A steady‐state analytical slope stability model for complex hillslopes

Talebi, Ali; Troch, P. A.; Uijlenhoet, R.

doi:10.1002/hyp.6881

Cited by 59 publications

(69 citation statements)

References 19 publications

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“…In general, occurrence of the saturation zone in hillslopes causes an increase in pore pressure followed by a decrease in the stability of hillslopes. Talebi et al (2008a) proved that the stability of the convergent hillslope is less than the divergent ones and the same is true about the concave hillslopes compared with the convex ones.…”

Section: Calculation Of the Saturation Zone Length In The Nine Basic mentioning

confidence: 85%

“…The soil moisture storage capacity (S c ) has been defined by Fan and Bras (1998) Talebi et al, 2008a) as:…”

Section: The Hillslope-storage Kinematic Wave Equationmentioning

confidence: 99%

“…This parameter was also used by Troch et al (2002) and Talebi et al (2008a) in their research. Figure 4 shows variations of the relative saturation along the nine basic hillslopes of Tables 1 and 2 for different recharge rates.…”

Section: Calculation Of the Saturation Zone Length In The Nine Basic mentioning

confidence: 99%

“…Troch et al (2003) and Hilberts et al (2004) demonstrated that (numerical) solutions of the 1D hillslope-storage Boussinesq (hsB) equation account explicitly for plan shape (by means of the hillslope width function) and profile curvature (local bedrock slope angle and hillslope soil depth function) of the hillslope. To investigate the key role of geometric characteristics of hillslopes (plan shape and profile curvature) on shallow landslides, Talebi et al (2008a) presented a steadystate analytical hillslope stability model based on kinematic wave subsurface storage dynamics. Comparison between the hillslope-storage Boussinesq and Richards' equation models for various scenarios and hillslope configurations shows that the hsB model is able to capture the general features of the storage and outflow responses of complex hillslopes Hilberts et al, 2004).…”

Section: Introductionmentioning

confidence: 99%

“…1. (a) A three dimensional view of a convergent hillslope overlying a straight bedrock profile, (b) a definition sketch of the cross section of a one-dimensional hillslope aquifer overlying a bedrock with a constant bedrock slope angle (after Talebi et al, 2008a).…”

Section: Introductionmentioning

confidence: 99%

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A steady-state saturation model to determine the subsurface travel time (STT) in complex hillslopes

Sabzevari

Talebi

Ardakanian

et al. 2010

Hydrol. Earth Syst. Sci.

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Abstract. The travel time of subsurface flow in complex hillslopes (hillslopes with different plan shape and profile curvature) is an important parameter in predicting the subsurface flow in catchments. This time depends on the hillslopes geometry (plan shape and profile curvature), soil properties and climate conditions. The saturation capacity of hillslopes affect the travel time of subsurface flow. The saturation capacity, and subsurface travel time of compound hillslopes depend on parameters such as soil depth, porosity, soil hydraulic conductivity, plan shape (convergent, parallel or divergent), hillslope length, profile curvature(concave, straight or convex) and recharge rate to the groundwater table. An equation for calculating subsurface travel time for all complex hillslopes was presented. This equation is a function of the saturation zone length (SZL) on the surface. Saturation zone length of the complex hillslopes was calculated numerically by using the hillslope-storage kinematic wave equation for subsurface flow, so an analytical equation was presented for calculating the saturation zone length of the straight hillslopes and all plan shapes geometries. Based on our results, the convergent hillslopes become saturated very soon and they showed longer SZL with shorter travel time compared to the parallel and divergent ones. The subsurface average flow rate in convergent hillslopes is much less than the divergent ones in the steady state conditions. Concerning to subsurface travel time , convex hillslopes have more travel time in comparison to straight and concave hillslopes. The convex hillslopes exhibit more average flow rate than concave hillslopes and their saturation capacity is very low. Finally, the effects of recharge rate variations, average bedrock slope and soil depth on saturation zone extension were investigated.

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Section: Calculation Of the Saturation Zone Length In The Nine Basic mentioning

confidence: 85%

“…The soil moisture storage capacity (S c ) has been defined by Fan and Bras (1998) Talebi et al, 2008a) as:…”

Section: The Hillslope-storage Kinematic Wave Equationmentioning

confidence: 99%

Section: Calculation Of the Saturation Zone Length In The Nine Basic mentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

See 3 more Smart Citations

A steady-state saturation model to determine the subsurface travel time (STT) in complex hillslopes

Sabzevari

Talebi

Ardakanian

et al. 2010

Hydrol. Earth Syst. Sci.

