Reservoir Landslide Physical Modelling under Ice-Snow Melting and Reservoir Water Combined Action

Extreme ice-snow melting in winter affects the infiltration process of snow water on the slope surface significantly and plays an important role in the deformation stability of landslide. Variation in pore water pressure is regarded as an essential factor of landslide instability induced by snow water. In order to figure out the internal relationship between the infiltration process of snow water and the failure mode of deformation and instability of the accumulation landslide, the response law and deformation and failure mode of pore water pressure and soil pressure of landslide accumulation under different ice-snow melting conditions are deeply studied based on the indoor large-scale landslide model test. We have studied the physical model test under the combined action of reservoir water and ice-snowmelting. It reveals the seepage erosion deformation and failure mechanism. It undoubtedly provides references of great importance for the geological hazard governance of bank slope in the ,ree Gorges Reservoir Area.


Introduction
In early 2008, the rare ice-snow climate occurred and induced large geological disasters in southern China. e soil within 5 cm-10 cm underground can be frozen in short time and tends to form freezing-thawing cycles. e process of thawing ice is short and can form centralized surface runoffs. Frost-heaving force of surface frozen soil will not directly induce landslide and collapse; however, the repeated freezing-thawing of surface soil and the infiltration of melting ice and snow are the main factors of geological disasters.
Extreme ice-snow disasters are characterized by a large amount of ice and snow, deep snow, and a long duration of low temperature and freezing. After the extreme ice-snow disaster in the ree Gorges Reservoir Area of China, the ice-snow melting did not reach the level of rainstorm [1]. In the ree Gorges Reservoir Area of China, water reservoir landslides are affected by the reservoir water and hydrodynamic conditions, such as rainfall and reservoir water level variation, and they do have different degrees of impacts on the stability of these landslides [2][3][4][5][6][7]. e infiltration of ice-snow melting is one of the important factors that induce the slope instability in winter [8]. e slope instability caused by snow melting is a long-term lag accumulation effect [9]. In view of the research results obtained by stability analysis of the bank slope under the extreme ice-snow disaster weather [10], the extreme icesnow boundary conditions and the seepage characteristics of slope rock mass were adopted for reference. e stability analysis of the bank slope under the condition of ice-snow melting is conducted the seepage calculation and stability analysis of snow melting infiltration under different factors [11], using the saturated-unsaturated seepage finite element method [12], during which process the statistical data of snow thickness. e key to the numerical simulation of the slope instability is revealed theoretically the change process of the slope stress [13][14][15], characteristics and failure process of the infiltration, and the transient additional water load [16]. e distribution of the soil saturation factor in time and space is obtained by using GIS platform [17]. rough the numerical simulation of energy balance equation and water balance equation [18], a physical snow melting model based on the single point and double layer is established [19], and a theoretical model of snow ion infiltration is proposed simultaneously, which shows that the relationship between ion concentration and infiltration volume is nonlinear and positive covariance [20]. e snowmelt yield and confluence are simulated to improve the simulation accuracy; the water heat stress coupling numerical simulation of rock freezing and thawing cycle is studied [21]. e overturning stability coefficient of rock slope changes obviously due to the influence of extreme ice-snow disaster [22]. Snow water infiltrates along the fracture, and the water in the fracture freezes after freezing. e original equilibrium failure results in landslides and collapses [23]. If the effect is combined with reservoir water variation, the possibility and scale of landslides and collapses may be bigger. e reliability of slope under different working conditions is calculated and analyzed, respectively [24]. According to the field investigation, the main causes and factors of the soil slope's freeze-thaw instability are discussed [25][26][27]. Moreover, although many landslide model tests of combined effect of rainstorm and reservoir water have been carried out [28][29][30][31][32][33][34], large-scale three-dimensional physical model tests of the reservoir bank slope under the combined action of snow melting and reservoir water are in urgent need.
In 2000, Yigong landslide occurred in permafrost regions of China, the ice-snow melting causes landslides and debris flow, and the ice-snow melting has caused huge geological disasters of rock and soil. In comparison with extreme ice-snow in the ree Gorges Reservoir Area, the depth, thermal, and freeze-thaw processes are not the same, the rare ice-snow climate occurred in the ree Gorges Reservoir Area is rare, and the geological disaster caused by it has not been paid enough attention. In addition, there are great differences in topography, geological environment, climate environment, and so on.
erefore, under the condition of extreme snow and ice disaster in the middle and low latitudes of the ree Gorges Reservoir Area in China, the theoretical, experimental, and numerical studies on the types of geological disasters and their influencing mechanisms are basically blank.

Physical Model.
e preliminary design scheme of the three-dimensional artificial landslide model test steel frame mainly includes the following two modes: the outer inclined support mode and the rotating staircase mode, both meet the test requirements. In consideration of the high requirements for longitudinal rigidity in the middle, through the 3D finite element calculation and research, the external inclined support mode covers a large area and needs high rigidity of the inclined support steel frame. After optimization and combination, the rotary stair type scheme is then formed and selected. e concrete-filled steel tube support is adopted, which greatly improves the longitudinal rigidity of the model steel frame. e internal dimension is 12 m long, 6 m high, and 6 m wide, adopting the open top steel structure form and water sealing material. e lateral deformation is required to be within 0.3%, and its structure and system composition are shown in Figure 1.

