# Formation Mechanism and Stability Analysis of the Hejia Landslide

Authors: Hao Zhang; Zaiqiang Hu; Xingzhou Chen; Hongru Li
Journal: Advances in Materials Science and Engineering
 (2021)

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## Abstract

The existing research data show that, after reservoir impoundment, due to the repeated rise and fall of water level and water-rock interaction, the mechanical parameters of landslide are reduced, which will have an adverse effect on the stability of landslide. Therefore, sufficient attention must be paid to the stability of slope after reservoir impoundment. Hejia landslide is the largest landslide near the bank of Miaojiaba hydropower station, and its stability plays an important role in the normal operation of the hydropower station. Through field investigation and analysis of regional geological conditions, it is concluded that Hejia landslide is a large-scale landslide, through long-term sliding-bending deformation; it is generated from the external hard rock with thick layers and sliding zone for layered soft rock; the formation mechanism of landslide is as follows: (1) high-steep and hard-soft layered slope is the slope structure condition that caused the large landslide; (2) the existence of thick soft rock belt provides material conditions for the formation of slip surface; (3) certain air conditions provide displacement space for the separation and disintegration of the sliding body, and the landslide is stable at present. Numerical analysis results show that reservoir impoundment will adversely affect the stability of landslide. In order to ensure the normal operation of power station, certain engineering measures must be taken to treat Hejia landslide. After taking measures, years of monitoring data show that the deformation of Hejia landslide tends to be stable, and the current operation is normal, indicating that the engineering treatment measures are reasonable and feasible.


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## Body

## 1. Introduction

Over the past 20 years, most hydropower stations in China have been constructed in the western mountains and valleys with harsh natural conditions, poor geological conditions, and broken rock masses. In the reservoir area, unfavorable geologic bodies such as landslide and toppling mass are widely distributed. If improperly treated, they will have an adverse effect on the construction and operation of the hydropower stations. There were landslides in the Longyangxia Hydropower Station [1], Lijiaxia Hydropower Station [2], Manwan Hydropower Station [3], and Laxiwa Hydropower Station [4] after their completion and operation. Although these landslides did not cause harm to the major buildings, the repair was expensive. Therefore, during the construction of hydropower stations, we need to pay close attention to the slope safety.Previous studies worldwide have focused on how the changes of reservoir water level will influence the landslide. Yi et al. [5] investigated the formation mechanism of Tang Gudong landslide. Dai [6] studied the deformation and the loss of stability of the large landslide in Ou’tang near the Three Gorges Reservoir. Yuan et al. [7] established a multistage filling slope model by using PLAXIS finite element software and conducted sensitivity analysis and stability analysis on the slope under different working conditions. Guo [8], Yu [9], and Wei [10] studied the deformation and stability of rock slope under water level fluctuations. Yuan et al. [11] proposed a parameter index to quantify the effect of residual soil reinforcement based on the equivalent confining pressure, which can provide reference for the safe operation of retaining wall and slope. Wu [12] studied the deformation of the landslide in the upper reaches of the Minjiang River. Xiao et al. [13] conducted a model test to study slope deformation under rainfall and the variation of reservoir water level. Based on the theory of rainfall infiltration, Yuan et al. [14] established the surface infiltration model of multilevel filled slope by using the SEEP/W module of GeoStudio. The influence of the change of the rainfall conditions on the VWC and PWP was considered. He et al. [15] analyzed the stability of slope under the change of water level. Yang et al. [16] studied the seepage lag of landslide accumulation with the fluctuation of reservoir water level. According to previous studies, the water storage of the reservoir may threaten the slope stability because it causes the physical and chemical reactions in the slope, deteriorates the physical and mechanical properties of the rock and soil bodies, and destroys the original seepage field and the stress field of the slope. To control flood and generate power, large hydropower stations have to frequently change the water level of the reservoir during the operation, which greatly affects the slope stability.This paper studied the formation mechanism of the landslide in the reservoir area of a hydropower station in southwest China. Backed by results from the field survey and analysis of regional geology, it carried out a numerical analysis of the landslide stability to provide basis for engineering design.


## 2. Overview of the Landslide

### 2.1. Topography of the Landslide

The hydropower station is located in a canyon area of western China, where landslides and deformation bodies extremely develop. The largest landslide is situated on the left bank, approximately 600 m upstream of the dam site. It can be categorized as a super large landslide as its longitudinal length is 80∼900 m and its horizontal width is 360∼400 m. The diamond-shaped landslide has an area of 0.34 km2, with average thickness longer than 57 m and a volume of 2,350 × 104 m3. The slope was gentle in the upper part and steep in the lower part, with angles of 24∼30° in the upper, 34° in the middle, and 41° in the lower. There are two gullies developed in the sliding mass without cutting through it. They are 550∼600 m long, 20∼40 m deep, and 2∼6 m wide at the bottom. The leading edge, with an elevation of 800∼810 m, was 90∼100 m above the river level; the trailing edge, with an elevation of 1,450 m, had an obvious 200 m high triangular rupture wall, as shown in Figure 1.Figure 1
General view of the Hejia landslide.


### 2.2. Structural Characteristics of the Landslide

#### 2.2.1. Lithology and Structure of the Landslide

The Hejia landslide develops in Changchengian Bikou Group metamorphic rocks interbedded with tuff and slate. The field survey suggests that the trailing edge of the landslide and the downstream area consist of argillite; the upstream boundary is dominated by metamorphic tuff and the leading edge of the landslide comprises thick-layered metamorphic tuff (Figure2). Figure 2 shows that the upper sliding bed and the rock mass beneath it consist of argillite, the lower surface of the landslide comprises tuff, and the lower sliding bed is dominated by argillite.Figure 2
Geological plan of the Hejia landslide.


#### 2.2.2. Composition of the Landslide Surface

According to the field survey, the composition of the landslide surface is as follows:(1)
The trailing edge and the surface layer consist of loess.(2)
The section in the trailing edge consists of disintegrated slate gravel and rock. The downstream sliding mass contains slate gravel and rock with plate and sheet shapes.(3)
The upstream boundary comprises massive tuff rocks.(4)
The rock-layer reverse in the leading edge mainly contains small slate gravel as well as mud-like slate or sheets of slate. They are formed by the rolling up of slate near the slip zone.(5)
The sliding mass had partition characteristics and can be divided into the downstream partition (partition II) and the upstream partition (partition I). The partition map of the Hejia landslide is shown in Figure3. Composed of slate gravel, partition I is 2∼3 times wider than partition II, which mainly contains tuff and partly disintegrated slate.Figure 3
Partition map of the Hejia landslide.


