2.1. Snow avalanche numerical modeling

Snow avalanches are complex flows (e.g. Reference AnceyAncey, 2006; Reference Pudasaini and HutterPudasaini and Hutter, 2007). Their typical vertical stratification has been demonstrated through field measurements (Reference Sovilla, Sommavilla and TomaselliSovilla and others, 2001; Reference Ancey and MeunierAncey and Meunier, 2004) on full-scale experimental sites. To be consistent with observations, avalanche flows can be modeled within the formal framework of continuum mechanics (Reference Savage and HutterSavage and Hutter, 1989) by different layers with different physical properties (Reference IsslerIssler, 1998; Reference NaaimNaaim, 1998; Reference ZwingerZwinger, 2000). Such models are often used to back-calculate well-documented events. However, due to the time needed for one avalanche simulation, these models cannot be used within a probabilistic framework requiring at least a few hundred simulations.

Considering only the dense layer of the avalanche simplifies the problem, since the depth of the flow is then small compared to its length, allowing a shallow-water approximation of the mass and momentum conservation equations to be used. Although some physical processes (e.g. the formation of the powder part of the flow and vertical velocities in the dense flow) are thus ignored, a realistic representation of the avalanche can be obtained. Computation times are much more reasonable, allowing Monte Carlo simulations to be implemented (Reference Barbolini, Cappabianca and SaviBarbolini and others, 2003).

In this paper, we therefore represent avalanche propagation with a fluid model based on depth-averaged Saint-Venant equations. We assume that the study site can be described by a curvilinear profile whose equation in a Cartesian frame is z = f ₁ (x), where z is the altitude and x the distance measured in Cartesian coordinates starting at the top of the path. The propagation model, noted G in Figure 1, is described by Reference Naaim, Naaim-Bouvet, Faug and BouchetNaaim and others (2004). However, to facilitate the specification of the input conditions corresponding to each simulation and reduce computation times, we ignore snow incorporation and deposition here, so that mass is conserved. Variation in momentum corresponds to the difference between gravity g and a friction term, Fric, which is sometimes called the retarding acceleration (Reference Gauer, Lied and KristensenGauer and others, 2009). The equations of mass and momentum conservation, in which v is the flow velocity, h is the flow depth, ϕ is the local slope and t is time, are

They are solved numerically using a finite volume scheme (Reference NaaimNaaim, 1998). Even if they are expressed in a two-dimensional (2-D) frame, they in fact represent a one-dimensional (1-D) flow on the curvilinear profile (Reference Greve, Koch and HutterGreve and others, 1994; Reference Gray, Wieland and HutterGray and others, 1999; Reference Pudasaini and HutterPudasaini and Hutter, 2003).

Fig. 1.

Direct acyclic graph of the stochastic avalanche model.

k _sv is the ratio between the stress normal to the slope and the stress parallel to the slope. It can be calculated from the Mohr–Coulomb plasticity model for quasi-static deformations (Reference Savage and HutterSavage and Hutter, 1989). For dense granular flows on rough surfaces, Reference Silbert, Ertas, Grest, Halsey, Levine and PlimptonSilbert and others (2001) showed that the normal stress is equal to the stress along the slope. Even if it is not true in general, particularly during deposition (Reference Pudasaini, Hutter, Hsiau, Tai, Wang and KatzenbachPudasaini and others, 2007; Reference Pudasaini and KrönerPudasaini and Kröner, 2008), Reference Pouliquen and ForterrePouliquen and Forterre (2002) showed, using k _sv = 1, that, for depth-averaged equations, k _sv has no significant effect on the dynamics of the flow. α _sv is the shape of the vertical velocity profile. Observations of real snow flows showed a quasi-constant velocity over the whole core of the avalanche, and highly sheared vertical velocity profiles close to the bottom (Reference Bouchet, Naaim, Bellot and OussetBouchet and others, 2004). This implies α _sv is very close to 1. We therefore set both α _sv and k _sv to 1 for the entire study.