Model Generalization.
In this paper, the research object of the project is the area where the Outang landslide is located in Anping Town, Fengjie County, Chongqing, which is located on the right bank of the ree Gorges Reservoir 12 km upstream of Fengjie County. Landslides have been formed by multilevel and multistage sliding in the geological history, and the scale is huge. Since the impoundment of the ree Gorges project, the front edge of the Outang landslide has been submerged by the reservoir water, resulting in large deformation.
e overall form of the landslide is like an ancient bell with a spoon-shaped profile. e total area is about 1.78 km 2 , the total volume is about 9000 × 104 m 3 , and the thickness of the sliding body in the front part is over 110 m. e maximum longitudinal length of the landslide is about 1800 m, the maximum width of the front edge along the river channel is about 1100 m, and the width of the back edge is about 580 m. e elevation of the front edge is about 95 m, part of it is submerged below the water level of the reservoir, the elevation of the back edge is about 705 m, and the relative height difference between the front edge and the back edge is about 610 m. e surface of the earth is steep and gentle, showing a broken line, with an average slope of about 26°. e plan of the Outang landslide is shown in Figure 2. e shallow sliding mass has a better permeability in the east and west of the Outang landslide. e deformation trend of groundwater and reservoir water is synchronous. e soaking softening effect of reservoir water on sliding belt is quite obvious. e anti-sliding force of the anti-slide section is significantly reduced. Because the cataclastic rock mass adjusts the stress, creep occurs along the potential bedding slip surface. e severe deformation areas in the east and west are mainly affected by precipitation (snow).
Based on the principle of reflecting the deformation, failure characteristics, and evolution process of the Outang landslide and according to the detailed investigation report of the Outang landslide in Fengjie County, the model test satisfied the requirements of geometric, material, kinematic, and dynamic similarities and simulated the anticipated loading conditions. e model test results can be used to predict the deformation and failure modes of the reservoir landslide. e boundary conditions and relevant information were determined from the field investigation and the topomap. e MATLAB software was used to extract the 3D coordinates and elevations. Moreover, the total station was used to set out the model construction.
e model was established based on the observed one of landslide at the ree Gorges Reservoir Area. e scale ratio between the model and the prototype was 1 : 175. e landslide model section is shown in Figure 3.
In order to explore the law of deformation and failure, under ice-snow melting and water-level rise, which give birth to a new born reservoir landslide of the typical bedding accumulation body in the ree Gorges Reservoir Area, this paper selected the Outang landslide as the research object. According to the test purpose, test method, and test conditions, the prototype is generalized. e generalization objective contains the geological structure generalization and the environmental condition generalization.

Geological Structure Generalization.
Selection of landslide test section. e deformation and failure of the Outang landslide is shown with the 3D characteristics in space. e whole structure data of slope is analyzed using multistation 3D laser scanning technology. Based on digital simulation test, select A-A′ profile, shown in the Figure 3. Based on borehole data, exploration profile data, surface terrain data, surface remote sensing image, reconnaissance engineering, and other design data, the Outang landslide bank slope model was established. e 3D geological generalization model is as shown in Figure 4.

Environmental Condition Generalization.
e generalization of environmental conditions changes the external environment of the complex landslide to the controlled model boundary conditions by human. e ice-snow melting and the water level are considered in the model test.
e reservoir water action can be generalized as two processes, which rise from 0 cm to 100 cm by the rate of 25 cm/h and stabilize the reservoir water level at 100 cm. e effects of reservoir water in front of the landslide are infiltration, erosion, scouring, erosion, deformation, and destruction.
e physical mechanical properties of the soil are weakened by the immersion of reservoir water, which is the front edge of the bank slope. Soaking in reservoir water and soil mass seepage are affecting the stability of reservoir landslide [35]. e effect of ice-snow melting infiltration (total amount, rate, and duration of ice-snow melting) on slope infiltration, runoff generation, and soil seepage erosion creep deformation.

Model Test
eory. e model test theory mainly includes the following four parts: (1) Model similarity theory and similarity criterion (2) e method of determining and optimizing the model similar materials (3) Noncontact measurement technology and method (4) Model distortion correction method e formation of landslide is a comprehensive action of internal and external factors. e main internal factors are the physical mechanical parameters of the slip body and the slip material. e similarity theory of the landslide model should be satisfied in many aspects, for example, geometric dimensions, boundary conditions, load density, strength, deformation, and hydraulic characteristics of similar materials. e geometric similarity coefficient C l is determined by combining the landslide prototype size and model groove size. C l is equal to 175. As for dimensional analysis, the pattern can be written as follows: where C g is the gravitational similarity coefficient; C ρ is the density similarity coefficient; C φ is the internal friction angle similarity coefficient; C μ is Poisson's ratio similarity coefficient; C t is the time similarity coefficient; C q is the snowfall similarity coefficient; C v is the velocity similarity coefficient; C k is the infiltrate similarity coefficient; C l is the geometry similarity coefficient; C c is the cohesion similarity coefficient;    Figure 5 and Table 1. Physical-mechanical parameters and components of model landslide are shown in Table 2, where C ρ , C k , C c , and    Advances in Civil Engineering C φ are similarity coefficients. e slip zone is made of glass beads with different diameters. e big bead diameter is 10 mm. e small bead diameter is 5 mm. e thickness of the sliding belt in the model test is 50 mm.

Sensor Layout
(1) ree longitudinal sections and three transverse sections are arranged at different positions of the landslide to analyze the variation characteristics of the stress field, seepage field, and displacement field, respectively.
In addition, a total of 36 sensors, evenly arranged on the three transverse sections, are installed, including three soil pressure sensors, six earth pressure (thrust) sensors, nine pore water pressure sensors, nine displacement sensors, and nine soil moisture sensors (c-ray method). Setup 9 optical measurement points to observe the changes of earth pressure, pore water pressure, displacement, and soil moisture, respectively.
e C-C profile is located at 230 cm of the front edge of the landslide. e earth pressure sensor and the pore water pressure sensor are located near the front sliding zone. e corresponding prototype elevation is about 118 m. e displacement sensor is arranged on the surface of the section. e corresponding prototype elevation is about 180 m; soil moisture measuring points, which the corresponding prototype elevation is about 165 m. e elevations of the three noncontact displacement measurement points were respectively set at 170 m, 160 m, and 150 m. e sensors on the B-B section and A-A section are arranged in accordance with C-C section. See Figure 6 for the specific location.  Table 3.

