the Creative Commons Attribution 4.0 License.
the Creative Commons Attribution 4.0 License.
Finitehillslope analysis of landslides triggered by excess pore water pressure: the roles of atmospheric pressure and rainfall infiltration during typhoons
Lucas Pelascini
Philippe Steer
Maxime Mouyen
Laurent Longuevergne
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 Final revised paper (published on 05 Oct 2022)
 Preprint (discussion started on 16 Nov 2021)
Interactive discussion
Status: closed

RC1: 'Comment on nhess2021340', Anonymous Referee #1, 07 Jan 2022

AC1: 'Reply on RC1', Lucas Pelascini, 15 Mar 2022
Review of “Modelling the control of groundwater on landslides triggering: the respective role of atmosphere and rainfall during typhoons”
Summary:
In this contribution, Pelascini et al. examined the effects of pore pressure changes due to atmospheric pressure and rainfall infiltration on the stability of hillslopes of finite length. Here the MohrColoumb failure criterion was the conceptual basis of stability, though throughout the paper, emphasis was placed on pore pressure components of the effective stress rather than the failure criterion. Timeevolution of pore pressure at the hillslope crest and toe were calculated by convolving analytical solutions for groundwater flow and diffusion of pore pressure with synthetic and real timeseries of rainfall and atmospheric pressure. The results showed that the importance of the two dynamic pore pressuregenerating mechanisms (atmospheric pressure and infiltration) varied in space on the slope, largely driven by differences in depth to the water table, and in time depending on the mechanism’s response timescale. The results suggest that more attention should be paid to slope stability effects of atmospheric pressure fluctuations in large storms, and that estimates of landslide timing in relation to pressure fluctuations and precipitation could help distinguish drivers of landslides.
We are grateful to the referee for this detailed and precise comments on the preprint.
My experience makes me most suited to comment on the groundwater hydrology aspects of this paper, rather than the landslide hazard component. In this respect I have a few concerns.
 The hydrological model used in this paper is a combination of a DupuitForchheimer (DF)
aquifer model and a onedimensional infiltration model based on the Richards equation. After
reading the paper I was left unclear on how exactly these two models interact, and what effects the transient component of the water table response has on their results.
 There needs to be more careful attention paid to the relationship between this hydrological
model and the expected groundwater dynamics of the landscapes the model intends to capture.(Steep landscape hillslope hydrology see e.g. Montgomery et al. (1997)). The linearized, horizontalbased form of the DF model may be appropriate in low relief settings or for deep aquifers that respond slowly to recharge, but the landscapes considered here are steep, and recharge here is assumed to infiltrate instantaneously to the water table.
 The two hydrological models operating together contain potentially contradictory information
on the pore water pressure below the water table.
While I recognize that issues 2 and 3 are acknowledged in Discussion section 5.1, it seems that most of the paper does not meaningfully engage with these limitations. If the authors retain the current
hydrological model, rationale and limitations of the model need to be more clearly stated up front in the introduction and methods sections. While I cannot comment on the novelty of the landslide hazards component of this paper, I was left with the impression that there is merit to exploring the processes they consider here, though I think the hydrological basis of this work could use more thought. I’ve added more details in the linebyline notes below.
Our goal was to better understand the specific (physical) controls of rainfall and atmospheric pressure changes on landslide triggering.
In geomorphology, the 1D diffusion model (Iverson model) remains as a reference for rainfalldriven landslides. Though, this model has strong limitations (infinite slope, i.e. local point of view, inability to consider both recharge and GW upflow, define initial conditions …) and therefore difficult to use at hillslope scale.
Our point of view was to develop a simple model, as simple as the original Iverson model, which could better represent groundwater dynamics under hydrological and atmospheric boundary conditions. As a consequence, we are far from the quality of a “site model”, as we rather define physical controls. Following this work, we are now setting up a modflowbased model on a Taiwanese catchment, driven by a landsurface model, to better represent actual groundwater flow, and also interception with the surface.