A major problem is to specify a realistic friction term, Fric. The scarcity of measurements in real avalanche flows leaves the question open, but it seems reasonable to postulate that snow avalanches do not accelerate indefinitely on a quasi-constant slope. Since, with no erosion, the flow can reach an equilibrium speed only if friction increases with velocity, a constant friction term cannot be used in our model. Experimental approaches have supported this choice, showing using small-scale flows (Reference Rognon, Chevoir, Bellot, Ousset, Naaim and CoussotRognon and others, 2008) and shear cells (Reference Casassa, Narita and MaenoCasassa and others, 1989, Reference Casassa, Narita and Maeno1991) the quasi-parabolic increase of friction with velocity. Although it continues to be debated in the avalanche community, the widely used Voellmy model (Reference VoellmyVoellmy, 1955) is therefore a good candidate. It associates a Coulombian term with a velocity square-dependent term, with two friction coefficients μ and ξ to be specified, so that

With this model, the limit velocity can be attained for constant slopes tan(ϕ) > μ. Traditionally (Reference Salm, Burkard and GublerSalm and others, 1990), it is assumed that the coefficient μ summarizes snow properties as a function of altitude, exposure, etc., whereas ξ is assimilated to a morphological parameter representing the roughness of the path. However, this interpretation of the Voellmy equation continues to be discussed since it is based on expert considerations rather than on measurements. Its main advantage while fitting the model on a set of observed avalanches is that it reduces the number of unknown quantities. We therefore adopt this point of view: μ is modeled as a latent variable describing the random effects from one avalanche to another, and ξ as a parameter in the strict statistical sense of the term. ξ and μ_i , i ∊ [1, N], where N is the total number of observed avalanches, are estimated from the data.

2.2. Pressure computations

The dynamic pressure in the free surface flow is defined as ρ_Nv ², i.e. double the kinetic energy per unit volume. Impact pressure Pr can be expressed as

where ρ_N is the density of the flowing snow and Cx the drag coefficient. We compare the statistical distribution of the dynamic pressure in the free surface flow with the distributions of impact pressures obtained with both the experimental formulation of Reference Sovilla, Schaer, Kern and BarteltSovilla and others (2008) and the semi-empirical formulation of Reference Naaim, Faug, Thibert, Eckert, Chambon and NaaimNaaim and others (2008). For all computations, a constant density of 300 kg m⁻³ is assumed. The related uncertainty is not taken into account.

In the empirical formulation proposed by Reference Sovilla, Schaer, Kern and BarteltSovilla and others (2008), the drag coefficient is expressed as

where the Froude number Fr is the ratio between inertial forces and gravity. The parameter pair (v ₁, v ₂) depends on the obstacle and the event considered (e.g. on the snow properties) and is fitted on various avalanche events from the Vallée de la Sionne test site in Switzerland. We use the values v ₁ = 5770 and v ₂ = 1.9, which correspond to the best-documented event.

Reference Naaim, Faug, Thibert, Eckert, Chambon and NaaimNaaim and others (2008) used the framework of gradually variable shallow flows to define a macroscopic viscosity and a Reynolds number based on the mean velocity and on the obstacle-specific diameter. Assuming the Reynolds similarity, the drag coefficient formula obtained for simple fluids was extended to free surface flows of complex fluids. It is considered that the drag coefficient accounts for two different contributions. The first is determined by the shape of the obstacle. The second is related to the flow regime and is considered to be independent of the shape contribution.

The generalized Reynolds number Re represents the ratio between inertial and viscous forces. Assuming a quasi-permanent and uniform flow impacting an obstacle with a specific diameter d ₀ on a slope characterized by a slope angle ϕ, it can be written as

The formula is valid for a prismatic shape. For a cylindrical shape, the drag force is divided by 2. To investigate the influence of the size of the obstacle considered, we study two diameters: d ₀ = 0.25 m (e.g. a pylon) and d ₀ = 5 m (e.g. a small house or a defense structure such as a deflecting mound).

