN (m3)Elasticity modulusE (MPa)Poisson’s ratioμPorosityPermeability coefficient (m/d)Cohesionc (kPa)Internal friction angleφ (°)Suction friction angleφb (°)VerticalHorizonalLoess15.2460.350.510.122.4e − 214.516.815.1Silty clay19.5900.30.302e − 42e − 460.022.0—Sand and gravel20.01400.30.402.02.0———Sandy mudstone interbedding22.02000.30.101e − 51e − 5———Figure 10
The calculation model (① loess; ② silty clay; ③ sand and gravel; ④ sandy mudstone interbedding; and ⑤,⑥, and ⑦ the distance between the fracture location and the edge of the pier is 5 m, 15 m, and 33 m).In general, soil intensity under the groundwater level uses saturated intensity in slope stability analysis, and that above the groundwater level uses shear strength at natural water content or plastic limit water content. But partly shear strength induced by the negative pore pressure under the groundwater level is usually ignored. It is unreasonable for the landslides at which the sliding surface above the groundwater level because soil intensity and matric suction drop when groundwater level increases. Therefore, matrix suction distribution in the slope and shear strength of unsaturated soil should be considered during the slope stability analysis. The paper takes unsaturated theory to study the problem. FLAC3D is used in stability calculation program, the function of unsaturated stability analysis is developed through FISH programming language of FLAC3D software, filled in the lacuna of unsaturated seepage analysis and the properties of unsaturated materials.


## 3.1. Unsaturated Loess Test

The analysis of saturated and unsaturated seepage requires knowing the soil–water characteristic curve and the coefficient of permeability of unsaturated soil. The mechanical behaviour of unsaturated soil and the water characteristics are closely related with the soil–water characteristic curve [34]. Measurements of the soil–water characteristic test is on TRIM (soil–water characteristic fast measurement); the curves and the Hydrus-1D program were used to process moisture absorption data based on the Van Genuchten, Mualem, and suction stress models. The soil–water curve (Figure 7) for moisture absorption and dehumidification and the coefficient of the permeability function curve (HTC) were obtained [35].Figure 7
The soil–water curve for moisture absorption and dehumidification and the coefficient of the permeability function curve (HTC).The unsaturated strength of the Heifangtai loess was obtained by unsaturated triaxial shear tests in a GDS device with controlled matrix suction. Based on the Fredlund’s shear strength model [36, 37], shear strength of unsaturated loess is given by(1)τf=19.0+σ−uatan16.2°+ua−uwtan15.1°,where τf is the shear strength, σ is the principal stress, ua is the pore gas pressure, and uw is the pore water pressure.Figure8 shows the Mohr circles for matrix suction of 50 kPa and 100 kPa. Based on Figure 8, the effective cohesion of loess is 14.5 kPa, effective internal friction angle is 16.8°, and suction friction angle is 15.1°.Figure 8
The Mohr circles of shear strength of unsaturated loess.