It appears the goal of the paper is not stated clearly enough, and this causes confusion for the reader. Some clarifications are indeed needed and will be added in the first parts of the manuscript. The goal is here to consider the water table variations through a simple analytical model in order to improve slope stability assessments.
 The DupuitForchheimer (DF) model considers horizontal flows and defines the water table surface. The 1D diffusion models allows for the computation of pressure propagation through the groundwater. The two models do not interact, the rainfall pressure diffusion feeds on the output of the DF model.
 Additional explanations are provided lines 8891, 150152, 175177 and figure 1 has been modified to further illustrate how the models are implemented.
 The hydrological model here is indeed basic. It is based on the hypothesis of negligible vertical flow, which might be suitable for thick aquifers and/or low angle slopes. The hypothesis might not be valid in Taiwan. While this doesn’t represent the complexity of the geology for the slopes in Taiwan, it has been deemed necessary to keep the model simple.
 We clarify this when we introduce the hydrogeological model (lines 121126)
 The two pore pressure diffusion models indeed predict different pore pressures in response to the different forcing, but the solution of the diffusivity equation can be added by linearity. Physically this can lead to a pressure gradient and groundwater flows in two opposite directions.
 This limitation of the model is addressed in the discussion (lines 351354).
Line by line:
Title:
Title feels a little unspecific – what about the atmosphere, and what about groundwater? Could I
suggest something along the lines of: “Finitehillslope analysis of landslides triggered by excess pore
water pressure: the roles of atmospheric pressure and rainfall infiltration during typhoons”
We agree with this comment and have changed the title accordingly.
Abstract:
Two things in the abstract seem contradictory to me. Please reconcile or clarify the following:
Lines 1011 you state that “atmospheric pressure changes and rainfall induced groundwater level
change can generate pore pressure changes with similar amplitude,” but then in line 1718, you say they differ by perhaps several orders of magnitude.
Thank you for pointing this out. When thinking about pressure change, 10 hPa atmospheric pressure change is equivalent to a 100mm rainfall event. Therefore, atmospheric effects can generate similar pore pressure amplitudes as rainfall, in some specific cases. However, the rainfall effects generally reach values of pore pressure orders of magnitude above the atmospheric ones because the latter is function of the derivative of the atmospheric pressure, and atmospheric pressure rarely drops in an instant. The sentence line 12 has been modified to prevent this potential confusion.
Lines 1415 you state that “rainfall infiltration and atmospheric pressure variations” are described by
diffusion equations, but then in line 18 you say the effects of atmospheric pressure are instantaneous. This may be a matter of the phrasing, but it is confusing.
The phrasing can indeed be confusing. Both rainfall and atmospheric effects are described with diffusion equations. However, the atmospheric effect is instantaneous due to the transfer of the pressure load from the atmosphere to the pores through the skeleton or solid phase of the medium. The decay of this change in pore pressure is described with diffusion equations. This is now clarified lines 1820.
Introduction:
Line 31: “cumulated rainfall” > “groundwater recharge”
Done
Line 38: “Little attention has been by received by this potential slope destabilisation factor” > “This
slope destabilisation factor has received little attention.”
Done
Line 40: “…modifying slope stability.” Citation?
The work that was been referred to here was Schultz et al. (2009), and the citation has been added.
Line 5556: “As both rainfall and atmospheric effects implies pore pressure diffusion in groundwater, the link to slope stability requires a specific model.” This sentence seems vague to me.
The sentence has been clarified (lines 5758).
Line 59: “allows us to define”
Done
Line 62: remove “about”
Done
Methods:
Line 65: Not sure what “homogenous half space” means and it is not mentioned anywhere else in the
text.
“Infinite homogeneous slope” might be more selfexplanatory indeed.
Line 90: “Under rainfall constrain” ?
“under rainfall forcing”
Line 101: “hydrogeological model” usually refers to a model of the characteristics of an aquifer – it’s
permeability, porosity, stratigraphy and composition (e.g., Condon et al. 2021 5.1). Maybe hydrological model would be better?