According to Reference Naaim, Faug, Thibert, Eckert, Chambon and NaaimNaaim and others (2008), the variation of the drag coefficient can be expressed as

This semi-empirical formula was obtained by compiling existing data on the drag coefficient of Newtonian and non-Newtonian fluids. Low and moderate Reynolds numbers ranging from 0.1 to 200 were investigated, corresponding to the typical variation range of the equivalent Reynolds number in snow avalanche flows. For Re > 200, log ₁₀(Re) + 3 tends to zero and Equation (6) is no longer valid. This is not a real problem for pressure computations in dense snow avalanches since the drag coefficient then becomes constant. For a prismatic shape, Cx tends to 2 (Fig. 11a, shown further below).

Finally, with the formalism and friction model used, no steady and quasi-uniform flow is possible for slope angles lower than arctan(μ), because the avalanche is then in its decelerating phase. To compute the Reynolds number using Equation (5), the slope angle is therefore taken as the local slope angle ϕ(x) for avalanches that do not decelerate at abscissa x, and as arctan(μ), the last slope angle for which a steady flow was possible, for avalanches that decelerate at abscissa x. This can be rewritten as

2.3. French avalanche database, data transformation and stopping condition

The Enquête Permanente sur les Avalanches (EPA; permanent avalanche survey) is a database describing the avalanche events of ∼4000 determined paths in the French Alps and the Pyrenees since the beginning of the 20th century (Reference MouginMougin, 1922; Reference Bélanger, Cassayre and ElderBélanger and Cassayre, 2004). Avalanche counts are registered by local foresters as exhaustively as possible. A great deal of other quantitative and qualitative information is also collected. This unique database is particularly well designed for statistical–dynamical approaches and for more phenomenological large-scale studies relying on the entire database (Reference Eckert, Parent, Bélanger and GarciaEckert and others, 2007a).

When using these data to calibrate a numerical avalanche model, the main difficulty is that not all the input variables needed are registered in the database. For example, for our propagation model, the length of the release zone, L _start, which we measure along the x axis, as well as the mean snow depth in the release zone, h _start, are necessary but not available. Following Reference Meunier, Ancey and RichardMeunier and others (2004), we evaluate the dimensions of the starting zone associated with the registered events using a deterministic transformation of the recorded deposit volume v _stop. However, the procedure chosen is highly speculative. A more realistic description of the release conditions, including the most recent developments concerning the size distribution of snow avalanches (Reference McClungMcClung, 2009) could easily be included in our framework.

The three dimensions of the starting zone are assumed to have the same influence on the deposit volume, which implies dependencies to the power of 1/3 between v _stop and (h _start, L _start, l _start), respectively, the latter being the width of the release zone. Moreover, expert considerations are used to set the snow depth and the length of the starting zone associated with a very small and a very large avalanche. Under the assumption of a constant snow volume, this allows the relationship between the deposit volume and the mean snow depth in the release zone to be expressed as

and the relationship between the deposit volume and the length of the release zone as

A linear relationship between the snow depth and the length of the release zone then exists:

In addition, the width of the release zone can be evaluated using

where ϕ _start is the mean slope of the release zone between the abscissas x _start and x _start + L _start. Weighting by cos ϕ _start is necessary because of the projection of L _start on the release slope ϕ _start.

Our propagation model does not take into account the width of the release zone. When only L _start and h _start are used as input variables, roughly one-third of the variability of the deposit volumes is lost. An equivalent release volume depending on the mean release width can be computed as

Its variability from one avalanche to another represents the variability introduced in the propagation model more realistically than the variability of the observed deposit volumes.

Finally, when numerical avalanche propagation stops, the granular media are reorganized along the slope (e.g. Reference Pudasaini, Hutter, Hsiau, Tai, Wang and KatzenbachPudasaini and others, 2007). A stopping condition therefore has to be specified to distinguish these quasi-static motions from the avalanche flow. Here we assume any avalanche to be stopped as soon as the maximal propagated discharge is smaller than

This varying threshold is convenient for simulating avalanches of very different volumes. Very small avalanches are not immediately stopped, which occurs if the constant threshold chosen is too high; while, for very large avalanches, quasi-static reorganization is excluded, which is not the case if a low constant threshold is chosen.