## 3.2. Numerical Simulation

The Jiaojiayatou landslide 13 was analysed to understand the slope stability under irrigation. The strata in the slope are Qp3 loess, Qp2 alluvial deposits, and the interface of Cretaceous sandstone and mudstone (Figure 9). The model parameters are shown in Table 2. Based on the engineering geological profile, we built the saturated–unsaturated finite-element model in Figure 10. The model height is 80 m and the width is 135 m at the top and 223 m at the bottom. The bottom is horizontal and constrained on both sides, but the surface is free. The water level is fixed at the left; that is, a waterhead is set on the left to simulate the groundwater level under different irrigation conditions. The bottom is the confining boundary, and the slope surface is the seepage surface boundary.Figure 9
Engineering geological profile of landslide (1: loess; 2: silty clay; 3: sand and gravel; and 4: sandy mudstone interbedding).Table 2
Material parameters of the model [1, 2].
TitleWeightρ/kN (m3)Elasticity modulusE (MPa)Poisson’s ratioμPorosityPermeability coefficient (m/d)Cohesionc (kPa)Internal friction angleφ (°)Suction friction angleφb (°)VerticalHorizonalLoess15.2460.350.510.122.4e − 214.516.815.1Silty clay19.5900.30.302e − 42e − 460.022.0—Sand and gravel20.01400.30.402.02.0———Sandy mudstone interbedding22.02000.30.101e − 51e − 5———Figure 10
The calculation model (① loess; ② silty clay; ③ sand and gravel; ④ sandy mudstone interbedding; and ⑤,⑥, and ⑦ the distance between the fracture location and the edge of the pier is 5 m, 15 m, and 33 m).In general, soil intensity under the groundwater level uses saturated intensity in slope stability analysis, and that above the groundwater level uses shear strength at natural water content or plastic limit water content. But partly shear strength induced by the negative pore pressure under the groundwater level is usually ignored. It is unreasonable for the landslides at which the sliding surface above the groundwater level because soil intensity and matric suction drop when groundwater level increases. Therefore, matrix suction distribution in the slope and shear strength of unsaturated soil should be considered during the slope stability analysis. The paper takes unsaturated theory to study the problem. FLAC3D is used in stability calculation program, the function of unsaturated stability analysis is developed through FISH programming language of FLAC3D software, filled in the lacuna of unsaturated seepage analysis and the properties of unsaturated materials.


## 4. Results and Discussion

### 4.1. Seepage Characteristics in Slope under Uniform Infiltration

The groundwater level rise is slow; therefore, steady flow is used and different groundwater levels are used to simulate the seepage owing to irrigation. The phreatic water in the loess is 31–56 m. The loess layer is dry when the groundwater level is lower than that of the aquifer prior to irrigation. We calculate the saturated and unsaturated seepage and then the pore pressure distribution in the slope (Figure11).Figure 11
The distribution of pore pressure of different groundwater level. (a) 31 m. (b) 36 m. (c) 41 m. (d) 46 m. (e) 51 m. (f) 56 m.
(a)(b)(c)(d)(e)(f)At the beginning of irrigation, there is no stable groundwater level in the loess and the isoline of the pore pressure is nearly horizontal (Figure11(a)). The groundwater level rises with increasing irrigation and irrigation time, which causes the bottom of the loess to become saturated and the groundwater to flow slowly from the inner saturated zone to the unsaturated zone under the influence of matrix suction. The velocity of the increase in pore pressure in the slope is greater than that horizontally and pore pressure is decreased. With increasing groundwater level, the water content in the unsaturated zone increases, and the pore pressure in the unsaturated zone and the saturated area increases as well. In addition, the hydraulic gradient in the slope and the seepage velocity increases, which increases the water flow at the slope and decreases the slope stability.Figure12 shows the distribution curves of the matrix suction in the slope under different groundwater levels. Figure 12(a) shows that the groundwater level rises in the slope with rising groundwater level, whereas the matrix suction decreases linearly with respect to the water table. Based on the shear strength model of Fredlund, the decrease in matrix suction decreases the shear strength and thus the slope stability also decreases.Figure 12
The relationship between groundwater and matric suction. (a) 0 kPa. (b) 50 kPa. (c) 100 kPa. (d) 200 kPa.
(a)(b)(c)(d)