We agree, “hydrological model” is more appropriate since no assumption on the structure and stratigraphy are made.
Line 101: I would use “slope” or “topographic slope” over “dip,” because dip has a different geologic
meaning.
Done
Line 104: Interesting, I have not seen this called the diffusivity equation before. Looking around online, it seems this term is more commonly applied in the petroleum industry to other fluids? In hydrology I see this called the Boussinesq equation (e.g. Troch 2013, paragraph 9, Boussinesq equation for horizontal aquifers) or simply the DupuitForchheimer equation.
We used the term diffusivity equation by default since it describes this physical phenomenon, but indeed, it is generally named after Boussinesq in hydrology. It will therefore be referred to as Boussinesq’s equation in order to fit the hydrology community convention.
Line 110: “storage” > “storage coefficient”
Done
Line 112: “in term of” > “in terms of”
Done
Line 119, 130: “in function of” > “as a function of”
Done
Line 131: It's unclear to me whether you use this solution, given the discussion in 2.3, where it seems
that only h_s matters. Does the static pressure head in response to recharge come into effect in your
model?
This comment corresponds to the same issues raised in the general comment #1. The models needed to be presented with more clarity. The static position h_s of the water table is taken into account to define the water table initial position. The water table level is then updated using the transient solution h_t. The static pressure head (due to h_s) does not create dynamic pore pressure, and is not investigated in this study. Indeed, the focus of this work is the dynamic transient effects – this is why the slope is considered at yield – an no absolute values of safety factor are computed. We deliberately only modelled the transient/dynamic effects due to changes in water table level h_t inducing new loadings. These loadings are then fed into the diffusion model to propagate in depth.
 Precisions have been added lines 150152, and the use of transient water table into the rainfallinduced pore pressure diffusion model is explained lines 175177 with the help of a new graph in Fig. 1.
Line 135: This sounds you are disregarding the transient component of the water table variation in the DupuitForchheimer model? Or are you only disregarding its affect on pressure head and not on water table position?
This is answered in the previous comment.
Lines 137138: It is not necessarily described by diffusion. In Iverson (2000) there are extensive
assumptions and conditions required to reduce the Richards equation to this particular 1D diffusion
form. These need to be identified and discussed.
Indeed, the propagation of pore pressure can be described by pressure diffusion – which is what Iverson proposed in his model, under the main hypothesis of an infinite slope geometry, and wet initial conditions, so that there are no changes in hydraulic conductivities above and below the water table. Then flow is described using Richard’s equation and reduced to a onedimensional diffusion equation.
 These hypothesis are now mentioned line 157.
Line 138: “characterise” > “characterised”
Done
Line 139: “model considered a 2D mode” Model? Consider rephrasing to avoid repetition.
Done
Line 141: “onedimension” > “onedimensional”
Done
Lines 148149: Could you more clearly state the boundary conditions to arrive at this solution? The
constant loading gives the surface boundary condition, what is the condition at depth? Seems like this solution is not accounting for the water table depth?
The upper boundary condition at the surface is a Neumann condition (known flow). There is no lower boundary condition, the solution used here is for the diffusion through a semiinfinite solid (therefore no lower boundary), as the aquifer is taken with a sufficient thickness for the horizontal DF model and its lower boundary can be considered at infinity with regards to the depths investigated here.
 We now clearly state the boundary conditions of the model lines 165166
Line 152: tc = z2/D should this be \hat{D}?
The characteristic time, as presented in several studies (Iverson, 2000; Handwerger et al., 2013), is indeed tc = z2/D . Its definition has been rewritten in a clearer manner lines 161163.
Line 154: “convoluted” > “convolved”
Done
Line 167: Again more clearly state lower boundary condition.
As for the commentary relative to lines 148149, there is no lower boundary condition, it is considered to infinity. The upper boundary this time is a Dirichlet condition. As for the previous commentary, additional explanation as well as more precise citation are provided lines 192193.
Line 168: change citation type to “Carslaw and Jaeger (1959)”
Done
Figure 1:
Can you label hydraulic head h?