2.4. Multivariate stochastic modeling

Stochastic modeling allows the variability of avalanche events on a given path to be described. Here we expose our assumptions concerning the distributions of the different input–output variables of the propagation model. The main characteristics of the obtained stochastic avalanche model are summarized in Figure 1 using a directed acyclic graph (Reference LauritzenLauritzen, 1996). The relevance of the different probabilistic choices is discussed in section 5.4.

A distinction is made between avalanche frequency a and avalanche magnitude y. Avalanche frequency is a scalar discrete random variable corresponding to the number of avalanches recorded each winter and whose long-range mean is necessary for computing return periods. Avalanche magnitude is a random vector including all the correlated multivariate quantitative characteristics that vary from one event to another: runout distance, velocity and pressure profiles, snow volume, etc. The stochastic model is noted p(y, a|θ_M , θ_F ), indicating that the joint distribution p of the random variables y and a is indexed by the parameters (θ_M , θ_F ). Finally, the hypothesis of magnitude– frequency independence is made, considering that the number of avalanches per winter does not affect their quantitative characteristics. This classic hypothesis in avalanche modeling is fulfilled if the number of avalanches affecting the studied path each winter is not too high. It can be expressed as

Avalanche frequency is assumed to be an independent Poisson-distributed process (Reference Eckert, Parent, Bélanger and GarciaEckert and others, 2007a), with its single parameter λ quantifying the mean annual avalanche number:

The magnitude model embeds the sliding block propagation model within several stochastic operators describing the variability of the different input–output quantities. Reference McClungMcClung (2003) adopts a similar approach that describes avalanche events as a Poisson process with log-normal marks for avalanche masses.

The release abscissa x _start that corresponds to the beginning of the release zone is assumed to be purely random and beta-distributed (Reference Meunier, Ancey and NaaimMeunier and others, 2001). A normalization is necessary, and the length of the release zone is used, so that

where x _max and x _min are the maximal and minimal abscissas of the release zone. x _max and x _min are assumed to be known. They can be estimated using simple topographical thresholds or the available data.

Given the normalized release abscissa, the mean release depth h _start is assumed to be gamma-distributed, with a parameterization reflecting the dependency of the snow depth on the release abscissa and a constant dispersion around the mean. For simplicity, the conditioning by x _max and x _min is dropped, which leads to

This model is chosen to represent the skewness of a hydrological variable such as snow depth (values much higher than the mean are plausible) as well as the possible variation of snow depth with altitude. Since a linear relation between the release depth and the length of the release zone exists (Equation (10)), there is no need to specify probability distributions for other input quantities.

Given the normalized release abscissa and the flow depth, the latent friction coefficient μ is assumed to be normally distributed, with four parameters characterizing its dependency on the release abscissa and mean release depth and with a constant dispersion around the mean. This can be written as

Small Gaussian differences between the observed runout distances and the latent computed runout distances x _stop are postulated, such as

These differences can result from numerical errors due to the imperfection of the propagation model, and/or from observation errors. The standard deviation σ _num is to be specified.

To sum up, the proposed frequency model has only one parameter, θ_F = λ. Conversely, the magnitude model is relatively complex, with ten parameters θ_M = (a ₁, a ₂, b ₁, b ₂, σ_h , c, d, e, σ, ξ) and, for each avalanche, the latent friction coefficient μ and the computed runout distance x _stop. The different input variables and μ are explicitly modeled as dependent variables to take into account possible correlations that may affect extreme events. The joint probability of the magnitude observations given parameters and latent variables is obtained by combining the different conditional distributions:

μ appears in the right-hand side term only indirectly, by constraining the deterministic propagation and x _stop.

Finally, we note , i ∊ [1, N] and a_t , t ∊ [1, T _obs], our datasets corresponding to the N avalanches registered on the studied site during T _obs years of observation. They are assumed to be mutually independent, which implies

For the magnitude model, this hypothesis is fulfilled if all avalanches that occur in a given winter are neither too numerous nor temporally too close, so that the quantitative characteristics of the first avalanche do not affect those of the next avalanches. For the frequency model, the physical independence of the number of avalanches occurring in two consecutive winters is clear.