### 4.2. Seepage in Slope under Infiltration

First, the method of unsteady flow is adopted to calculate the seepage inside the slope with different fracture locations. Figure13 shows the distribution of pore water pressure at 33 m, 15 m, and 5 m, respectively, which is the distance between the fracture location and the edge of the pier after 60 days. A channel forms near the fracture because the pore water pressure increases as irrigation water seeps through. With time, the pore water pressure increases 2 m around the fracture and a saturated zone forms locally. In addition, the closer the fracture is to the edge of the platform, the higher the pore pressure is when the water seepage flows into the potential sliding surface.Figure 13
Distribution of pore pressure (kPa) in the slope body at different fissure locations. (a), (b), and (c) The distance between the fracture location and the edge of the pier is 33 m, 15 m, and 5 m.
(a)(b)(c)The matrix suction varies greatly; inside the slope, it is almost constant, whereas near the fracture, it decreases significantly (Figure14). A large amount of water is injected into the fissure and causes the soil recharge near the fissure to increase dramatically. The permeability of loess is low and there is no obvious upward movement of the groundwater level in the slope but an obvious saturation zone forms in the fissure based on the groundwater level line at matrix suction of 0 kPa.Figure 14
Distribution curve of matric suction (kPa) in the slope at different fissure locations. (a), (b), and (c) The distance between the fracture location and the edge of the pier is 33 m, 15 m, and 5 m.
(a)(b)(c)Figure15 shows the distribution of pore water pressure inside the slope at different fractures after 60 days of flooding. The increase in the number of fissures increases the pore water pressure in the fractured area. The fractures little affect the groundwater level (0 kPa contour line) based on the distribution of matrix suction as a function of the different number of cracks (Figure 16). This is due to the poor permeability of the loess; however, the pore water pressure near the fissure increases rapidly and a saturated zone forms as the seepage flow in loess and the infiltration of groundwater decreases. With increasing the number of fractures and loess collapsibility, sinkholes form in the area and then landslides are induced. This is due to the rapid decrease in slope stability over short time, whereas the infiltration of irrigation water and the water recharge in the surface soil increase fast.Figure 15
Distribution of pore pressure (kPa) in the slope body of different number of fissures ((a) two fissures; (b) three fissures; and (c) four fissures).
(a)(b)(c)Figure 16
Distribution curve of matric suction (kPa) in the slope of different number of fissures (a), (b), and (c) matric suction at 0 kPa, 50 kPa, and 200 kPa.
(a)(b)(c)


### 4.3. Mechanism of Loess Landslide Induced by Irrigation

Based on the laboratory test results and field monitoring, the loess landslide pattern induced by irrigation is shown in Figure17. Before irrigation (Figure 17(a)), the groundwater level is below the aquifer, which is unwatering with some exceptions in the low-lying areas in the middle of the tableland and a few fissures at the edges of the tableland. This is why such few landslides occur before irrigation.Figure 17
The failure mode of loess landslide induced by irrigation (1: loess; 2: silty clay; 3: sand and gravel; 4: sandy mudstone interbedding; 5: landslide deposits; 6: spring; and 7: groundwater level).At the beginning of irrigation, there is no stable groundwater level in the loess tableland and the pore pressure contours in the slope are horizontal. With increasing irrigation times, some areas develop migration pathways, such as fissures and sinkholes, owing to the loess collapsibility. The irrigated water rapidly recharges groundwater through preferential migration pathways (Figure17(b)) and the groundwater level rises, while the bottom of the loess becomes saturated (Figure 17(c)). The underground runoff slowly flows from the saturation zone to the unsaturated zone because of the matrix suction; furthermore, the increase in the pore pressure away from the edge of slope is faster than it is close to the edge and deflection of the pore pressure contours is seen. With rising groundwater level, the quantity flowing to the unsaturated zone and the pore pressure increase and, consequently, the saturation zone becomes larger (Figure 17(d)). The hydraulic gradient of the slope increases owing to the rising groundwater level and seepage velocity is thus greater than before. Because of the engineering properties of the loess, broad irrigation induces more fissures at the edge of the tableland, with many small saturation zones around the fissures. Thus, the loess strength decreases over time and latent sliding surfaces form near the slope edges (Figure 17(e)). When the saturation zone expands to a certain extent, the stability of the loess slope rapidly decreases and landslides occur (Figure 17(f)).Increased irrigation water infiltration through preferential migration pathways induces landslides in the Heifangtai tableland. The groundwater level rise leads to matrix suction and strength decreases and loess slope instability.