Done
Results – Synthetic:
Line 176: “toe of and at the very top of” I would call the top either crest or ridge.
Required changes have been done, the top of the slope is now been referred as crest in the manuscript.
Line 177: I think some more elaboration of this consideration of the slope at yield is needed. It seems
critical to how your are interpreting the results.
Yes, this is a critical part in this study. The slope is considered at yield in order to investigate only dynamic variations and not static effects (as already discussed in response to the commentary on line 131). This is done so that the results of the models are not dependent on the intrinsic mechanic and topographic properties of the slope. We have clarify that in the manuscript. A discussion about the reason why we consider a slope at yield has also been added in the description of the failure mechanism lines 9294.
Line 183: Don’t need the figure description in parenthesis.
Indeed, this was a mistake and should not have appear here.
Line 185: “an 86.4 mm cumulated rainfall” > “86.4 mm of accumulated rainfall”
Done
Line 197: Underestimation of tc… Can you provide more insight into the physical meaning of tc here?
Semantically, it also seems to me less that tc is underestimated, and more that it may not be the right quantity for comparison with the timescale estimated.
We fully agree with this remark. The characteristic time tc is not really appropriate to these comparisons. It represents the minimum time at which a strong pore pressure occurs at the depth z, which is why it is compared to the maximum response time. However, Handwerger et al. (2013) showed it corresponds to “the time 48% of the surface forcing is felt at a given depth”. It still gives an idea of the timing of the diffusion. The definition and a discussion about tc is provided lines 221224.
Line 200: “slop” > “slope”
Done.
Line 214: Still unclear exactly how the water table rise during event is incorporated into your model.
This is the same issue as addressed in the general comment #1 and the comments concerning lines 131 and 135. The description of the models is clarified.
Results – Application:
Line 247: “east of Taiwan” > “eastern Taiwan” or “the east of Taiwan”
Done
Line 251: “inferior to” > less than
Done
Line 255: “contrasted” > contrasting
Done
Line 257: remove “has”
Done
Figure 5: Great plot on the left – I like how your selected storms are a kind of envelope around the
extreme events.
Section 4.2:
 How did you select hillslope length? How sensitive are results to hillslope length? Can you use your
analytical solutions to show something about this?
The hillslope length L, in the equations presented by Townley (1995) does not have an influence on the form of the static water table. Only the position along the hillslope – namely the parameter x/L – impacts the water table response. The transient water table variation would keep the same form but see its response time changing accordingly to the diffusion characteristic time over the full hillslope length L²/D. The hillslope length has been set as 500 m as it seems to represent hillslopes in Taiwan quite well (Fig. 8 (a)). We now discuss the scale of the hillslope lines 525529.
 Is there evidence in the literature or in published well/piezometer data that hillslopes fully saturate
during typhoons?
To our knowledge, no study or data monitoring water table of hillslopes undergoing typhoons with high spatial and temporal resolution exist. But this is a very important question and we are exploring whether sentinel satellites can define such behaviour.
 Provide the equation for the infinite slope model used for comparison
The equation of diffusion of pore pressure for the infinite slope model is the same as the one used in the finite hillslope model (equations 7 and 8), as specified in the manuscript. It does not seem necessary to provide the equation a second time.
 Can you say anything from your model about which storms cause landslides and which ones don’t?
The model shows the greatest rainfallinduced pore pressure are achieved when weather events strike hillslopes with a deep water table level, which allow for large water table variations. The atmospheric effect is more pronounced when the drop of atmospheric pressure is rapid. Therefore, according to the model, a sudden and violent storm occurring after a drought period is the most prone to trigger a landslide. On the other hand, a storm striking a fully saturated hillslope with a gradual drop of atmospheric pressure is less likely to cause slope failure. However, this model does not take the static components of the safety factor into account, nor the seepage forces, and these might cause a fully saturated hillslope to fail.
Line 278: you say “amount of rainfall” which to me implies rainfall depths, but rates are given. I would make these agree.
Values given are indeed rates. They correspond to the mean rate during the past 6 months before the typhoons. The sentence has been corrected.