Test Process and Test Result Analysis
Before the large-scale three-dimensional model test, the bank slope model was pretreated so that the test soil can reach the initial water content (volumetric water content of 22-24%), and the bank slope test soil area was 50 m 2 . In winter, the operational water level of the ree Gorges Reservoir Area was 175 m, and the reservoir water level of the bank slope in the model test bank slope was set to be 100 cm correspondently. e ice and snow with a thickness of 30 cm was evenly laid which was started from 6 a.m. and Internal friction angle 18.6 Advances in Civil Engineering ended at 7 a.m. on February 1, 2019 (the local temperature of the test site at that time was about 0 o C). At this time, the water was slowly stored at the speed of 25 cm/h from the bottom (0 cm) of the reservoir in the model to the water level of 100 cm. During the rising of water level, the front part of the bank slope was gradually submerged by the reservoir water to the position of 100 cm water level, and microcracks were observed on the soil body at the front edge of the bank slope. At 8 a.m. on February 8, 2019, ice-snow melting was ended, and the combined effect of ice-snow melting water and 100 cm reservoir water level was made to last for 7 days, about 170 hours. e deformation process of the reservoir bank slope under the above effect is shown in Figure 7. e high water level had been maintained for 15 days until 8 a.m. on February 16, 2019.

Volume and Rate Calculation of Indoor Ice-Snow Melting.
In this test, the thickness of bank slope soil is about 1.5-2.0 m and that of slope top is 1.5 m. It is evenly laid according to the actual slope shape trend from the top to the toe of the slope, and the maximum thickness of the middle is 2.0 m. Seven tons ice and snow is laid in total. e surface area of the bank slope is 50 m 2 , with an average thickness of ice and snow to be 30 cm. e 24-hour temperature of the slope surface is strictly recorded; we have calculated snow melting rate and intensity by temperature difference. e ice and snow melts completely in 7 days, while 80% of the total amount of ice and snow melts in the first 5 days, with the rate of 1.1 T/d, namely, 46 kg/h or 0.76 kg/min. e density of ice and snow used in the model test is 0.5 × 10 3 -0.6 × 10 3 kg/m 3 , and the slope angle of the model test landslide is 26°. e 30 cm thick ice and snow laid on the soil mass of the bank slope is the ice sheet waiting for gradual melting, and the load applied to the soil body of the bank slope equals to that of 7T water in the water tank gradually falling on the bank slope.

Model Boundary Conditions.
In this paper, the transient seepage field of slope changed by water level. e sliding surface is a barrier boundary, that is, zero flow boundary.  Figure 6: Sensor layout. (1) Build the model bank slope and calibrate the buried sensor which is then debugged to meet the standard. Stable initial settlement of the bank slope is achieved when the similar materials of the bank slope reach the initial volumetric water content of the test, i.e., 22-24%; (2) Evenly pave the ice and snow with a thickness of 30 cm in the 50 m 2 test bank slope soil; (3) e water rises at a speed of 25 cm/h from the bottom (0 cm) of the dam to the high water level at 100 cm; (4). e water at the high water level of 100 cm in the model tank is fused with the ice-snow melting water until it completely melts.
15 day 6 Advances in Civil Engineering e boundary of constant head is below the water level. e infiltration process of ice-snow melt water is essentially a process of snow water migration and deformation in the unsaturated region. e infiltration is the boundary of soil water flow. e shallow sliding mass has a very good permeability in the east and west of the Outang landslide. e groundwater and the reservoir level has the same change trend， and the deformation is large. e sliding belt has soaking effect quite obvious by reservoir water. e anti-slide force is obviously reduced. e broken soil has adjust stress. e creep deformation has occurred at the potential bedding slip surface. e model failure mainly occurred in the soil at a depth of 80 cm. e soil has strong permeability. e seepage characteristic is unsaturated vertical infiltration. e failure mode is unsaturated shallow failure [36], and surface runoff also occurs.

Test Response of Ice-Snow Melting Infiltration.
e matrix suction of the unsaturated zone decreased gradually as ice and snow continuously melted, followed by gradual decrease in the overall stability of the slope and gradual increase in both horizontal and vertical displacement of the slope surface. e deformation showed that the deformation of the front edge was larger than that of the back edge in the horizontal direction, and the back edge in the vertical direction was downward staggered, while the front edge was uplifted. With the infiltration of snowmelt water and increase in the pore water pressure of the slope, the effective stress of the soil decreased, accompanied by simultaneous decrease in the shear strength of the soil and the stability of the slope. e deformation of the bank slope under ice-snow melting is shown in Figure 8. At this time, the load effect of ice-snow melting water can be divided into the following three processes: (1) At the beginning of snowmelt infiltration, the snowmelt water infiltrated into the slope body, leading to gradual increase in the water content of the slope soil on the surface layer from the initial water content, and the snowmelt water colored by faint yellow was discharged out of the slope body about 24 hours later. After 48 hours, the water content of the surface soil reached the saturated water content. During the first 48 hours, the advancing trend of the wetting front was parallel to the soil slope. After 72 hours, the wetting front started to move downward in a semielliptical shape and the unsaturated soil at the lower part of the bank slope got saturated. At the 96th hour, the soil at the depth of 30 cm of the soil slope reached saturation, and the vertical depth of the wetting front then gradually reached 40 cm. Subsequently, the seepage expanded to 50 cm along the slope direction, and the internal saturation line of the bank slope steadily moved down. (2) e respective water content at the depth of 30 cm and 40 cm at the top, middle, and near the foot of the slope changed rapidly. After 10 days of ice and snow melting, the above water content slowly decreased and gradually stabilized, among which there were minor differences. However, the water content in the foot at the depth of 50 cm changed obviously and increased to some extent after snowmelt water infiltration stopped. e increase in water content was attributed to the continuous infiltration caused by the hysteresis of the water content of the upper soil. In addition, a large range of transient saturation area may appear in the gentle slope zone and the slope foot. (3) After 120 h, the infiltration peak of ice-snow melting water gradually slowed down and the water content increasing rapidly in the saturated area of the slope gradually stabilized with weakening characteristics.
Here, occurred a lag effect during the infiltration process. e seepage of the wetting front and along the slope direction expanded, followed by continuous soil softening and swelling of slope foot soil with a speed significantly lower than that at the peak of snowmelt.
Snow melting intensity is closely related to the failure mode of landslide. e variation of pore water pressure with snow melting intensity is different at different depths Advances in Civil Engineering 7 in the same section.
e response time of pore water pressure to snow melting intensity is positively proportional to the snow melting intensity. When the snow melting intensity is 0.0116 kg/min.m 2 , the soil will flow at the foot of the slope; when the snow melting intensity is 0.0128 kg/min.m 2 , the failure mode of the landslide is that the slope toe starts to form multistage backward shallow creep deformation step by step. When the snow melting strength is 0.0152 kg/min.m 2 , the landslide mass will creep along the most dangerous shear plane and eventually form plastic creep flow.