#### 2.2.3. Internal Structure of the Sliding Mass

Figure4 is the typical geological profile of the Hejia landslide. The sliding mass can be categorized into 6 zones based on differences in composition. (i)
The loess zone on the surface of the slip band is mainly distributed in the gentle slope of the trailing edge at elevations higher than 1,200 m.(ii)
The gravel, rock, and layered rock zone are in the shallow surface of the sliding mass. This zone is mainly distributed in the shallow surface of the sliding mass below 1,200 m elevation. It is composed of gravel and rock formed by the landslide. The zone at the middle part of the sliding mass is the most deformed. Although the patent rock, metamorphic tuff, and arenaceous argillite have decomposed into gravel and rock, the sequence structure of primary rock is still visible (Figure5). The zone at the front part of the sliding mass consists mainly of badly decomposed primary rock, with much narrow diameters of 0.3∼1 m and more fine grain materials can be found (Figure 6).The lateral gullies of the partition II cut deep inside the sliding mass. Some of the gullies even cut through the sliding mass. The materials exposed on the gully bank are layered metamorphic tuff and arenaceous argillite. Their size depends on the thickness of the single layer of the parent rock. These rocks accumulate and are supported on stilts. Compared with the occurrence of the bedrock, the layered rock in the partition II has changed more. The change was caused by landslide movement. When the landslide occurred, rocks cut by the bedding plane and the structural plane in the sliding mass had uncoordinated displacement, so they separated or squeezed each other. As a result, the occurrence of layered rock in the partition II changed more (Figure7).(iii)
The zone of residual layered rocks and large rocks is distributed in the middle and shallow parts of the sliding mass. This zone is composed of metamorphic tuff gravel and rock. As revealed by the adits PD1 and PD3, the horizontal thickness of zone is 60∼65 m. The parent rock is gray-green medium-thick metamorphic tuff. The diameter of residual layered rocks and large rocks in the zone varies greatly from 20∼30 cm to over 3 m. Most rocks are about 1 m. The zone has a loose structure without fine-grained material filling inside.(iv)
The middle and deep parts of the landslide mass still retain the layered structure. This zone is about 40∼45 m thick and the single layer of the residual rock is 30∼40 cm thick. The dip direction of this zone is 200°∼225°, close to that of the bedrock. However, the dip angle of the rock stratum has changed 40°∼71°, which is a large variation. Although the layered remnants of the parent rock are relatively complete, the zone still contains the characteristics of displacement, dislocation, fracture, and separation along the bedding plane and the structural plane.⑤
The highly folded zone of argillite: the first 5∼10 m of the zone mainly consists of breccia and rock dust. There are also some scattered gravel and rock and a few magenta argillaceous materials. The lower part is a strongly crumpled stratum composed of arenaceous and argillaceous slate. It has developed asymmetric recumbent folds, with local ruptures. The stratum is tightly compressed without any fracture or overhead and the axial plane dips inside the slope.⑥
The slip zone: this zone is about 6∼9 m thick and is composed of grayish white rock dust and yellow dark brown argillaceous material. It also contains breccia, which is compact, wet, and sandy, with a particle diameter of 0.3∼1 cm. The sliding surface is 133 m away from the adit PD1 and 162 m away from the adit PD3. The sliding bed is composed of fine-grained tuffaceous slate. The single rock layer is 2∼3 cm thick and the rock structure is relatively intact, with an occurrence of 191∼202∠43∼52°, the same as the sliding surface.Figure 4
Typical geological profile of the Hejia landslide.Figure 5
Gravel and rock retaining the sequence structure of primary rock in partition I at 960∼1,200 m.Figure 6
Composition of the front of the sliding mass in partition I.Figure 7
Material composition of the sliding mass in partition II.Different parts of the slip zone revealed by the exploration adits have good correspondence in occurrence, location, thickness, and composition properties. Therefore, it can be concluded that the slip zone has a unified main sliding surface composed of a single rock stratum (interbedded and compressed). Moreover, as the branch sections in the three adits at different elevations show almost the same characteristics of the main sliding mass, and the five zones of different materials, from the surface to the center, have good correspondence in terms of extension, direction, thickness, and state, the possibility of multilevel sliding masses existing inside the main sliding mass can be ruled out.


### 2.3. Deformation Characteristics of the Landslide

#### 2.3.1. Deformation Characteristics of the Trailing Edge

There is a 20° gentle slope in the trailing edge of the Hejia landslide. The wide slope is covered by 10∼20 m thick loess. According to the field survey, this slope does not have step-like terrain, indicating that the trailing edge has never been greatly deformed in history. This is confirmed by the lush vegetation and tall trees. The sliding mass has a length of over 800 m. Controlled by the residual layered structure of the sliding mass, the slope surface is roughly consistent with the residual layered surface. The field survey showed that the slope was relatively straight without large steps.


#### 2.3.2. Deformation Characteristics of the Sliding Mass

The sliding mass has a length of over 800 m. Controlled by the residual layered structure of the sliding mass, the slope surface is roughly consistent with the residual layered surface. If there was a large deformation, a step-like terrain would appear. The field survey showed that the sliding mass was relatively straight without large steps.


#### 2.3.3. Deformation Characteristics near the Sliding Zone

For exploration, the adits of the Hejia landslide were first excavated in 1990. The field survey in 2009 suggested that the main adits retained their original shape without any supports [17]. This suggested that the sliding mass composed of slate near the sliding zone had good integrity and tightness.


## 2.1. Topography of the Landslide

The hydropower station is located in a canyon area of western China, where landslides and deformation bodies extremely develop. The largest landslide is situated on the left bank, approximately 600 m upstream of the dam site. It can be categorized as a super large landslide as its longitudinal length is 80∼900 m and its horizontal width is 360∼400 m. The diamond-shaped landslide has an area of 0.34 km2, with average thickness longer than 57 m and a volume of 2,350 × 104 m3. The slope was gentle in the upper part and steep in the lower part, with angles of 24∼30° in the upper, 34° in the middle, and 41° in the lower. There are two gullies developed in the sliding mass without cutting through it. They are 550∼600 m long, 20∼40 m deep, and 2∼6 m wide at the bottom. The leading edge, with an elevation of 800∼810 m, was 90∼100 m above the river level; the trailing edge, with an elevation of 1,450 m, had an obvious 200 m high triangular rupture wall, as shown in Figure 1.Figure 1
General view of the Hejia landslide.


## 2.2. Structural Characteristics of the Landslide

### 2.2.1. Lithology and Structure of the Landslide

The Hejia landslide develops in Changchengian Bikou Group metamorphic rocks interbedded with tuff and slate. The field survey suggests that the trailing edge of the landslide and the downstream area consist of argillite; the upstream boundary is dominated by metamorphic tuff and the leading edge of the landslide comprises thick-layered metamorphic tuff (Figure2). Figure 2 shows that the upper sliding bed and the rock mass beneath it consist of argillite, the lower surface of the landslide comprises tuff, and the lower sliding bed is dominated by argillite.Figure 2
Geological plan of the Hejia landslide.