Line 290: “caps off” colloquial language, consider replacing
Done
Line 296: “in function of the event” what does this mean?
We have rephrased as: “depending on the event”
Figure 6: The use of black and blue together in plots bi is difficult to read. I would choose a better color contrast.
Done
Discussion:
Line 314: “models limitations” > “model limitations”
Done
Line 315: “considered in this study consider” rephrase
Done
Line 355: “has been” > was
Done
Line 365: Worth mentioning in this section that the diffusivity in the 1D model is Iverson (2000)’s
maximum hydraulic diffusivity, derived for conditions near saturation.
Hydraulic diffusivity in Iverson’s model is indeed the maximum hydraulic diffusivity, and is the diffusivity considered along this paper. This is added in the description of the rainfallinduced diffusion model (Sec. 2.3), line 160.
Line 385: Can you provide some more physical insight here on why diffusivity affects these in opposite ways?
The impact on diffusivity on each effect is developed and explained just above, and it doesn’t seem to require any modifications in that way.
Line 392: When considering only these two effects. Do you think atmospheric pressure effects could be more important than other mechanisms going on when hillslopes fully saturate, like seepage? (Found this, line 455456)
This is a very good question also raised by the other reviewer. The intensity of seepage has not been modelled in this study, which is focused on the two effects of Psi_rain and Psi_air’. However, the atmospheric effects will never exceed the atmospheric pressure change, which is unlikely to change more than 5 kPa. The seepage is function of the flow of groundwater, and might surpass these values.Lines 399: When you say that the response of psi_air is instantaneous, I think that then the pore pressure response to a gate function should just look like the gate function. But it seems like what you’re implying is that there is no delay in the beginning of the response, even though there still is a decay of the response in time?
Yes, the response to atmospheric effects is instantaneous because of the load transfer through the skeleton, but fades slowly by diffusion. The response to the gate function at a low diffusivity (D=10e6 m²/s) is almost identical to the gate function, because little diffusion occurred during the forcing.
Lines 406408: How does this finding compare with literature? Do we see landslides occurring in these locations?
This statement was referring to the model’s outcome, not to actual data. No studies were found reporting landslides locations under these conditions.
Line 431: “dominants” > dominant
Done
Line 443, 449: “repartition” Partitioning? Check word choice.
The word has been changed to “distribution”.
Line 450: “typhon induced” > “typhooninduced”
Done
Line 478: weeks or months after the rain event – has this been observed? I think a reference would
strengthen this argument.
This has been reported in the context of longterm forcing in slowmoving landslides (Iverson and Major, 1987), but not observed for typhoons.
Line 489: “amount of cumulated rainfall” > “depth of rainfall” or “accumulation of rainfall”
Done
Line 495: large variations in pore water pressure?
Yes, this was referring to the possibility of the water table in the case of Morakot to accommodate for large variations in water table level, and therefore in pore pressure. The sentence has been corrected (line 547).

AC1: 'Reply on RC1', Lucas Pelascini, 15 Mar 2022

RC2: 'Comment on nhess2021340', Anonymous Referee #2, 01 Feb 2022
Re: Review of Modelling the control of groundwater on landslides triggering: the respective role of atmosphere and rainfall during typhoons by Pelascini et al., submitted to Natural Hazards and Earth System Sciences as NHESS2021340
The subject manuscript describes a modeling study focused on identifying relative (and absolute) contributions of rainfall and atmospheric pressure change during typhoons in causing landslides. Consideration of atmospheric pressure effects on slope stability is quite novel; I’m aware of only one other study related to this subject (cited in paper). During typhoons, atmospheric pressure can drop several kPa, causing reduced slope stability by reducing effective normal stress, whereas rainfall amounts may contribute several tens (or more) of kPa to reduce this normal stress. However, by using simple 2D and 1D hydrogeologic modeling, the authors show that these effects on effective normal stress vary through time and slope position, such that differing initial water table conditions and hydraulic diffusivity of hillslope materials may result in relatively greater or lesser effects on slope instability from rainfall and atmospheric pressure change. The manuscript therefore presents important new insights into landslide triggering factors. Unfortunately, the model is poorly tested by empirical evidence, primarily because of the lack of data available to identify landslide timing and potential triggering during typhoons when rainfall and atmospheric pressure drop both are significant.