Test Response of Combined Action of Ice-Snow Melting and Reservoir
Water. e 100 cm reservoir water level can submerge 19.2% of the bank slope in the model test. With the combination of the above water level and ice-snow melting, the infiltration produced a continuous seepage force to the outer side of the slope and the cracks at the foot and front edge of the bank slope expanded, deepened, and infiltrated continuously. Cracks and settlement of the front edge of the bank slope occurred, resulting in the slump deformation. e process curve of measured values changed with time of each sensor under the condition of combined action of ice-snow melting and reservoir water, based on the distortion model and correction method of distortion [37], as shown in Figure 9. e sensor takes reading every 10 minutes. e conclusions are presented as follows: (1) e volumetric water content of ice-snow melt water is higher than 35%. e change of each water content sensor is significant, and the values of all water content sensors are increased. After a certain period of time, the wetting front reaches the monitoring point and the water content gradually increases to the peak value and tends to be stable. e water level of the reservoir rises slightly with the increase in snowmelt.
(2) As shown in Figure 9(b), the pore water pressure increases until it reaches saturation and is generally stable under the condition that the soil mass on the bank slope below the water level of 100 cm turns to be saturated gradually after a certain period of immersion. However, the pore water pressure of the soil above the water level of 100 cm is always negative, which indicates that the saturation range of ice-snow melt water is relatively shallow at the beginning of the infiltration, and the soil of the depth, to which the pore water pressure sensor is  Advances in Civil Engineering buried, is not completely soaked. With the continuous infiltration, the pore water pressure above the 100 cm water level gradually approaches to 0 from the negative value and the saturation range of snowmelt infiltration is gradually expanding. e change of pore water pressure at the measuring point increases with the rise of reservoir water level, and the change of pore water pressure lags slightly. From the monitoring data of the sensor, it can be seen that the time when the pore water pressure measuring the C-C profile has the fastest maximum response pore water pressure, the C-C profile has the fastest response. Maximum pore water pressure. e gentle middle part is favorable for snow water infiltration. e seepage formed by hydraulic gradient has pointed to the middle and front of bank slope. e A-A section in the rear edge is slightly behind the B-B section. e pore water pressure near the slip zone is positively proportional to the response intensity of snow melting. When the snow melting intensity is higher, the variation curve of pore water pressure is always above of the middle

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Advances in Civil Engineering and back. e ice-snow is melting quickly day and night. e slope surface temperature is 0.1°C at 1 : 00 a.m. in the evening, and the amount of ice-snow melting is very small. At this time, the slope is partially drained. ere are many groups of cracks in the surface soil, and they form dominant infiltration channels. After noon tomorrow, the melting intensity and the infiltration rate increased. (3) It can be seen from Figure 9(c) that the soil thrust increases rapidly during the peak period of snowmelt. e change of soil pressure, slightly lagging behind, increases with the rise of reservoir water level. (i) At this time, the soil body at the depth of 80 cm on the surface of the bank slope is completely saturated. e sliding thrust at the front end of the slope can reach the peak value under the action of ice-snow melt water, which causes softening and strength reduced of the soil. After 96 hours of snow melt water infiltration, the sliding force of the No 4# soil is greater than its anti-sliding force, and the soil near the soil thrust sensor is unstable, as shown in Figure 10(a). (ii) e bank slope began to store water, and the slope toe was partially creeping and deformed. e earth pressure sensors of No 0# and No 2# at slope toe decreased in a small range. ere are two main reasons: ① e soil at the foot is carried away by the scouring of reservoir water and snow water, resulting in local soil flow, which leads to the reduction of the density l and the earth pressure. ② Sliding failure occurs in the front soil, and the squeezing force is reduced by soil. is will lead to the decrease in earth pressure.
(iii) e leading edge accumulation body is partially penetrated and dislocated, as shown in Figure 11(b). No 0#, No 1#, and No 2# earth pressure sensor. A large amount of snow water enters the cracks, resulting in the increase in soil bulk density, and the earth pressure obviously increases when the snowmelt intensity further increases. Finally, it leads to plastic flow. e earth pressure will decrease slowly with the loss of surface soil. (iv) When reservoir water level rises, the reservoir water infiltrates into the slope, the soil bulk density increases, the Earth pressure gradually increases, and the total stress of soil increases. e slope surface temperature is 0.1°C at 1 : 00 a.m. in the evening, and part of the water in the slope is discharged along the seepage channel. e soil bulk density decreases, and the earth pressure decreases slowly, as shown in Figure 9(c). e response of soil pressure to snow melting rate is consistent with that of pore water pressure. We can see that the higher the melting rate, the faster the infiltration; the increasing trend of earth pressure become more obvious.
(4) With the continuous development of reservoir water and snow melting, the surface displacement increases rapidly, as shown in Figure 9(d). Cracks of different scales appear in the slope, especially at the junction of ice-snow and reservoir water in the middle-front part. After 4 days, combined action of reservoir water and ice-snow melting occurs at the junction of ice and water in the middle and front. e disturbance is affected by the speed of ice-snow melting alternately. e 300 cm long crack was appeared, as shown in Figure 11(a). e No 3#and No 4# soil pressure sensors will increase significantly located in the failure area. When the intensity of snow melting increases, the plastic flow will eventually occur. e earth pressure will decrease slowly with the loss of surface soil.
From displacement monitoring curve, the deformation of slope has obvious zoning in time and space. At time， the deformation development is mainly concentrated after the saturated deformation of the shallow soil (continuous icesnow melting 50-110 h). e slope has no obvious large deformation failure. In space, the front edge becomes deformed severely and the deformation caused displacement, respectively, 7.56 mm and 9.93 mm; the middle part was 3.95 mm and 2.93 mm, and the posterior edge was only 1.2 mm and 1.15 mm. So, the large deformation occurs in the leading edge and middle. Combined with the displacement monitoring curve, it can be seen that there is a corresponding relationship between the change of soil pressure and the development of slope deformation.