### 2.2.2. Composition of the Landslide Surface

According to the field survey, the composition of the landslide surface is as follows:(1)
The trailing edge and the surface layer consist of loess.(2)
The section in the trailing edge consists of disintegrated slate gravel and rock. The downstream sliding mass contains slate gravel and rock with plate and sheet shapes.(3)
The upstream boundary comprises massive tuff rocks.(4)
The rock-layer reverse in the leading edge mainly contains small slate gravel as well as mud-like slate or sheets of slate. They are formed by the rolling up of slate near the slip zone.(5)
The sliding mass had partition characteristics and can be divided into the downstream partition (partition II) and the upstream partition (partition I). The partition map of the Hejia landslide is shown in Figure3. Composed of slate gravel, partition I is 2∼3 times wider than partition II, which mainly contains tuff and partly disintegrated slate.Figure 3
Partition map of the Hejia landslide.


### 2.2.3. Internal Structure of the Sliding Mass

Figure4 is the typical geological profile of the Hejia landslide. The sliding mass can be categorized into 6 zones based on differences in composition. (i)
The loess zone on the surface of the slip band is mainly distributed in the gentle slope of the trailing edge at elevations higher than 1,200 m.(ii)
The gravel, rock, and layered rock zone are in the shallow surface of the sliding mass. This zone is mainly distributed in the shallow surface of the sliding mass below 1,200 m elevation. It is composed of gravel and rock formed by the landslide. The zone at the middle part of the sliding mass is the most deformed. Although the patent rock, metamorphic tuff, and arenaceous argillite have decomposed into gravel and rock, the sequence structure of primary rock is still visible (Figure5). The zone at the front part of the sliding mass consists mainly of badly decomposed primary rock, with much narrow diameters of 0.3∼1 m and more fine grain materials can be found (Figure 6).The lateral gullies of the partition II cut deep inside the sliding mass. Some of the gullies even cut through the sliding mass. The materials exposed on the gully bank are layered metamorphic tuff and arenaceous argillite. Their size depends on the thickness of the single layer of the parent rock. These rocks accumulate and are supported on stilts. Compared with the occurrence of the bedrock, the layered rock in the partition II has changed more. The change was caused by landslide movement. When the landslide occurred, rocks cut by the bedding plane and the structural plane in the sliding mass had uncoordinated displacement, so they separated or squeezed each other. As a result, the occurrence of layered rock in the partition II changed more (Figure7).(iii)
The zone of residual layered rocks and large rocks is distributed in the middle and shallow parts of the sliding mass. This zone is composed of metamorphic tuff gravel and rock. As revealed by the adits PD1 and PD3, the horizontal thickness of zone is 60∼65 m. The parent rock is gray-green medium-thick metamorphic tuff. The diameter of residual layered rocks and large rocks in the zone varies greatly from 20∼30 cm to over 3 m. Most rocks are about 1 m. The zone has a loose structure without fine-grained material filling inside.(iv)
The middle and deep parts of the landslide mass still retain the layered structure. This zone is about 40∼45 m thick and the single layer of the residual rock is 30∼40 cm thick. The dip direction of this zone is 200°∼225°, close to that of the bedrock. However, the dip angle of the rock stratum has changed 40°∼71°, which is a large variation. Although the layered remnants of the parent rock are relatively complete, the zone still contains the characteristics of displacement, dislocation, fracture, and separation along the bedding plane and the structural plane.⑤
The highly folded zone of argillite: the first 5∼10 m of the zone mainly consists of breccia and rock dust. There are also some scattered gravel and rock and a few magenta argillaceous materials. The lower part is a strongly crumpled stratum composed of arenaceous and argillaceous slate. It has developed asymmetric recumbent folds, with local ruptures. The stratum is tightly compressed without any fracture or overhead and the axial plane dips inside the slope.⑥
The slip zone: this zone is about 6∼9 m thick and is composed of grayish white rock dust and yellow dark brown argillaceous material. It also contains breccia, which is compact, wet, and sandy, with a particle diameter of 0.3∼1 cm. The sliding surface is 133 m away from the adit PD1 and 162 m away from the adit PD3. The sliding bed is composed of fine-grained tuffaceous slate. The single rock layer is 2∼3 cm thick and the rock structure is relatively intact, with an occurrence of 191∼202∠43∼52°, the same as the sliding surface.Figure 4
Typical geological profile of the Hejia landslide.Figure 5
Gravel and rock retaining the sequence structure of primary rock in partition I at 960∼1,200 m.Figure 6
Composition of the front of the sliding mass in partition I.Figure 7
Material composition of the sliding mass in partition II.Different parts of the slip zone revealed by the exploration adits have good correspondence in occurrence, location, thickness, and composition properties. Therefore, it can be concluded that the slip zone has a unified main sliding surface composed of a single rock stratum (interbedded and compressed). Moreover, as the branch sections in the three adits at different elevations show almost the same characteristics of the main sliding mass, and the five zones of different materials, from the surface to the center, have good correspondence in terms of extension, direction, thickness, and state, the possibility of multilevel sliding masses existing inside the main sliding mass can be ruled out.


## 2.2.1. Lithology and Structure of the Landslide

The Hejia landslide develops in Changchengian Bikou Group metamorphic rocks interbedded with tuff and slate. The field survey suggests that the trailing edge of the landslide and the downstream area consist of argillite; the upstream boundary is dominated by metamorphic tuff and the leading edge of the landslide comprises thick-layered metamorphic tuff (Figure2). Figure 2 shows that the upper sliding bed and the rock mass beneath it consist of argillite, the lower surface of the landslide comprises tuff, and the lower sliding bed is dominated by argillite.Figure 2
Geological plan of the Hejia landslide.


## 2.2.2. Composition of the Landslide Surface

According to the field survey, the composition of the landslide surface is as follows:(1)
The trailing edge and the surface layer consist of loess.(2)
The section in the trailing edge consists of disintegrated slate gravel and rock. The downstream sliding mass contains slate gravel and rock with plate and sheet shapes.(3)
The upstream boundary comprises massive tuff rocks.(4)
The rock-layer reverse in the leading edge mainly contains small slate gravel as well as mud-like slate or sheets of slate. They are formed by the rolling up of slate near the slip zone.(5)
The sliding mass had partition characteristics and can be divided into the downstream partition (partition II) and the upstream partition (partition I). The partition map of the Hejia landslide is shown in Figure3. Composed of slate gravel, partition I is 2∼3 times wider than partition II, which mainly contains tuff and partly disintegrated slate.Figure 3
Partition map of the Hejia landslide.