The conceptual and mathematical models developed in the manuscript involves deep groundwater within a homogeneous hill (peak to valley), discounting oftentimes perched groundwater within regolith, where many landslides generate during/following intense rainfall. How representative of the test locations in Taiwan is this conceptual model? What implications/omissions exist with respect to the lack of consideration of regolith?
The 2D and 1D models differently treat application of transient atmospheric pressure and rainfall, with diffusion occurring from different locations (ground surface or water table) depending on the forcing. Section 5.2 summarizes some of these differences and indicates that model uncertainty might explain some field observations. The dramatic differences between the models and, sometimes, their output makes me wonder what results may be believed, as well as wonder why the modeling approaches were not more consistent. A more critical evaluation of the implications of their differences is warranted with respect to both magnitudes and timing of effective normal stress change. For example, lines 349350 indicate that the lack of an infiltration model and application of rainfall immediately and entirely at the water table “might underestimate the response time.” Actually, except in special circumstances, these factors definitely underestimate the response time and by variable amounts ranging likely over several orders of magnitude for realistic conditions. What are the overall impacts of the simplifications involved with the modeling?
One or two lines mention that seepage forces may be important contributors to slope instability, and they certainly are, especially near discharge zones near slope toes (e.g., Iverson 2000, cited in paper). The importance of nonhydrostatic gradients in slope instability should be emphasized, especially with respect to landslide triggering from regions near slope toes. Additionally, please see next comment regarding landslides near slope toes.
2D modeling of the homogeneous hill suggests that groundwater is shallower near the slope toe and deeper near the slope crest, as is well known. This initial condition strongly affects atmospheric and rainfallinduced pore pressure change timing and magnitude along the height of the hillslope, as the manuscript demonstrates. The authors note that, for one typhoon, landslides in Taiwan concentrated near the lower parts of the slope, and they propose that this at least partly resulted from the shallower groundwater depth there. However, much of the preceding text noted that slope toes are more likely than upper parts of slopes to be saturated from longterm conditions, and if saturated, rainfall has no effect on stability and atmospheric pressure change will be of primary importance. Why would atmospheric pressure change in saturated regions not have been responsible for the landslide distribution? Additionally, such hillslope groundwater distribution should be ubiquitous, so does not the paper imply that rainfall/atmosphericpressureinduced landslides everywhere should concentrate on lower parts of slopes? Can the authors provide evidence for this? Finally, 3 typhoons in Taiwan are mentioned. It would be beneficial if the authors described how prestorm rainfall for the 3 events may have resulted in different landslide distributions, in accordance with their model.
Please see the accompanying markup for additional comments and suggestions to improve the manuscript.

AC2: 'Reply on RC2', Lucas Pelascini, 15 Mar 2022
Review of “Modelling the control of groundwater on landslides triggering: the respective role of atmosphere and rainfall during typhoons”
The subject manuscript describes a modeling study focused on identifying relative (and absolute) contributions of rainfall and atmospheric pressure change during typhoons in causing landslides. Consideration of atmospheric pressure effects on slope stability is quite novel; I’m aware of only one other study related to this subject (cited in paper). During typhoons, atmospheric pressure can drop several kPa, causing reduced slope stability by reducing effective normal stress, whereas rainfall amounts may contribute several tens (or more) of kPa to reduce this normal stress. However, by using simple 2D and 1D hydrogeologic modeling, the authors show that these effects on effective normal stress vary through time and slope position, such that differing initial water table conditions and hydraulic diffusivity of hillslope materials may result in relatively greater or lesser effects on slope instability from rainfall and atmospheric pressure change. The manuscript therefore presents important new insights into landslide triggering factors. Unfortunately, the model is poorly tested by empirical evidence, primarily because of the lack of data available to identify landslide timing and potential triggering during typhoons when rainfall and atmospheric pressure drop both are significant.