Seepage-Erosion-Deformation
Process within Physical Model Test e ice-snow melting is more likely to occur in the erosion deformation of the soil mass inside the bank slope. e variation of fine particles content in the soil skeleton is due to the ice-snow melting. e shallow sliding mass in the east and west of the Outang landslide has good permeability. e change trend of groundwater level and reservoir level is synchronous, and the deformation is large. e soaking softening effect of reservoir water on sliding belt is quite obvious. e anti-slide force is obviously reduced. Creep occurs along the potential bedding slip surface due to stress adjustment. e shallow deformation areas in the east and west are seriously affected by the melting water of ice and snow. e deformation on the west side of the front edge is the most serious.
In this paper, the model test has two working conditions.
(1) Failure process on the west side of the front edge under the single action of ice-snow melting (2) e transverse crack deformation in middle front under the combined action of reservoir water and ice-snow melt water In this paper, the model test is characterized by creep deformation instability.

Seepage Erosion Equation of Soil.
e soil matrix of soils susceptible to suffusion is usually composed of mixed coarse and fine particles. Under certain geometric and hydromechanical conditions, the fine particles can be detached from the solid skeleton and behave as a part of the liquid phase in the form of liquidize fine particles, which can be transported away by the flowing liquid. To describe this fines migration process, unsaturated soils composed of mixed coarse and fine particles with their pore spaces filled by liquid or air are treated as a kind of three-phase multispecies porous media [38]. e loss of fine particles in the soil of bank slope leads to the change in microstructure of the soil. e nonlinearity of the permeability coefficient is a typical characteristic of the soil subjected to seepage erosion on the microscale. e overall erosion deformation of the bank slope surface is shown in Figure 12. Based on the theory put forward by Sterpi [39], the relationship between the density ρ e of erosion fine particles and the hydraulic gradient and time is established in accordance with the model test results. e erosion equation can be expressed as follows:

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Advances in Civil Engineering where ρ 0 is the initial fine particle mass density (mass of fine particles per unit volume, kg/m 3 ); t 0 refers to 1 h; and m, n, and p are all dimensionless test parameters. Equation (2) shows the response of the density for eroded fine particles under the condition of hydraulic gradient and time.

Failure Process of Slope Under the Single Action of Ice-Snow
Melting. e single action of ice-snow melting can be included with two working conditions. On the one hand, there is no water storage at the bottom of the reservoir. During the one-hour snow spreading from 6:00 to 7:00 in the morning of February 1, the ice and snow changed dynamically and the load gradually increased. On the other hand, the water rose from the bottom (0 cm) of the dam at the speed of 25 cm/h to the high water level at 100 cm within 4 hours from 7:00 a.m. to 11:00 a.m.
In the process of numerical simulation of unsaturated soil seepage, the following two aspects are mainly involved: (1) e permeability coefficient of the joint is adjusted by obtaining the saturation of the joint. (2) e relationship between matrix suction and water content in the process of soil moisture absorption and dehumidification is simplified to the same function, and the relationship between matrix suction and soil saturation can be thus obtained. e deformation of the leading edge on the left is shown in Figure 10.
Since an impermeable bottom is assumed for the slope, water can accumulate once reaching this boundary. At time t � 0.5 h, positive water pressure can be observed near the toe of the slope, and plastic shear strains begin to develop near this region. Along with the water infiltration, plastic shear strains develop and accumulate with time. At time t � 1 h, continuous localized plastic shear strains can be observed through the slope, which represents that a continuous slip surface has been developed. Slight deformation took place, and the failed mass starts to move downwardly under gravity.
Simulation of coupled seepage-erosion-deformation process within slopes. Soils in landslide deposits show the geometrical features which are susceptible to internal erosion under ice-snow melting infiltration. Upon seepageinduced erosion, fine particles will be transported from the middle part and surface of the slope to the toe and deeper part of the slope. e fines migration process will inevitably alter the characteristics of slope soils, which influences both the failure mechanism and the post-failure motion of the slope. e ice-snow melting induced failure process of an unsaturated slope comprised of soils prone to internal erosion is simulated with the coupled seepage-erosiondeformation. e slope model contains 10,240 material points which are distributed uniformly in a background grid of three material points per cell with the cell size of 1 mm × 1 mm. Both the right and left sides of the material point domain are prescribed with boundary for both solid and liquid phase, which prevents horizontal displacement and liquid flow; a fully fixed boundary for both solid and liquid phase is prescribed at the bottom to simulate a perfectly rough interface with the impermeable bedrock below; zero pore liquid pressure and concentration boundary conditions are assigned on the slope surface to trigger clean snow melting infiltration.
Retrogression can be observed after the full saturation of the slope. By using the analog computation coupled seepageerosion-deformation, the evolution of mass fraction of erodible fine particles and the volumetric concentration of liquidized-fines particles can be obtained. As can be seen, the internal erosion process developed along with the infiltration process, which led to severe fine particles decrease near the slope surface. Meanwhile, liquidized-fines particles are generated along with the erosion process, which are then