## 2.2.3. Internal Structure of the Sliding Mass

Figure4 is the typical geological profile of the Hejia landslide. The sliding mass can be categorized into 6 zones based on differences in composition. (i)
The loess zone on the surface of the slip band is mainly distributed in the gentle slope of the trailing edge at elevations higher than 1,200 m.(ii)
The gravel, rock, and layered rock zone are in the shallow surface of the sliding mass. This zone is mainly distributed in the shallow surface of the sliding mass below 1,200 m elevation. It is composed of gravel and rock formed by the landslide. The zone at the middle part of the sliding mass is the most deformed. Although the patent rock, metamorphic tuff, and arenaceous argillite have decomposed into gravel and rock, the sequence structure of primary rock is still visible (Figure5). The zone at the front part of the sliding mass consists mainly of badly decomposed primary rock, with much narrow diameters of 0.3∼1 m and more fine grain materials can be found (Figure 6).The lateral gullies of the partition II cut deep inside the sliding mass. Some of the gullies even cut through the sliding mass. The materials exposed on the gully bank are layered metamorphic tuff and arenaceous argillite. Their size depends on the thickness of the single layer of the parent rock. These rocks accumulate and are supported on stilts. Compared with the occurrence of the bedrock, the layered rock in the partition II has changed more. The change was caused by landslide movement. When the landslide occurred, rocks cut by the bedding plane and the structural plane in the sliding mass had uncoordinated displacement, so they separated or squeezed each other. As a result, the occurrence of layered rock in the partition II changed more (Figure7).(iii)
The zone of residual layered rocks and large rocks is distributed in the middle and shallow parts of the sliding mass. This zone is composed of metamorphic tuff gravel and rock. As revealed by the adits PD1 and PD3, the horizontal thickness of zone is 60∼65 m. The parent rock is gray-green medium-thick metamorphic tuff. The diameter of residual layered rocks and large rocks in the zone varies greatly from 20∼30 cm to over 3 m. Most rocks are about 1 m. The zone has a loose structure without fine-grained material filling inside.(iv)
The middle and deep parts of the landslide mass still retain the layered structure. This zone is about 40∼45 m thick and the single layer of the residual rock is 30∼40 cm thick. The dip direction of this zone is 200°∼225°, close to that of the bedrock. However, the dip angle of the rock stratum has changed 40°∼71°, which is a large variation. Although the layered remnants of the parent rock are relatively complete, the zone still contains the characteristics of displacement, dislocation, fracture, and separation along the bedding plane and the structural plane.⑤
The highly folded zone of argillite: the first 5∼10 m of the zone mainly consists of breccia and rock dust. There are also some scattered gravel and rock and a few magenta argillaceous materials. The lower part is a strongly crumpled stratum composed of arenaceous and argillaceous slate. It has developed asymmetric recumbent folds, with local ruptures. The stratum is tightly compressed without any fracture or overhead and the axial plane dips inside the slope.⑥
The slip zone: this zone is about 6∼9 m thick and is composed of grayish white rock dust and yellow dark brown argillaceous material. It also contains breccia, which is compact, wet, and sandy, with a particle diameter of 0.3∼1 cm. The sliding surface is 133 m away from the adit PD1 and 162 m away from the adit PD3. The sliding bed is composed of fine-grained tuffaceous slate. The single rock layer is 2∼3 cm thick and the rock structure is relatively intact, with an occurrence of 191∼202∠43∼52°, the same as the sliding surface.Figure 4
Typical geological profile of the Hejia landslide.Figure 5
Gravel and rock retaining the sequence structure of primary rock in partition I at 960∼1,200 m.Figure 6
Composition of the front of the sliding mass in partition I.Figure 7
Material composition of the sliding mass in partition II.Different parts of the slip zone revealed by the exploration adits have good correspondence in occurrence, location, thickness, and composition properties. Therefore, it can be concluded that the slip zone has a unified main sliding surface composed of a single rock stratum (interbedded and compressed). Moreover, as the branch sections in the three adits at different elevations show almost the same characteristics of the main sliding mass, and the five zones of different materials, from the surface to the center, have good correspondence in terms of extension, direction, thickness, and state, the possibility of multilevel sliding masses existing inside the main sliding mass can be ruled out.


## 2.3. Deformation Characteristics of the Landslide

### 2.3.1. Deformation Characteristics of the Trailing Edge

There is a 20° gentle slope in the trailing edge of the Hejia landslide. The wide slope is covered by 10∼20 m thick loess. According to the field survey, this slope does not have step-like terrain, indicating that the trailing edge has never been greatly deformed in history. This is confirmed by the lush vegetation and tall trees. The sliding mass has a length of over 800 m. Controlled by the residual layered structure of the sliding mass, the slope surface is roughly consistent with the residual layered surface. The field survey showed that the slope was relatively straight without large steps.


### 2.3.2. Deformation Characteristics of the Sliding Mass

The sliding mass has a length of over 800 m. Controlled by the residual layered structure of the sliding mass, the slope surface is roughly consistent with the residual layered surface. If there was a large deformation, a step-like terrain would appear. The field survey showed that the sliding mass was relatively straight without large steps.


### 2.3.3. Deformation Characteristics near the Sliding Zone

For exploration, the adits of the Hejia landslide were first excavated in 1990. The field survey in 2009 suggested that the main adits retained their original shape without any supports [17]. This suggested that the sliding mass composed of slate near the sliding zone had good integrity and tightness.


## 2.3.1. Deformation Characteristics of the Trailing Edge

There is a 20° gentle slope in the trailing edge of the Hejia landslide. The wide slope is covered by 10∼20 m thick loess. According to the field survey, this slope does not have step-like terrain, indicating that the trailing edge has never been greatly deformed in history. This is confirmed by the lush vegetation and tall trees. The sliding mass has a length of over 800 m. Controlled by the residual layered structure of the sliding mass, the slope surface is roughly consistent with the residual layered surface. The field survey showed that the slope was relatively straight without large steps.


## 2.3.2. Deformation Characteristics of the Sliding Mass

The sliding mass has a length of over 800 m. Controlled by the residual layered structure of the sliding mass, the slope surface is roughly consistent with the residual layered surface. If there was a large deformation, a step-like terrain would appear. The field survey showed that the sliding mass was relatively straight without large steps.


## 2.3.3. Deformation Characteristics near the Sliding Zone

For exploration, the adits of the Hejia landslide were first excavated in 1990. The field survey in 2009 suggested that the main adits retained their original shape without any supports [17]. This suggested that the sliding mass composed of slate near the sliding zone had good integrity and tightness.