 We thank the reviewer for his comments. This specific comment summarizes well the novelty and limits of our manuscript. The model we use has indeed only be tested against data from a slowmoving landslide (Schulz et al., 2009) for small atmospheric pressure changes. Our manuscript uses this tested model in the case of larger atmospheric pressure changes (i.e., typhoons) and consider mostly the case of catastrophic landslides. For these landslides, there is to our knowledge (as also stated by the reviewer) no clear evidence of landslides triggered by atmospheric pressure changes, potentially due to the current inability of observations to resolve the timing of landslides during large storms.
The goal of the modelling approach was (1) define a simple model, as simple as the original Iverson model, which could better represent groundwater dynamics under hydrological and atmospheric boundary conditions (2) define the main physical controls. This allows to underline observation requirements which could better inform on actual processes in landslide generation.
 We now clearly state that the model has not been tested against natural catastrophic landslides (Lines 182184)
The conceptual and mathematical models developed in the manuscript involves deep groundwater within a homogeneous hill (peak to valley), discounting oftentimes perched groundwater within regolith, where many landslides generate during/following intense rainfall. How representative of the test locations in Taiwan is this conceptual model? What implications/omissions exist with respect to the lack of consideration of regolith?
 This is a very good point. Our model considers a homogeneous hillslope with no lithology change above a single unconfined aquifer. This hypothesis comes from the hydrological model, which considers an aquifer relatively thick in comparison to the 500 m length of the hillslope so that the groundwater flow can be described as horizontal.
This simplification indeed does not fully account for the hydrogeological complexity under Taiwan’s hillslopes but is necessary to develop a model rooted on basic analytical solutions.
However, the model can be applied at any scale and therefore represent smaller aquifer – including perched ones – at smaller scales, as long as the boundary conditions and the hypothesis of the hydrological model are respected. Considering smaller aquifers, for instance developed in the regolith, and depending on their connexion with the hillslope aquifer, this would lead to similar water table profile yet with shorter characteristic times, following this scaling , where L is the length of the considered perched aquifer.
Following this work, we are now setting up a modflowbased model on a Taiwanese catchment, driven by a landsurface model, to better represent actual groundwater flow in heterogeneous systems.
 We now acknowledge this simplification and limitation and discuss the scale effect in the discussion (lines 347350 & 525529) and illustrated it with a new figure (Fig. 8)
The 2D and 1D models differently treat application of transient atmospheric pressure and rainfall, with diffusion occurring from different locations (ground surface or water table) depending on the forcing. Section 5.2 summarizes some of these differences and indicates that model uncertainty might explain some field observations. The dramatic differences between the models and, sometimes, their output makes me wonder what results may be believed, as well as wonder why the modeling approaches were not more consistent. A more critical evaluation of the implications of their differences is warranted with respect to both magnitudes and timing of effective normal stress change. For example, lines 349350 indicate that the lack of an infiltration model and application of rainfall immediately and entirely at the water table “might underestimate the response time.” Actually, except in special circumstances, these factors definitely underestimate the response time and by variable amounts ranging likely over several orders of magnitude for realistic conditions. What are the overall impacts of the simplifications involved with the modeling?
 We acknowledge this comment. The 2D hillslope model mainly differs from the infinite slope model by having a dynamic and fluctuating water table, and especially to represent the impact of uphill groundwater flow contributing to local pressure change, in addition to local recharge. This is very important, and translates as critical when considering the specific behavior at the toe and crest of the hillslope. This leads to a key difference as the 2D model uses the water table variations to feed into the pore pressure diffusion. The underlying hypothesis here is that pore pressure variations induced by rainfall are caused by changes in the height of the water table. As a consequence, since the pore pressure is applied from the water table, the infiltration time needed for rainfall to reach the water table is disregarded. Indeed, this underestimates the response time for the areas where the water table is deep – namely the upper part of the hillslope – and does not allow to describe shallow landslides.