2.5. Bayesian inference

Inference of the proposed stochastic model is performed under the Bayesian paradigm. Bayes’ theorem (Reference BayesBayes, 1763) allows the observations to be combined with a prior distribution π(θ_M , λ) which encodes prior knowledge about the unknowns. The result of the computation is the joint posterior distribution of all parameters and latent variables p(θ_M , λ, μ, x _stop|data), where data denotes all observations .

Under the magnitude–frequency independence hypothesis, the frequency and the magnitude models can be inferred separately. For the frequency model, inference is analytically feasible as soon as a gamma prior,

is chosen for the parameter λ. The parameter pair (a_λ., b_λ ) represents the prior knowledge concerning avalanche occurrences. The posterior distribution is then still gamma-distributed, with the parameter pair verifying and .

For the magnitude model, inference is more cumbersome. Indeed, the probability of the latent variables given parameters and observations must be considered in Bayes’ theorem in addition to the prior and the probability of observations given parameters and latent variables, i.e.

The latent variable distribution is obtained by combining the distribution of the friction coefficient μ and the result of the deterministic propagation noted as the Dirac distribution δ():

In other words, x _stop must be equal to G(x _start, h _start, μ, ξ), otherwise a zero probability is assigned. This emphasizes that, even if our model has two latent variables, μ and, x _stop, they are deterministically linked.

2.6. Markov chain Monte Carlo methods and the Metropolis–Hastings algorithm

The normalizing constant in Equation (23) cannot be computed analytically, so recourse to a simulation-based estimation algorithm is necessary. A general exposition of the Markov chain Monte Carlo (MCMC) methods that can be used to obtain samples from p(θ_M , μ, x _stop |data, σ _num) can be found in various sources (Reference Gilks, Richardson and SpiegelhalterGilks and others, 1996; Reference RobertRobert, 1996; Reference BrooksBrooks, 1998; Reference CongdonCongdon, 2001; Reference Parent and BernierParent and Bernier, 2007). Their principle is that, under few assumptions, there is a single stationary distribution for a Markov chain. Iterative MCMC algorithms have therefore been developed to construct chains in the space of model unknowns that converge to the target posterior distribution. Such procedures include the extremely general MH algorithm (Reference Metropolis, Rosenbluth, Rosenbluth, Teller and TellerMetropolis and others, 1953; Reference HastingsHastings, 1970), and the efficient but less general Gibbs sampler (Reference Geman and GemanGeman and Geman, 1984).

An initial state of the chain must be specified for all model unknowns, in our case (θ_M , μ, x _stop) ^(o) _. Then a burn-in period is needed to ensure that the chain has reached its so-called ergodic state. Finally, running enough iterations of the chain after the burn-in period reconstructs the target distribution. For example, each iteration k of the MH algorithm consists in the generation using an exploration function f ₂ of a candidate value for the unknowns (θ_M , μ, x _stop)^(C) = f ₂ (θ_M , μ, x _stop)^(k−1) and in a probabilistic acceptance–rejection rule deciding whether (θ_M , μ, x _stop)^(k) = (θ_M , μ, x _stop)^(C) or whether (θ_M , μ, x _stop)^(k) = (θ_M , μ, x _stop)^(k−1). The random feature in the acceptance–rejection rule is the key point: if the candidate is a posteriori more likely than the previous state of the chain, it is always accepted. In the opposite case, it is sometimes accepted, allowing the algorithm to leave the regions of high posterior probability where it mostly gravitates, and jump to regions of lower posterior probability. This way, the algorithm randomly browses the whole domain, looking for potential local second-order modes of the posterior distribution.