## 3. Analysis of the Landslide Formation

### 3.1. Hard, Soft, High, and Steep Layered Slope Provided Structural Conditions for the Preparation of the Sliding Mass

The sliding mass of the Hejia landslide was over 800 m in length. To support such a long sliding mass, the rock mass must have a thick layer and high mechanical parameters. The deformation body of Bawang Mountain is situated 5 km away from the upstream of the Ertan Dam on the Yalong River. The over 900 m high slope comprises medium-thick limestone interbedded with clay rock. Many experts and engineers believe that it belongs to the sliding-bending (buckling) deformation failure. As the rock stratum is thick and high in modulus, it serves a stiff “plate” to hold the large slope, resulting in the great height and bending (buckling) depth of the slope.The exterior of the Bawang Mountain slope consists of thick-layered limestone and its interior is interbedded with clay rock. The structure and properties of the Bawang Mountain slope are similar to those of the Hejia landslide, which has thick-layered hard tuff outside and extremely thin argillite inside. Moreover, the slope of Bawang Mountain is as high as the Hejia landslide. Thus, the thick-layered tuff outside the slope of the Hejia landslide provided the major structural condition for supporting the sliding mass.


### 3.2. Thick-Layered Weak Rock Zone Provided Material Conditions for the Formation of the Sliding Surface

The exterior of the Hejia landslide was made of thick and hard tuff and the 110∼120 m area inside the sliding mass consisted of extremely thin layers of argillite and many weak interbeds. The thin layers and weak interbeds constituted a low-strength bedding surface within the slope. The surface was prone to large shear deformation (or plastic deformation) along the weak zone under slope stress. Long-time shear creep will lead to large plastic deformation of the slope and trigger a landslide.


### 3.3. Critical Conditions Provided Displacement Space for the Separation and Disintegration of the Sliding Mass

There was a large gully downstream of the Hejia landslide and there were several other gullies roughly parallel to it. They were developed along the argillite or interbedded compressed zone in the layered rock mass. Figure8 shows that these large gullies served as the downstream boundary of the Hejia landslide, forming conditions of downstream part being laterally separated from the slope. The upstream boundary of the landslide was comprised mainly of metamorphic tuff, with small gullies, thus having insufficient critical conditions. Moreover, away from the downstream boundary, there was a ridge stretching along the inclined direction of the rock layer. The ridge might block the slide and the large gullies in the lower right of the landslide (downstream boundary) provided conditions for a slight change of direction of the landslide displacement when the slide was blocked.Figure 8
Downstream gully and downstream boundary of the Hejia landslide.


## 3.1. Hard, Soft, High, and Steep Layered Slope Provided Structural Conditions for the Preparation of the Sliding Mass

The sliding mass of the Hejia landslide was over 800 m in length. To support such a long sliding mass, the rock mass must have a thick layer and high mechanical parameters. The deformation body of Bawang Mountain is situated 5 km away from the upstream of the Ertan Dam on the Yalong River. The over 900 m high slope comprises medium-thick limestone interbedded with clay rock. Many experts and engineers believe that it belongs to the sliding-bending (buckling) deformation failure. As the rock stratum is thick and high in modulus, it serves a stiff “plate” to hold the large slope, resulting in the great height and bending (buckling) depth of the slope.The exterior of the Bawang Mountain slope consists of thick-layered limestone and its interior is interbedded with clay rock. The structure and properties of the Bawang Mountain slope are similar to those of the Hejia landslide, which has thick-layered hard tuff outside and extremely thin argillite inside. Moreover, the slope of Bawang Mountain is as high as the Hejia landslide. Thus, the thick-layered tuff outside the slope of the Hejia landslide provided the major structural condition for supporting the sliding mass.


## 3.2. Thick-Layered Weak Rock Zone Provided Material Conditions for the Formation of the Sliding Surface

The exterior of the Hejia landslide was made of thick and hard tuff and the 110∼120 m area inside the sliding mass consisted of extremely thin layers of argillite and many weak interbeds. The thin layers and weak interbeds constituted a low-strength bedding surface within the slope. The surface was prone to large shear deformation (or plastic deformation) along the weak zone under slope stress. Long-time shear creep will lead to large plastic deformation of the slope and trigger a landslide.


## 3.3. Critical Conditions Provided Displacement Space for the Separation and Disintegration of the Sliding Mass

There was a large gully downstream of the Hejia landslide and there were several other gullies roughly parallel to it. They were developed along the argillite or interbedded compressed zone in the layered rock mass. Figure8 shows that these large gullies served as the downstream boundary of the Hejia landslide, forming conditions of downstream part being laterally separated from the slope. The upstream boundary of the landslide was comprised mainly of metamorphic tuff, with small gullies, thus having insufficient critical conditions. Moreover, away from the downstream boundary, there was a ridge stretching along the inclined direction of the rock layer. The ridge might block the slide and the large gullies in the lower right of the landslide (downstream boundary) provided conditions for a slight change of direction of the landslide displacement when the slide was blocked.Figure 8
Downstream gully and downstream boundary of the Hejia landslide.


## 4. Soil Properties of the Sliding Zone of the Landslide

### 4.1. Physical Indicators of the Sliding Zone Soil

The sliding zone soil was exposed in several exploration adits of the Hejia landslide. The undisturbed samples were collected at multiple points, and their physical indicators were measured on site and indoor, respectively. The results are shown in Table1.Table 1
Physical indicators of the sliding zone soil.
No.Density (g/cm3)Water content (%)ProportionDry density (g/cm3)Void ratioSaturation (%)Plastic limitLiquid limit12.1610.522.771.950.420.7015.82422.199.972.791.990.390.6915.82432.129.012.751.940.410.6016.223.942.149.082.781.960.420.6116.223.9Average value2.159.652.771.960.410.651624A particle size analysis test of the sliding zone soil was conducted. The results showed that the content of debris and gravel (≥0.075 mm) was 60.8%, and the content of clay and silt (<0.005 mm) was 39.2%. The results are shown in Table2.Table 2
Results of the particle size analysis test of the sliding zone soil.
No.>20 mm20～2 mm2～0.075 mm0.075～0.005 mm<0.005 mm18.030.122.022.518.028.331.521.621.417.2Average value8.230.821.821.917.3


### 4.2. Fitting Test of Soil Stress-Physical Properties in Sliding Zone of Hejia Landslide

In this study, several groups of gravity fitting compaction tests were carried out. The process method was to make the sliding zone soil into a near-liquid sample first and then carry out the stress-compaction test. The void ratio at various pressures obtained in the test is shown in Table3.Table 3
Gravity fitting compression test pressure and porosity ratio.
Pressure (kPa)012.5255010020040060016003200Void ratio0.560.460.440.410.390.370.350.320.300.27The correlation formula between pressure and void ratio obtained from the table is as follows:(1)e=−0.0342lnP+0.548r=0.999.By using element method, formula (1) of the normal stress caused by the dead weight of the sliding body on the sliding surface can be calculated. The normal stress obtained in different sections of the sliding surface is shown in Figure 9. It is shown that the normal stress in the sliding zone of Hejia landslide is relatively small in the upper part and gradually increases in the middle part, and the maximum normal stress in the lower part can reach 3.4–3.6 MPa under the action of the dead weight of the overlying sliding body.Figure 9
Calculation results of normal stress in slip zone of Hejia landslide.The pressure-void ratio relationship established by the normal stress and gravity compaction tests can help us understand the void ratio in different areas of the slip surface, and then the corresponding water content can be calculated by using the relationship between saturation, void ratio, and specific gravity value.