e Deformation under the Combined Action of Reservoir Water and Ice-Snow Melt
Water. e infiltration process of ice-snow melt water is simulated by adopting the saturatedunsaturated seepage analysis module, flow boundary conditions, and transient analysis method. e calculation results are saved every 10 minutes in the early stage of icesnow melt water and every 30 minutes in the middle and later stages, with the pore water pressure at the monitoring point recorded in real time simultaneously.
is paper analyzes the stability of the slope. e distribution of the seepage field and the location of the infiltration line in the slope are unknown. e only information given is that the infiltration line is exposed at the foot of the slope, and it is under the condition of still water at 100 cm. For the reservoir water at 100 cm and ice-snow melt water, the lower limit element type and upper limit element type are adopted, respectively. Furthermore, 10,240 elements and 3 grid adaptive iterations are adopted. As a part of the whole analysis, the calculation of seepage field is automatically done by the software. In addition, when seepage is introduced into the analysis, variables related to the seepage field are included in the adaptive control variables. e model process of unsaturated soil seepage is as follows: (1) Set the basic seepage material parameters. Set the icesnow infiltration boundary on the membrane unit, and set the water infiltration value according to the measured snow water intensity.
(2) e saturation of the unsaturated grid nodes is obtained by the built-in program language of the program, and then the matrix suction of the corresponding nodes is calculated by the fitted matrix suction formula, followed by the negative pore water pressure of the nodes assigned.
(3) e saturation of the element can be calculated by the weighted difference method on the basis of the node saturation obtained from the previous step based on which the relative permeability coefficient of the element is calculated and then assigned to the corresponding element. (4) rough the above correction of pore water pressure and permeability coefficient and traversing all nodes in this way, the seepage of unsaturated soil can be realized.
e seepage calculation of unsaturated soil can be carried out through the above four steps where the saturation is taken as the judgment basis for calculation. In specific, when the node saturation is less than 1, it shows that the node is in an unsaturated state, and the matrix suction and permeability coefficient can then be calculated by the above formula and assigned to the corresponding node unit; as the snow water infiltration soil gradually saturates, the pore water pressure of the saturated soil can be calculated according to the seepage, and the permeability coefficient of the saturated soil is then a constant value. Soil deformation of the slope surface at the snow and water interface is shown in Figure 11.
During the test process, the existence of cracks in the slope body was observed. erefore, elements with cracks are set in the slope body. According to numerical simulation, the failure process and the change processes of pore water pressure and horizontal soil pressure of the slope can be obtained.
e specific analysis results are illustrated in Figure 11(b).
It can be seen from the above that the soil mass of the slope has large transverse cracks on the surface at the front and middle of the ice and water junction, and the bank slope has been damaged. In the failure area, the isocline of soil pressure in horizontal direction is relatively dense, which indicates that the soil pressure in horizontal direction in this area changes significantly; when the slope is damaged, the horizontal soil pressure of soil near the sliding zone changes greatly and the isocline is relatively dense, which is caused by the failure of the soil in this area and the transition of the stress between the soil in the damaged area.
During the rise of reservoir water at the front edge, the part with the largest impact on the slope is the front part where the water can penetrate. ere is little change in the readings of the pressure sensors at the back edge and no hydrodynamic pressure. In the process of reservoir water rising, the hydrodynamic pressure and normal stress gradually increase. In the process of reservoir water rising, cracks are produced step by step, and the front slope appears creep, but no large-scale sliding occurs. e hydraulic gradients of combined action of reservoir water and ice-snow melting as well as the velocity fields are homogenous along the depth; therefore, homogenous erosion rates will be generated. In addition, the fine particles inside soils will be eroded until the fine content fraction reaches the ultimate fine content fraction which is also dependent on the ice-snow melting seepage velocity. e horizontal and vertical displacements gradually increase infiltration with the ice-snow melting. e influence area of snow melting infiltration on slope seepage field is concentrated in the slope toe and slope center; that is, the area formed by transient saturation region preferentially. e vector concentration at the toe of the slope means that obvious slip deformation has taken place. At the same time, the transient saturation zone is connected with the reservoir water level. e increase in pore water pressure caused by snow water infiltration. As a result, the effective stress at the toe of slope decreases， and the vertical displacement increases. Figure 11(c) is "water hammer" mechanism reflected in bank slope deformation-failure under combined action of reservoir water and ice-snow melting. e reservoir water rapidly inundates the ice-snow covered by the landslide front edge. At this time, the ice and snow rupture expansion area is directly connected with the reservoir water with high water head. e reservoir water rapidly penetrates into icesnow mass. e flow of reservoir water produces cracks on the ice surface, and the negative pressure area is formed by the fracture opening. e rapid inflow of reservoir water had driven the ice blocks on both sides to close quickly. After, because the ice-snow was quickly soaked in the reservoir water, the crack outlet was blocked due to poor discharge. e phenomenon of "water hammer" can be produced at this time. A large amount of excess pore water pressure with high water head is caused on the sudden ice and snow fracture surface. e 10 cm fountain had been ejected from ice and snow cracks. e ice and snow covered on the slope moves towards the reservoir water. Its leading edge bears the buoyancy of reservoir water, causing ice and snow mass to "break." e reservoir water rapidly penetrates into the ice and snow cracks under the water head difference of 100 cm. Because of the narrow crack at the outlet, blocking highspeed flow of water forms fountain. e mechanism of water hammer is of great significance to the sudden collapse of underwater rock and soil in front of the bank slope.