Convergence should occur for any symmetric exploration function that keeps the Markov chain homogeneous. However, the use of the MH algorithm is very subtle in practice because no general theoretical result concerning the rate of convergence is available. Moreover, for high-dimension parameter spaces, the posterior surface is likely to exhibit numerous modes and curvature ridges that may trap the algorithm and make it difficult to visit all regions according to their posterior probabilities. The choice of an appropriate exploration function is therefore the critical point in writing an algorithm that converges reasonably fast. A class of exploration functions is generally chosen and the strength of its jump is tuned to obtain the fastest convergence. Reference Gelman, Carlin, Stern and RubinGelman and others (1995) showed that the main criterion to define a suitable value for the jump strength is the observed acceptance rate computed after a given number of iterations. A high acceptance rate means that candidates result from too small jumps around a main distribution mode, leading to numerous tiny moves. It then takes a long time to explore the whole posterior space. By contrast, a low observed acceptance rate implies that the jump values used are too high and that the chain is stuck. The observed acceptance rate must therefore stay around 0.23 for a number of unknowns greater than 5 and be ∼0.44 for a single parameter.

In addition to visual inspection, the convergence must be quantitatively checked (Reference Brooks and GelmanBrooks and Gelman, 1998; Reference Brooks and RobertsBrooks and Roberts, 1998), generally by launching many chains from different starting points of the parameter space. This allows verification that the different subsamples belong statistically to the same population by various parametric and nonparametric tests (Reference Mengersen, Robert, Guihenneuc-Jouyaux, Bernardo, Berger, Dawid and SmithMengersen and others, 1999). For example, the Gelman–Rubin convergence diagnosis compares the variability of the generated parameters within and across the different sequences (Reference Gelman, Gilks, Richardson and SpiegelhalterGelman, 1996). Further useful hints concerning exploration functions and convergence diagnosis for the MH algorithm are provided by F. Torre and others (http://www.cybergeo.presse.fr/).

Here a multivariate normal random-walk jump function has been used. This means that the candidate has been drawn from a multivariate normal distribution centered on the previous value of the chain. For strictly positive variance parameters, a logarithmic transformation has been used. The variance–covariance matrix of the jump function had to be tuned. To simplify this task, a sequential version of the MH algorithm has been implemented. This means that a diagonal variance–covariance matrix has been set for candidate proposals, and that for each iteration the credibility of the candidates for the different parameters has been evaluated separately. The target acceptance rate was 0.35–0.45 for all parameters except ξ. Since all avalanches must be propagated with the same value of ξ, the credibility of the different runouts obtained had to be evaluated simultaneously with regard to the data. ξ and all the latent variables μ, x _stop were therefore calibrated within the same acceptance–rejection rule, with a target acceptance rate of 0.25.

2.7. Computing reference scenarios using Monte Carlo simulations

For each unknown, a point estimate can be derived from the joint posterior probability distribution function (pdf) in addition to a credibility interval, which is the Bayesian counterpart for a confidence interval, but using the posterior pdf instead of the likelihood function. The posterior mean is the Bayesian estimator of the parameters of our model under the classic hypothesis of a quadratic loss function. and are then the posterior mean of the proposed models given and , respectively. These distributions quantify the randomness of the process studied given the data. The joint distribution includes the marginal distribution of some variables of interest for hazard zoning (runout distance, velocity, flow depth), and can also be used to compute the marginal distributions of Froude numbers , Reynolds numbers , drag coefficients , and impact pressures by combining the needed variables.

can easily be obtained because an explicit formulation of the model is available. However, for , a statistical–dynamical Monte Carlo approach is necessary to obtain the distribution of the outputs of the numerical avalanche propagation model given the distribution of its inputs. The specified conditional distributions must be used. Integration over the distribution of the latent friction coefficient μ must also be performed, which gives access to a sample of the distribution of the latent friction coefficient . This can be expressed as

To compute return periods, the expected annual frequency E[a|θ_F ] must be taken into account. With a Poisson frequency model, it is simply the unknown parameter λ. The return period , associated with the runout distance x _stop, is therefore estimated combining and , the estimated cumulative distribution function (cdf) of runout distances:

Practically speaking, if is the ordered sample obtained using Monte Carlo simulations, the empirical estimator for is simply k/n, where n is the sample size. For hazard zoning purposes, the inverse problem must be solved: the annual exceedance probability is known (e.g. 0.01 for the centennial event) and the associated runout distance quantile must be found. It is provided by the estimated inverse cdf of runout distances using

In the simulation set-up, the runout distance quantile corresponding to the return period T is then the th value of the ordered sample.