## 4.1. Seepage Characteristics in Slope under Uniform Infiltration

The groundwater level rise is slow; therefore, steady flow is used and different groundwater levels are used to simulate the seepage owing to irrigation. The phreatic water in the loess is 31–56 m. The loess layer is dry when the groundwater level is lower than that of the aquifer prior to irrigation. We calculate the saturated and unsaturated seepage and then the pore pressure distribution in the slope (Figure11).Figure 11
The distribution of pore pressure of different groundwater level. (a) 31 m. (b) 36 m. (c) 41 m. (d) 46 m. (e) 51 m. (f) 56 m.
(a)(b)(c)(d)(e)(f)At the beginning of irrigation, there is no stable groundwater level in the loess and the isoline of the pore pressure is nearly horizontal (Figure11(a)). The groundwater level rises with increasing irrigation and irrigation time, which causes the bottom of the loess to become saturated and the groundwater to flow slowly from the inner saturated zone to the unsaturated zone under the influence of matrix suction. The velocity of the increase in pore pressure in the slope is greater than that horizontally and pore pressure is decreased. With increasing groundwater level, the water content in the unsaturated zone increases, and the pore pressure in the unsaturated zone and the saturated area increases as well. In addition, the hydraulic gradient in the slope and the seepage velocity increases, which increases the water flow at the slope and decreases the slope stability.Figure12 shows the distribution curves of the matrix suction in the slope under different groundwater levels. Figure 12(a) shows that the groundwater level rises in the slope with rising groundwater level, whereas the matrix suction decreases linearly with respect to the water table. Based on the shear strength model of Fredlund, the decrease in matrix suction decreases the shear strength and thus the slope stability also decreases.Figure 12
The relationship between groundwater and matric suction. (a) 0 kPa. (b) 50 kPa. (c) 100 kPa. (d) 200 kPa.
(a)(b)(c)(d)


## 4.2. Seepage in Slope under Infiltration

First, the method of unsteady flow is adopted to calculate the seepage inside the slope with different fracture locations. Figure13 shows the distribution of pore water pressure at 33 m, 15 m, and 5 m, respectively, which is the distance between the fracture location and the edge of the pier after 60 days. A channel forms near the fracture because the pore water pressure increases as irrigation water seeps through. With time, the pore water pressure increases 2 m around the fracture and a saturated zone forms locally. In addition, the closer the fracture is to the edge of the platform, the higher the pore pressure is when the water seepage flows into the potential sliding surface.Figure 13
Distribution of pore pressure (kPa) in the slope body at different fissure locations. (a), (b), and (c) The distance between the fracture location and the edge of the pier is 33 m, 15 m, and 5 m.
(a)(b)(c)The matrix suction varies greatly; inside the slope, it is almost constant, whereas near the fracture, it decreases significantly (Figure14). A large amount of water is injected into the fissure and causes the soil recharge near the fissure to increase dramatically. The permeability of loess is low and there is no obvious upward movement of the groundwater level in the slope but an obvious saturation zone forms in the fissure based on the groundwater level line at matrix suction of 0 kPa.Figure 14
Distribution curve of matric suction (kPa) in the slope at different fissure locations. (a), (b), and (c) The distance between the fracture location and the edge of the pier is 33 m, 15 m, and 5 m.
(a)(b)(c)Figure15 shows the distribution of pore water pressure inside the slope at different fractures after 60 days of flooding. The increase in the number of fissures increases the pore water pressure in the fractured area. The fractures little affect the groundwater level (0 kPa contour line) based on the distribution of matrix suction as a function of the different number of cracks (Figure 16). This is due to the poor permeability of the loess; however, the pore water pressure near the fissure increases rapidly and a saturated zone forms as the seepage flow in loess and the infiltration of groundwater decreases. With increasing the number of fractures and loess collapsibility, sinkholes form in the area and then landslides are induced. This is due to the rapid decrease in slope stability over short time, whereas the infiltration of irrigation water and the water recharge in the surface soil increase fast.Figure 15
Distribution of pore pressure (kPa) in the slope body of different number of fissures ((a) two fissures; (b) three fissures; and (c) four fissures).
(a)(b)(c)Figure 16
Distribution curve of matric suction (kPa) in the slope of different number of fissures (a), (b), and (c) matric suction at 0 kPa, 50 kPa, and 200 kPa.
(a)(b)(c)