Update of Soil Particle Volume, Porosity, Saturation, and
Permeability. For update, the geometry structure of the soil skeleton and the deformation gradient were updated within each time step using the following equation: where dI n+1 sp is the incremental deformation gradient given as in which G n ip is the gradient function. e strain rates of both solid and liquid phases on particle V n si are calculated with the corresponding nodal velocities. e updated Jacobian of the transformation of the solid phase J n+1 p which is the determinant of the deformation gradient is as follows: in which we determine the current volume and porosity: where V 0 p is the initial particle volume prior to any deformation. It is usually expressed as a function of both suction (p n+1 Lp ) and porosity (n n+1 p ) in case of large deformations, and S n+1 Lp is the saturation.
e updated porosity and saturation were obtained, and the current permeability of each particle would be updated with constitutive law dependent on the porosity and saturation.

k n+1
Lp � k 0 L k r S n+1 Lp , n n+1 where k 0 L is the initial soil hydraulic conductivity. e erosion law, which is adopted to govern the internal erosion process in this research, is developed based on model test results, shown in Figures 11(a) and 11(b). In this simulation, the hydraulic gradients as same as the velocity fields are homogenous with the depth; therefore, homogenous erosion rates will be generated, which lead to homogenous fine content distributions within the soil specimens. e evaluation profiles of the eroded fines mass ratio in the specimens under different constant seepage velocities are presented in Figure 13.
As can be seen, consistent with the erosion model, the erosion rate increases with the applied hydraulic gradient (seepage velocity), and the fine particles inside soils will be eroded until the fine content fraction reaches the ultimate (long term) fine content fraction which is also dependent on the seepage velocity.
e OPTUM-G2 simulation replicates the results as well as the experimental results quite well. Note that the discrepancy in the erodible mass between the numerical and the experimental results is due to the inaccuracies in the ultimate mass fraction curve. In our coupled OPTUM-G2 framework, the internal erosion effect is mainly accounted for the porosity change. In the model, two contributions for the porosity change can be identified, the skeleton deformation and the interphase mass transfer of fine species, which are difficult to be separated in the experiment. In this example, to validate the implementation of this seepage-erosion module, the skeleton deformation is assumed to be restricted. Accordingly, the porosity varies only with the internal erosion process. As shown in Figure 13, the porosity profiles simulated by the OPTUM-G2 almost overlap with the ones obtained by test values, which are proportional to the erosion process.

Quantitative Analysis of Creep Damage.
e creep displacement of landslide is essentially the damage and deformation evolution of rock and soil. Creep type slope refers to that under the action of gravity, and the sliding deformation soil mass has obvious creep characteristics; that is, deformation has the characteristics of slow evolution with time. is kind of slope is a dynamic development process from stable deformation to instability failure. e stress and strain develop continuously with time, and the deformation development lasts for long time.
e larger creep deformation occurs before the instability. e displacement changes the physical mechanical properties and slip boundary conditions. ere are three stages from initial displacement to slope failure. ere are initial creep stage, isokinetic creep stage, and accelerated creep stage. Different deformation stages have different deformation evolution characteristics and damage mechanism. e evolution of landslide is essentially the process of damage and deformation. e model test is carried out on creep slope with constant gravity field. Slope creep displacement and creep law decide the damage variable of bank slope. We quantitatively analyzed the slope displacement and slope damage variables. We established the quantitative relationship between damage variable and creep displacement of slope. e creep displacement of slope is produced under icesnow melting influent load. e slope material is weakened Advances in Civil Engineering due to water seepage erosion and time creep effect, resulting in irreversible creep and plastic deformation.
In this study, the hydraulic gradient changes from 0.53 to 0.66, which is greater than critical hydraulic gradient, and internal erosion will occur in landslide. e corresponding internal erosion control equation is the relationship between the porosity of soil mass, the mass of eroded particles, and the loss rate of fine particles.
Internal erosion under combined action of reservoir water and ice-snow melting occurs, and the fine particles are separated from the soil skeleton. In this hypothesis, the velocity of movement is consistent with the water flow. Cividini [40] proposed that the continuity equation of internal erosion is obtained by the law of conservation of mass: where ρ t is the density of eroded fine particles; v i is the moving speed of eroded particles in I direction; q e is the rate of erosion per unit volume of fine particles; and q d is the rate of deposition of eroded particles into the soil skeleton. When fine particles are eroded, fine particles flow with water. Density of eroded soil particles ρfs is as follows: which were calculated from equations 10 and 9; continuity governing equation of internal erosion is as follows: e seepage state in soil is very complex, and Darcy flow, non-Darcy flow, and dominant flow can exist at the same time. Equations describing the seepage state of soil are also different. But, in the early stage of internal erosion, Darcy flow is the main seepage in soil.
Based on the Carman-Kozeny equation, the relationship between saturation permeability coefficient K s and porosity n 0 is as follows: where n 0 is the initial porosity; ks0 is the initial saturated permeability coefficient; and n is the porosity of soil after snow water infiltration. Ice-snow melting intensity is closely related to the deformation and failure mode of landslide.

e Deformation Mechanism of Bank
Slope. Based on the above analysis, the bank slope deformation analysis model under the combined action of ice-snow melt water and reservoir water is built. In addition, the deformation and failure mechanism of bank slope under the combined action of icesnow melt water and reservoir water are thus expounded.
(1) Under the condition of ice-snow melting, the existence of cracks enhanced the infiltration capacity and the infiltration path of the slope soil. e snow water infiltrated from the fissure to both sides and the surface of the slope. e fissure layer was then saturated, and the stability was obviously reduced, as shown in Step 1 of Figure 12.
(2) With the increase in crack depth of slope surface soil, the vertical range of the saturated area was directly affected. e width of the crack opening mainly affected the boundary size of the ice-snow melt water. e deeper the crack was, the larger the saturated area was and the lower the slope stability was, as shown in Step 2 of Figure 12.