Using a Monte Carlo approach makes numerical errors unavoidable. A confidence interval for the non-exceedance probability associated with a given runout distance is

The confidence interval depends on the sample size, on the probability considered and on the quantile of the standard normal distribution corresponding to the desired confidence level α_c , usually 95%. It must be emphasized that such a confidence interval only accounts for the error due to a numerical evaluation. It allows checking that the sample size is large enough, but does not quantify other error sources (e.g. observation error, model error or estimation error). Their evaluation requires additional computational efforts to carry out sensitivity analyses and/or predictive simulations (section 5.5 for discussion).

Finally, the joint distribution of the exceedances summarizes the characteristics of all avalanche events at the abscissa . It can therefore be considered as the joint distribution of all the reference scenarios corresponding to the return period T. It can be obtained simply by considering only those events for which the runout distance exceeds . This partially counters the limitations of the return period for a multivariate hazard such as snow avalanches by giving the variation range to be considered at any abscissa.

3.1. Case study presentation

The chosen case study is one of numerous paths of the French avalanche database. It is situated in the village of Bessans, Savoie department. It is only slightly channelized, and ends in the large flat valley of the Arc river. It is approximately 2300 m long from the top of the path to the Arc river, with a vertical drop of 1500 m (Fig. 2). The average slope is high, with several moderate changes of concavity along the slope profile. The slope remains predominantly above 30° during the first 1900 m of the path. The potential release zone is therefore long, so we chose x _max = 1900 m and x _min = 0_. Forty-one avalanches were recorded during T _obs = 44 years, with an empirical avalanche rate of 0.93 avalanches per year. However, only 26 of them were well enough documented to be used to calibrate the magnitude model. Therefore, N = 26, even if 41 events had to be used to compute the posterior distribution of the frequency model.

Fig. 2.

Topography and available historical data for the case study. Bessans township, path EPA No. 13, Savoie, France.

The quantitative characteristics of the observed events are summarized in Table 1. Snow depths obtained from the deposit volumes range from 75 cm to 4 m, which seems plausible given the relatively large size of the studied avalanche site. Release zone lengths are ∼100–400 m. Release zone widths have a high residual variability, which is not taken into account for model calibration. Thus, the variability of the equivalent release volumes is significantly lower than the variability of the ‘true’ release volumes.

Table 1.

Dataset descriptive statistics

The runout zone shows an irregular topography that constrains the empirical distribution of avalanche runout distances to be strongly multimodal. Figure 2 shows that most of the observed avalanches stopped on the gentle slopes at the end of the path between x = 1900 m and x = 2090 m. A few avalanches stopped earlier, between x = 1600 m and x = 1850 m, on average slopes that are situated above the last slope increase. An extreme event that stopped in the flat Arc valley was also registered, with a very large runout abscissa of 2208 m. This large variability of runout distances renders this case study a good test for the efficiency of our MH algorithm in calibrating the chosen avalanche propagation model.

Empirical correlations between data are shown in Table 2. Although some of them are small, they are all significantly nonzero at the 95% significance level. The numerous correlation coefficients very close to 1 are due to the deterministic relationships used to estimate the nonobserved quantities. Correlations between the three dimensions (L _start, l _start, h _start) of the starting zone and the release abscissa x _start are slightly negative. For this path, the size of the avalanche decreases with the altitude of the beginning of the release zone. Correlations between (L _start, l _start, h _start) and the runout abscissa are also negative. The longest runouts therefore mainly correspond to avalanches released at relatively low altitudes. For example, the extreme event registered was released at 2000 m a.s.l., corresponding to x _start = 1518 m (Fig. 2).

Table 2.

Dataset linear correlations

3.2. Prior distribution

The parameters were assumed a priori mutually independent, so that the joint prior distribution is simply

i.e. the product of the marginal distributions of the scalar parameters. This usual choice that facilitates prior elicitation is not very constraining since interparameter dependence is taken into account a posteriori. Moreover, the marginal prior distributions were assumed to belong to standard parametric families with their hyper-parameters to be specified.