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A low‐dimensional physically based model of hydrologic control of shallow landsliding on complex hillslopes

Talebi

Uijlenhoet

Troch

2008

Earth Surf Processes Landf

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Hillslopes have complex three-dimensional shapes that are characterized by their plan shape, profile curvature of surface and bedrock, and soil depth. To investigate the stability of complex hillslopes (with different slope curvatures and plan shapes), we combine the hillslopestorage Boussinesq (HSB) model with the infinite slope stability method. The HSB model is based on the continuity and Darcy equations expressed in terms of storage along the hillslope. Solutions of the HSB equation account explicitly for plan shape by introducing the hillslope width function and for profile curvature through the bedrock slope angle and the hillslope soil depth function. The presented model is composed of three parts: a topography model conceptualizing three-dimensional soil mantled landscapes, a dynamic hydrology model for shallow subsurface flow and water table depth (HSB model) and an infinite slope stability method based on the Mohr-Coulomb failure law. The resulting hillslope-storage Boussinesq stability model (HSB-SM) is able to simulate rain-induced shallow landsliding on hillslopes with non-constant bedrock slope and non-parallel plan shape. We apply the model to nine characteristic hillslope types with three different profile curvatures (concave, straight, convex) and three different plan shapes (convergent, parallel, divergent). In the presented model, the unsaturated storage has been calculated based on the unit head gradient assumption. To relax this assumption and to investigate the effect of neglecting the variations of unsaturated storage on the assessment of slope stability in the transient case, we also combine a coupled model of saturated and unsaturated storage and the infinite slope stability method. The results show that the variations of the unsaturated zone storage do not play a critical role in hillslope stability. Therefore, it can be concluded that the presented dynamic slope stability model (HSB-SM) can be used safely for slope stability analysis on complex hillslopes. Our results show that after a certain period of rainfall the convergent hillslopes with concave and straight profiles become unstable more quickly than others, whilst divergent convex hillslopes remain stable (even after intense rainfall). In addition, the relation between subsurface flow and hillslope stability has been investigated. Our analyses show that the minimum safety factor (FS) occurs when the rate of subsurface flow is a maximum. In fact, by increasing the subsurface flow, stability decreases for all hillslope shapes.* This parameter has been calculated for a slope angle β = 15° (β/φ = 0·5). 1968A. Talebi, R. Uijlenhoet and P. A. Troch Figure 3. Variations of the safety factor on hillslopes with different plan shapes computed using the original HSB model (solid line) and the coupled HSB model (dashed line), assuming β = 0·5φ and N = 20 mm d −1 . Top panel, convergent; middle panel, parallel; bottom panel, divergent hillslope (profile curvature is constant).quickly. In contrast, in the divergent hillslopes (Figure 4, nos 3, ...

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Stability of supraglacial debris

Moore

2017

Earth Surf Processes Landf

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Rock debris on the surface of ablating glaciers is not static, and is often transported across the ice surface as relief evolves during melt. This supraglacial debris transport has a strong influence on the spatial distribution of melt, and is implicated in the formation of hummocky glacial topography in deglaciated terrain. Furthermore, as ice-dammed lakes and ice-cored slopes become increasingly common in deglaciating watersheds, there is rising concern about hazards to humans and infrastructure posed by mass-wasting of ice-cored debris. The existing quantitative framework for describing these debris transport processes is limited, making it difficult to account for transport in mass balance, hazard assessment, and landscape development models. This paper develops a theoretical framework for assessing slope stability and gravitational mass transport in a debris-covered ice setting. Excess water pressure at the interface between ablating ice and lowering debris is computed by combining Darcy's law with a meltwater balance. A limit-equilibrium slope stability analysis is then applied to hypothetical debris layers with end-member moisture conditions derived from a downslope meltwater balance that includes production and seepage. The resulting model system constrains maximum stable slope angles and lengths that vary with debris texture, thickness, and the rate of meltwater production. Model predictions are compared with field observations and with digital elevation model (DEM)-derived terrain metrics from two modern debris-covered glaciers on Mount Rainier, USA.

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A steady‐state analytical slope stability model for complex hillslopes

Cited by 59 publications

References 19 publications

A steady-state saturation model to determine the subsurface travel time (STT) in complex hillslopes

A steady-state saturation model to determine the subsurface travel time (STT) in complex hillslopes

A low‐dimensional physically based model of hydrologic control of shallow landsliding on complex hillslopes

Stability of supraglacial debris

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