 We now clearly discuss this limitation of the 2D model in the discussion comparing 1D and 2D models (lines 370375)
One or two lines mention that seepage forces may be important contributors to slope instability, and they certainly are, especially near discharge zones near slope toes (e.g., Iverson 2000, cited in paper). The importance of nonhydrostatic gradients in slope instability should be emphasized, especially with respect to landslide triggering from regions near slope toes. Additionally, please see next comment regarding landslides near slope toes.
 Indeed, the seepage effect leads to slope instabilities and is discussed in many papers. Loss of stability by seepage is mainly related to vertical flow, creating a force against the weight of the slope; yet the hydrological model only considers horizontal flows. Approximation of seepage forces based on such a model would greatly underestimate the effects on slope stability. A proper estimation would require the simulation of flowpaths, by a more complex hydrological model, better representing the impact of heterogeneity, and is beyond the scope of this study. The manuscript here focuses only on rainfall infiltration creating pressure front and atmospheric effects on the pore pressure – which are nonhydrostatic processes. This hypothesis is stated during the model description and the seepage is mentioned in the model limitations.
 A brief description of the seepage destabilising effect and why it is not computed in our model is provided in the section describing the water table model (lines 138141).
2D modeling of the homogeneous hill suggests that groundwater is shallower near the slope toe and deeper near the slope crest, as is well known. This initial condition strongly affects atmospheric and rainfallinduced pore pressure change timing and magnitude along the height of the hillslope, as the manuscript demonstrates. The authors note that, for one typhoon, landslides in Taiwan concentrated near the lower parts of the slope, and they propose that this at least partly resulted from the shallower groundwater depth there. However, much of the preceding text noted that slope toes are more likely than upper parts of slopes to be saturated from longterm conditions, and if saturated, rainfall has no effect on stability and atmospheric pressure change will be of primary importance. Why would atmospheric pressure change in saturated regions not have been responsible for the landslide distribution? Additionally, such hillslope groundwater distribution should be ubiquitous, so does not the paper imply that rainfall/atmosphericpressureinduced landslides everywhere should concentrate on lower parts of slopes? Can the authors provide evidence for this? Finally, 3 typhoons in Taiwan are mentioned. It would be beneficial if the authors described how prestorm rainfall for the 3 events may have resulted in different landslide distributions, in accordance with their model.
 The idea behind these observations is indeed that the landslides distribution could be induced by atmospheric pressure changes; since infiltration – and therefore rainfallinduced pore pressure – is prevented in fully saturated areas. However, as already stated the model focuses on the dynamic pore pressure effects, leaving aside seepage or more complex effect, and disregarding the hydrostatic loading, which also may decrease stability in these areas.
 We now more clearly state that the landslides distribution towards the toe of the hillslopes indicates an atmosphericdriven failure (lines 489491).
Taiwan has been chosen for the large number of typhoons, provoking many large atmospheric disturbances. The repartition of landslides towards the toe of the slope is indeed not limited to this area, but a general trend for landslides triggered by weather events. In case of earthquaketriggered landslides, slope failures tend to focus on the crest rather than the toe of the slope. These observations can be found in (Meunier et al., 2008) already cited in the manuscript.
Among the 3 typhoons showed, only Morakot led to massive amounts of landslides. Masta and Krosa generated mudslides and debris flow, but in less quantity. No study has been conducted on the landslides and slope failure distribution along the hillslope after all these events.
However, the model suggests such events over partially saturated slopes would have led to landslides near the toe of hillslopes during the typhoons, due to the atmospheric effect, then deeper landslides towards the upper unsaturated part of the hillslope after the typhoon due to the diffusion of rainfallinduced pore pressure. This has to be taken with caution, as the model does not represent all destabilizing processes – such as seepage – and should be verified with observed data.
Please see the accompanying markup for additional comments and suggestions to improve the manuscript.
The suggestions and comments have been taken into consideration in the manuscript.

AC2: 'Reply on RC2', Lucas Pelascini, 15 Mar 2022