### 4.3. Indoor Sliding Soil Strength Test

Shear tests were carried out on samples of sliding zone soil with different densities, water content, and void ratio in laboratory to establish the relationship between the void ratio, water content, and friction coefficient and cohesion of sliding zone soil. The calculation results are shown in Table4.Table 4
Strength index of soil in slip zone of Hejia landslide under different water content.
Number of samplesWater content (%)Friction coefficientCohesion (kPa)18.40.54124210.20.5842312.10.5535413.10.6026515.00.6013616.30.637717.50.622According to the analysis of multiple groups of test results, the soil in the sliding zone of Hejia landslide is composed of more coarse particles, with debris accounting for 60.8%, and the particle size is mainly 2–20 mm, and the clay content only accounts for 17.3%. Therefore, the change of water content has less influence on the friction coefficient F value. The experimental results show that thef value varies from 0.54 to 0.63 in the process of water content increasing from 8.4% to 17.5%, and most of the f value ranges from 0.58 to 0.60. The cohesion c value decreases with the increase of water content. The correlation analysis between water content and cohesion was conducted, and the relationship curve between cohesion C and water content W was obtained. The relevant formula is as follows:(2)lnc=7.857−0.362∗wr=0.995.According to Section4.2 of this paper, water content is calculated first, and then cohesion C can be calculated according to formula (2). The calculation results are shown in Table 5.Table 5
C values of representative section of the sliding surface of Hejia landslide.
Distance (m)Spacing (m)Normal stress P (MPa)Void ratioWater content (%)Cohesion(kPa)16.5116.510.280.358.97100.4782.5533.020.810.328.06139.67115.5833.020.890.327.98143.77181.6233.021.000.317.88149.07214.6433.021.010.317.87149.61280.6833.021.040.317.85150.70313.7033.021.050.317.84151.25412.7733.021.070.317.82152.35492.8421.752.050.297.26186.58536.3517.573.610.276.77222.80


### 4.4. Strength Test and Results Analysis Indicators of the Sliding Zone Soil

Remolded consolidated quick shear tests of five groups of the sliding zone soil samples were conducted, the test results are shown in Table6. With f = 0.606, c = 118 kPa above water and with f = 0.485, c = 36 kPa under water (f for friction coefficient and c for cohesive force).Table 6
Results of the particle size analysis test of the sliding zone soil.
PositionFriction coefficientCohesion (kPa)Above water0.606118Under water0.48536


## 4.1. Physical Indicators of the Sliding Zone Soil

The sliding zone soil was exposed in several exploration adits of the Hejia landslide. The undisturbed samples were collected at multiple points, and their physical indicators were measured on site and indoor, respectively. The results are shown in Table1.Table 1
Physical indicators of the sliding zone soil.
No.Density (g/cm3)Water content (%)ProportionDry density (g/cm3)Void ratioSaturation (%)Plastic limitLiquid limit12.1610.522.771.950.420.7015.82422.199.972.791.990.390.6915.82432.129.012.751.940.410.6016.223.942.149.082.781.960.420.6116.223.9Average value2.159.652.771.960.410.651624A particle size analysis test of the sliding zone soil was conducted. The results showed that the content of debris and gravel (≥0.075 mm) was 60.8%, and the content of clay and silt (<0.005 mm) was 39.2%. The results are shown in Table2.Table 2
Results of the particle size analysis test of the sliding zone soil.
No.>20 mm20～2 mm2～0.075 mm0.075～0.005 mm<0.005 mm18.030.122.022.518.028.331.521.621.417.2Average value8.230.821.821.917.3


## 4.2. Fitting Test of Soil Stress-Physical Properties in Sliding Zone of Hejia Landslide

In this study, several groups of gravity fitting compaction tests were carried out. The process method was to make the sliding zone soil into a near-liquid sample first and then carry out the stress-compaction test. The void ratio at various pressures obtained in the test is shown in Table3.Table 3
Gravity fitting compression test pressure and porosity ratio.
Pressure (kPa)012.5255010020040060016003200Void ratio0.560.460.440.410.390.370.350.320.300.27The correlation formula between pressure and void ratio obtained from the table is as follows:(1)e=−0.0342lnP+0.548r=0.999.By using element method, formula (1) of the normal stress caused by the dead weight of the sliding body on the sliding surface can be calculated. The normal stress obtained in different sections of the sliding surface is shown in Figure 9. It is shown that the normal stress in the sliding zone of Hejia landslide is relatively small in the upper part and gradually increases in the middle part, and the maximum normal stress in the lower part can reach 3.4–3.6 MPa under the action of the dead weight of the overlying sliding body.Figure 9
Calculation results of normal stress in slip zone of Hejia landslide.The pressure-void ratio relationship established by the normal stress and gravity compaction tests can help us understand the void ratio in different areas of the slip surface, and then the corresponding water content can be calculated by using the relationship between saturation, void ratio, and specific gravity value.


## 4.3. Indoor Sliding Soil Strength Test

Shear tests were carried out on samples of sliding zone soil with different densities, water content, and void ratio in laboratory to establish the relationship between the void ratio, water content, and friction coefficient and cohesion of sliding zone soil. The calculation results are shown in Table4.Table 4
Strength index of soil in slip zone of Hejia landslide under different water content.
Number of samplesWater content (%)Friction coefficientCohesion (kPa)18.40.54124210.20.5842312.10.5535413.10.6026515.00.6013616.30.637717.50.622According to the analysis of multiple groups of test results, the soil in the sliding zone of Hejia landslide is composed of more coarse particles, with debris accounting for 60.8%, and the particle size is mainly 2–20 mm, and the clay content only accounts for 17.3%. Therefore, the change of water content has less influence on the friction coefficient F value. The experimental results show that thef value varies from 0.54 to 0.63 in the process of water content increasing from 8.4% to 17.5%, and most of the f value ranges from 0.58 to 0.60. The cohesion c value decreases with the increase of water content. The correlation analysis between water content and cohesion was conducted, and the relationship curve between cohesion C and water content W was obtained. The relevant formula is as follows:(2)lnc=7.857−0.362∗wr=0.995.According to Section4.2 of this paper, water content is calculated first, and then cohesion C can be calculated according to formula (2). The calculation results are shown in Table 5.Table 5
C values of representative section of the sliding surface of Hejia landslide.
Distance (m)Spacing (m)Normal stress P (MPa)Void ratioWater content (%)Cohesion(kPa)16.5116.510.280.358.97100.4782.5533.020.810.328.06139.67115.5833.020.890.327.98143.77181.6233.021.000.317.88149.07214.6433.021.010.317.87149.61280.6833.021.040.317.85150.70313.7033.021.050.317.84151.25412.7733.021.070.317.82152.35492.8421.752.050.297.26186.58536.3517.573.610.276.77222.80