Advances in Civil Engineering
(3) e distribution of the cracks would affect not only the stability of the slope but also the condition of the sliding surface. e cracks were distributed in the middle and front parts of the slope. Ice-snow melt water was easy to cause shallow damage and had a great influence on the stability of the slope where cracks are distributed, as shown in Step 3 of Figure 12. (4) e speed of ice-snow melting mainly affected the saturation speed of the fracture soil on the surface. e saturation area of fracture layer increases with the extension of ice-snow water holding time, while the slope stability decreased with the increase in icesnow water melting strength. Finally, erosion and sliding deformation of the bank slope surface occurred, as shown in Step 4 of Figure 12.
During the day, the speed of ice and snow melting is faster than that at night. When the temperature is below 0°C, the icesnow will not melt. e snow melting speed changes with the temperature during the whole day. e degradation of soil medium mechanics and seepage characteristics caused by ice and snow melting and freeze-thaw will inevitably cause the expansion of infiltration depth and saturation range of ice and snow melting water, especially the irreversible damage. At the peak of ice-snow melting water, the saturation range of icesnow melting water will be further expanded; the seepage pressure will be increased; the groundwater level will be raised; and the deformation damage will be intensified. As a whole, there is no obvious deformation and failure of the slope except for small denudation and collapse in the saturated area, as shown in Figure 14.

Discussion
In this paper, the soil material are assigned with the same material parameters, including the ones for Mohr-Coulomb model, Darcy seepage flow, internal erosion law, and soil water retention curve.
An erosion law is necessary to describe the phase transfer rate of solid fine particles to liquidize fine particles. Most of them are empirical relations which relate the erosion rate to the flow characteristics (velocity and hydraulic gradient), porosity, fines density, and empirical erosion coefficients. In this study, the variation of fine particles content in the soil skeleton is assumed to be due only to the suffusion. e erosion law [41] is chosen to calculate the fines variation rate at pore surfaces.  e surface soil temperature is higher than that of indoor air temperature. e process of ice-snow melting is from the bottom to the top of the contact layer between ice and soil. In this paper, the complex ice-snow melting runoff process is conceptualized as the water tank connection relationship of water storage outflows from bottom to top. With the storage depth and the outflow of the side hole and the outflow of the bottom hole [42], calculate the runoff, concentration, and infiltration. e temporal and spatial distribution of icesnow melting is complex. e water tanks in series are arranged, with simulation of runoff process of ice-snow melting [43]. e theoretical diagram of water tank infiltration is as shown in Figure 15. e landslide soil is supposed to be a homogenous clay soil, whose fine particles can be eroded upon snow-ice melting infiltration.
e Mohr-Coulomb model using Bishop's effective stress [44,45] presented is adopted to capture the soil failure behavior, and the V-G equation is adopted as the soil water retention law: in which S L is the liquid saturation; S c and S ref are the matric suction and the reference suction values; S min is the minimum (residual) saturation can be reached; and b v and m v are fitting parameters. e impact of the variation of porosity on the intrinsic permeability relies on the liquid permeability on the level of saturation [46,47], as in the following power law:

Conclusions
is paper is based on the three-dimensional landslide test platform. According to the landslide prototype and the similarity theory, a large-scale physical model test was constructed. e deformation characteristics and influence mechanism of landslide are studied under the action of reservoir water level rise, ice-snow melting, and their combination. e conclusion is as follows: (1) In the early stage of water level rise, the effective stress increases the formation of seepage pressure in the slope. When the landslide mass is deformed and damaged, the response of pore water pressure and earth pressure of shallow soil is obvious, and when the deformation and failure of landslide occur, the sensor response lags in slope.
(2) Directly affected by reservoir water, the soil at the front edge of the bank slope is saturated rapidly under the action of ice-snow melt water, the shear strength is greatly reduced, with deterioration of stability. After, the edge is steeper due to continuous infiltration of snow-ice melting, the glide force increases and the downward penetration force is larger. During snowmelt infiltration, with the increase in pore water pressure, the shear strength gradually decreases; on the upper side of the failure zone, tensile cracks will occur; the lower side of the soil swells due to the extrusion, and local flowing soil will occur at the foot of slope. (3) In this model test, the infiltration of ice and snowmelting is the key factor to induce the deformation and instability of accumulation landslide. e icesnow melting intensity will increase the pore water pressure and the earth pressure. In the accelerated deformation stage, pore water pressure and soil pressure are fluctuated abnormally frequently. It is the sign of slope instability, which provides a certain reference for landslide early warning and prediction. (4) e formation of tensile cracks is the most fundamental reason to accelerate the creep deformation and failure of accumulation landslide. After 3 days of joint action, the surface soil has shallow erosion deformation. After 4 days of ice and snow melting, obvious thorough creep sliding deformation and failure occurred in the left part of the front edge of the bank slope. After 5 days of combined action, it is affected by the disturbance caused by the rate of ice and snow melting alternately day and night. ere are large transverse cracks in the front and middle parts of the slope; under the transverse cracks, there are some areas of thorough dislocation failure area. During a period of time after the end of ice-snow melting on the surface of the bank slope, under the joint action of reservoir water, the pressure head of local slope did not obviously decrease. It may continue to increase due to the influence of reverse osmosis and dynamic water cycle effect, and creep deformation occurs on the bank slope. (5) e response law of pore water pressure and earth pressure and the deformation and failure mode of slope with different profiles, depths, and snowmelt intensities are studied. e response time of pore water pressure and soil pressure to snow melting intensity is positively proportional to the snow melting intensity.
Data Availability e test data are included within the article and are available from the corresponding author upon request.

Conflicts of Interest
e authors declare that they have no conflicts of interest regarding the publication of this paper.