## 4.3. Mechanism of Loess Landslide Induced by Irrigation

Based on the laboratory test results and field monitoring, the loess landslide pattern induced by irrigation is shown in Figure17. Before irrigation (Figure 17(a)), the groundwater level is below the aquifer, which is unwatering with some exceptions in the low-lying areas in the middle of the tableland and a few fissures at the edges of the tableland. This is why such few landslides occur before irrigation.Figure 17
The failure mode of loess landslide induced by irrigation (1: loess; 2: silty clay; 3: sand and gravel; 4: sandy mudstone interbedding; 5: landslide deposits; 6: spring; and 7: groundwater level).At the beginning of irrigation, there is no stable groundwater level in the loess tableland and the pore pressure contours in the slope are horizontal. With increasing irrigation times, some areas develop migration pathways, such as fissures and sinkholes, owing to the loess collapsibility. The irrigated water rapidly recharges groundwater through preferential migration pathways (Figure17(b)) and the groundwater level rises, while the bottom of the loess becomes saturated (Figure 17(c)). The underground runoff slowly flows from the saturation zone to the unsaturated zone because of the matrix suction; furthermore, the increase in the pore pressure away from the edge of slope is faster than it is close to the edge and deflection of the pore pressure contours is seen. With rising groundwater level, the quantity flowing to the unsaturated zone and the pore pressure increase and, consequently, the saturation zone becomes larger (Figure 17(d)). The hydraulic gradient of the slope increases owing to the rising groundwater level and seepage velocity is thus greater than before. Because of the engineering properties of the loess, broad irrigation induces more fissures at the edge of the tableland, with many small saturation zones around the fissures. Thus, the loess strength decreases over time and latent sliding surfaces form near the slope edges (Figure 17(e)). When the saturation zone expands to a certain extent, the stability of the loess slope rapidly decreases and landslides occur (Figure 17(f)).Increased irrigation water infiltration through preferential migration pathways induces landslides in the Heifangtai tableland. The groundwater level rise leads to matrix suction and strength decreases and loess slope instability.


## 5. Conclusions

We studied the landslide mechanism induced by irrigation in loess, using the Heifangtai tableland as the study area. The main conclusions are the following:First, agriculture in arid and semiarid regions mainly relies on irrigation. Traditional broad irrigation wastes fresh water; moreover, irrigation water infiltration and preferential migration pathways change the hydrogeological conditions in the irrigated areas and induce landslides, collapses, and mudflows.Second, the groundwater level is below the aquifer before irrigation. Moreover, after long-term broad irrigation, the groundwater level rise decreases the loess matrix suction and strength and increases the loess slope instability.Finally, based on the loess landslide mechanism induced by irrigation in arid and semiarid regions, countermeasures are proposed. First, the traditional broad irrigation with water-saving irrigation methods should be replaced. Second, more drought-resistant crops should be planted. Third, the groundwater level should be lowered. Fourth, monitoring and early warning of loess landslides in the main growth area should be intensified.Geological hazards, such as landslides, collapses, and soil salinization, are induced by outdated irrigation methods, such as broad irrigation and oven filling. Based on the loess landslide mechanism induced by irrigation in arid and semiarid regions, four countermeasures are proposed. Firstly, replace the traditional broad irrigation by water-saving irrigation methods, such as trickle irrigation. Secondly, drought-resistant crops that require less water should be planted. Thirdly, lower the groundwater level. Fourthly, intensify monitoring and early warning in the central growth area.



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*Source: 8859166-2020-11-23.xml*