## 4.4. Strength Test and Results Analysis Indicators of the Sliding Zone Soil

Remolded consolidated quick shear tests of five groups of the sliding zone soil samples were conducted, the test results are shown in Table6. With f = 0.606, c = 118 kPa above water and with f = 0.485, c = 36 kPa under water (f for friction coefficient and c for cohesive force).Table 6
Results of the particle size analysis test of the sliding zone soil.
PositionFriction coefficientCohesion (kPa)Above water0.606118Under water0.48536


## 5. Determination and Stability Analysis of the Landslide Physical Parameters

### 5.1. Calculation Parameters of the Landslide

The calculation parameters of the landslide are shown in Table7.Table 7
Calculation parameters of the landslide.
No.NameUnit weightγ (KN/m3)fC (kPa)1Sliding zone (above water)21.50.6061182Sliding zone (under water)22.50.485363Bedrock (above water)27.20.5755504Bedrock (under water)27.50.46440


### 5.2. Calculation Condition of the Landslide

Four calculation conditions were considered for the landslide calculation as shown in Table8.Table 8
Calculation conditions of the landslide.
Calculation conditionCalculation condition 1Calculation condition 2Calculation condition 3Calculation condition 4Water levelNatural water levelNormal water level 800 mNormal water level 800 mNormal water level 800 mSeismic load——0.195 g—Collapsed bank——Collapsed bank 30 m wideCollapsed bank 30 m wide


### 5.3. Overall Stability Calculation Results of the Landslide

The stability of the landslide under each calculation condition was analyzed with the GeoStudio, a slope stability analysis software. The software’s built-in SEEP/W module can automatically import the seepage calculation results for stable analysis. Table9 shows the results of the landslide stability under different working conditions. The safety factor of calculation condition 1 is 1.337, indicating the landslide was in a stable state, the same as the field survey’s result. After the slope is saturated because of the water storage of the reservoir, its mechanical parameters are reduced, so the safety factor of the calculation condition 2 declines to 1.231, which is in line with the current general law. In the event of normal water level + earthquake, the safety factor drops to 1.086. After the slope toe collapsed after the water storage of the reservoir, the safety factor decreases but is still above the stable state of 1.0.Table 9
Overall stability calculation results of the landslide.
Calculation conditionCalculation condition 1Calculation condition 2Calculation condition 3Calculation condition 4Safety factor K1.3371.2311.0861.190


### 5.4. Stability Evaluation of the Landslide

According to the research of Section3 and the overall stability calculation results of this section, the Hejia landslide was a super large-scale buckling-type landslide caused by long-term sliding and bending deformation of medium-steep and layered rock mass with thick-layered hard tuff outside and a sliding zone of layered soft rock, and it was an incompletely disintegrated landslide. Under natural water level, normal water level 800 m, and normal water level 800 m (collapsed bank 30 m wide), it was in a stable state. However, after the reservoir impounds water and the leading edge of the slope collapses, it was basically stable under a seismic condition, with low safety reserves.


## 5.1. Calculation Parameters of the Landslide

The calculation parameters of the landslide are shown in Table7.Table 7
Calculation parameters of the landslide.
No.NameUnit weightγ (KN/m3)fC (kPa)1Sliding zone (above water)21.50.6061182Sliding zone (under water)22.50.485363Bedrock (above water)27.20.5755504Bedrock (under water)27.50.46440


## 5.2. Calculation Condition of the Landslide

Four calculation conditions were considered for the landslide calculation as shown in Table8.Table 8
Calculation conditions of the landslide.
Calculation conditionCalculation condition 1Calculation condition 2Calculation condition 3Calculation condition 4Water levelNatural water levelNormal water level 800 mNormal water level 800 mNormal water level 800 mSeismic load——0.195 g—Collapsed bank——Collapsed bank 30 m wideCollapsed bank 30 m wide


## 5.3. Overall Stability Calculation Results of the Landslide

The stability of the landslide under each calculation condition was analyzed with the GeoStudio, a slope stability analysis software. The software’s built-in SEEP/W module can automatically import the seepage calculation results for stable analysis. Table9 shows the results of the landslide stability under different working conditions. The safety factor of calculation condition 1 is 1.337, indicating the landslide was in a stable state, the same as the field survey’s result. After the slope is saturated because of the water storage of the reservoir, its mechanical parameters are reduced, so the safety factor of the calculation condition 2 declines to 1.231, which is in line with the current general law. In the event of normal water level + earthquake, the safety factor drops to 1.086. After the slope toe collapsed after the water storage of the reservoir, the safety factor decreases but is still above the stable state of 1.0.Table 9
Overall stability calculation results of the landslide.
Calculation conditionCalculation condition 1Calculation condition 2Calculation condition 3Calculation condition 4Safety factor K1.3371.2311.0861.190


## 5.4. Stability Evaluation of the Landslide

According to the research of Section3 and the overall stability calculation results of this section, the Hejia landslide was a super large-scale buckling-type landslide caused by long-term sliding and bending deformation of medium-steep and layered rock mass with thick-layered hard tuff outside and a sliding zone of layered soft rock, and it was an incompletely disintegrated landslide. Under natural water level, normal water level 800 m, and normal water level 800 m (collapsed bank 30 m wide), it was in a stable state. However, after the reservoir impounds water and the leading edge of the slope collapses, it was basically stable under a seismic condition, with low safety reserves.


## 6. Engineering Treatment Measures

### 6.1. Protection of the Water Level Fluctuation Area

The schematic diagram of water level protection zone is shown in Figure10. To ensure the stability of the Hejia landslide and prevent instability after bank collapse, the following measures were taken for the water level fluctuation area:(1)
Range of protection elevation: EL790～EL810.(2)
The slope and walkway within EL790∼EL810 were poured with concrete with a thickness of 80∼30 cm and a grade of C20. Then the surfaces were laid with reinforcing meshes with a diameter of 18 mm and a spacing of 25 cm.(3)
The gravel soil slope within EL790∼EL810 was laid with anchor rods with 28 mm diameter, 2 m spacing, and 4.5 m length, and 50 cm of the rod was exposed; the debris slope was installed with soil nails which were 48 mm in diameter and 18 m in length, and 50 cm was exposed.(4)
The slope was laid with PVC drainage pipes with a diameter of 50 mm and a spacing of 2 m, which extended into the slope and were wrapped with geotextile.(5)
Besides concrete and soil nails applied for the surface gravel soil in the shallow part, a row of 1,000 KN unbonded prestressed anchor cables, with a length of 30∼40 m, a spacing of 6 m, and a depth of entering rock of not less than 5 m, were laid at EL795 and EL800 to ensure the overall stability.Figure 10
Schematic diagram of water level protection zone.


### 6.2. Protection of the Fluctuation Area with Water Level Lower Than EL790 m

The fluctuation area with water level lower than EL790 m has problems as follows: During low-head operation of the reservoir, the slope is scoured by waves. After the water level rises, the slope immerses in the water for a long time. Once it becomes saturated, the bank may collapse. This may affect the stability of the protection area. Therefore, it must be treated.According to geological information and relevant literature, the underwater angle of repose of the slope colluvial deposits is 28∼32°. The underwater angles of repose for most slope colluvial deposits in the lower part of the protection area were greater than 29∼33°, with an average of 31°. When the reservoir stores water, the lower part may collapse and form a new slope, which would affect the stability of the upper protection area. To prevent this, it was planned to build a gabion retaining wall on the first terrace of the river. After renovation, the angle of the slope would be 30°. As it was close to the angle of repose underwater, the stability of the slope could be ensured.


### 6.3. Landslide Monitoring

In addition to necessary engineering protection and treatment, relevant prototype monitoring measures were taken to ensure the stability of the Hejia landslide. The detailed scheme was as follows:(1)
Three monitoring longitudinal sections were set, each with four points to monitor surface deformation. Eight working base points were set outside the landslide area to monitor horizontal displacement with the line of collimation method.(2)
Indium measuring lines were laid inside the exploration adits for relative level monitoring. Hydrostatic levelling points were set along the adit line to measure the vertical displacement. The deepest point was penetrated into the stable rock mass at the bottom of the landslide.(3)
Inclinometer pipes were buried in existing exploration bore-holes for deformation monitoring of the deep sliding mass.


## 6.1. Protection of the Water Level Fluctuation Area

The schematic diagram of water level protection zone is shown in Figure10. To ensure the stability of the Hejia landslide and prevent instability after bank collapse, the following measures were taken for the water level fluctuation area:(1)
Range of protection elevation: EL790～EL810.(2)
The slope and walkway within EL790∼EL810 were poured with concrete with a thickness of 80∼30 cm and a grade of C20. Then the surfaces were laid with reinforcing meshes with a diameter of 18 mm and a spacing of 25 cm.(3)
The gravel soil slope within EL790∼EL810 was laid with anchor rods with 28 mm diameter, 2 m spacing, and 4.5 m length, and 50 cm of the rod was exposed; the debris slope was installed with soil nails which were 48 mm in diameter and 18 m in length, and 50 cm was exposed.(4)
The slope was laid with PVC drainage pipes with a diameter of 50 mm and a spacing of 2 m, which extended into the slope and were wrapped with geotextile.(5)
Besides concrete and soil nails applied for the surface gravel soil in the shallow part, a row of 1,000 KN unbonded prestressed anchor cables, with a length of 30∼40 m, a spacing of 6 m, and a depth of entering rock of not less than 5 m, were laid at EL795 and EL800 to ensure the overall stability.Figure 10
Schematic diagram of water level protection zone.


## 6.2. Protection of the Fluctuation Area with Water Level Lower Than EL790 m

The fluctuation area with water level lower than EL790 m has problems as follows: During low-head operation of the reservoir, the slope is scoured by waves. After the water level rises, the slope immerses in the water for a long time. Once it becomes saturated, the bank may collapse. This may affect the stability of the protection area. Therefore, it must be treated.According to geological information and relevant literature, the underwater angle of repose of the slope colluvial deposits is 28∼32°. The underwater angles of repose for most slope colluvial deposits in the lower part of the protection area were greater than 29∼33°, with an average of 31°. When the reservoir stores water, the lower part may collapse and form a new slope, which would affect the stability of the upper protection area. To prevent this, it was planned to build a gabion retaining wall on the first terrace of the river. After renovation, the angle of the slope would be 30°. As it was close to the angle of repose underwater, the stability of the slope could be ensured.


## 6.3. Landslide Monitoring

In addition to necessary engineering protection and treatment, relevant prototype monitoring measures were taken to ensure the stability of the Hejia landslide. The detailed scheme was as follows:(1)
Three monitoring longitudinal sections were set, each with four points to monitor surface deformation. Eight working base points were set outside the landslide area to monitor horizontal displacement with the line of collimation method.(2)
Indium measuring lines were laid inside the exploration adits for relative level monitoring. Hydrostatic levelling points were set along the adit line to measure the vertical displacement. The deepest point was penetrated into the stable rock mass at the bottom of the landslide.(3)
Inclinometer pipes were buried in existing exploration bore-holes for deformation monitoring of the deep sliding mass.


## 7. Conclusion

Through the field survey and experimental study, this paper has analyzed the structural characteristics of the Hejia landslide and its formation mechanism; moreover, it has proposed engineering measures to enhance the stability of the slope as the water level of the reservoir fluctuated. The conclusions are as follows:(1)
The Hejia landslide is located in the reservoir area of a hydropower station. Its volume is as large as 2,350 × 104 m3; as a super large-scale landslide, it is formed by long-term sliding and bending deformation. The outside layer of the slope consists of high, steep, and layered hard rock and the sliding zone is comprised of layered soft rock.(2)
The formation mechanism of the landslide is as follows: ① Hard, soft, high, steep, and layered slope has provided structural conditions for the formation of the sliding mass; ② thick-layered weak rock zone has provided material conditions for the formation of the sliding surface; ③ free face conditions have provided displacement space for the separation and disintegration of the sliding mass.(3)
When the reservoir impounds water, the slope toe will be immersed under the water, which may decrease the safety factor, though the factor still meets the requirement.(4)
When the reservoir impounds water, the overall stability of the slope can be assured but the slope toe may collapse, so related engineering measures should to be taken.(5)
According to the operation monitoring data of the past multiple years, the landslide has been stable since the engineering measures were taken. This proves that the engineering treatment is reasonable.



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*Source: 1372621-2021-12-26.xml*