Relatively informative marginal priors were used for the parameters c and σ (mean and variance of the latent friction coefficient μ), the release depth (parameter b ₁) and the friction coefficient ξ whose inverse controls the increase of friction with velocity and thus the limit velocity that can be reached by the flow. The choice of an informative prior for ξ has been made to ensure the model can be identified. For the other parameters, it was a modeling choice aimed at bringing more information into the analysis (see section 5.1 for discussion and sensitivity analysis).

The correlation parameters (b ₂, d, e) were assumed to be unknown a priori: the means of their marginal prior distributions were set to zero to let the data decide whether significant correlations between the different input variables of the propagation model exist. Vague priors (Reference Bernardo and SmithBernardo and Smith, 1994) were also used for (a ₁, a ₂, λ), because prior knowledge was not available. The different marginal priors used are summarized in Table 3.

Table 3.

Marginal prior distribution. U refers to the uniform distribution, N to the normal distribution and Gamma to the gamma distribution

3.3. Running the MH algorithm and assessing convergence

The numerical error σ _num for the discrepancy between observed and computed runout distances was set to 15 m. The 1-D random-walk jump functions shown in Table 4 were chosen for MH inference. They were tuned with respect to Reference Gelman, Carlin, Stern and RubinGelman and others’ (1995) optimal acceptance rates to adapt the algorithm to the case study. After a burn-in period of 1000 iterations, 2000 iterations were performed and stored as a sample of the posterior distribution. Convergence was checked by launching different chains from different starting points of the parameter space and computing the Gelman–Rubin convergence diagnosis (see below). The total computations for one chain took ∼2 weeks on a recent standard PC. This very long time is related to the relative complexity of the propagation model used and to the fact that, at each iteration of the MH algorithm, N = 26 iterations of the propagation model had to be performed.

Table 4.

Jump functions for the MH algorithm. logN refers to the log-normal distribution. Notations indicate, for example, that at each iteration k of the MH algorithm, the candidate value for the a ₁ parameter is drawn from a normal distribution centered on the value at the previous iteration

Table 5 shows the acceptance rates obtained for one chain. They are very close to the target optimal values discussed in section 2.6, i.e. 0.34–0.49 for the scalar parameters and 0.26 for the multidimensional jump corresponding to the friction coefficients. Figure 3 shows how well the two chains (for two parameters) mix during the ergodic phase. For the parameter a ₁ characterizing the distribution of release abscissas, the trajectories of the two chains show a stabilized variation domain as well as strong variability from one iteration to the other, and they mix well. This indicates that convergence is easily reached. For ξ, the chains are more autocorrelated, with lower variability from one iteration to the other and thus a lower level of mixing. This indicates that, for the friction coefficients, reaching convergence and obtaining a good approximation of the posterior pdf is more cumbersome and requires more iterations of the MH algorithm. A more quantitative check of the convergence is given in Table 6, which presents the Gelman–Rubin statistics for the different unknowns. It is not equal to 1 for all parameters. However, the highest value is 1.03, which indicates that the variability of the generated samples across the different sequences is <1.05 times the variability within the different sequences, even for the friction coefficients μ and ξ. This is in practice more than sufficient for considering that convergence has been reached and that a satisfactory numerical approximation of the joint posterior pdf is therefore available.

Table 5.

Acceptance rates for the MH algorithm

Fig. 3.

Two chains of the MH algorithm for two parameters, a ₁ and ξ. The algorithm is in its ergodic phase (burn-in period is not considered).

Table 6.

Reference Gelman, Carlin, Stern and RubinGelman and others’ (1995) convergence diagnosis

3.4. Posterior distribution

4.1. Simulation set-up

For the predictive phase, 20 000 Monte Carlo simulations were performed. First, 20 000 values of the joint distribution of the input variables were sampled. This notation remembers that, in the predictive phase, all model parameters including ξ are fixed to their posterior estimates. The distribution of the release length L _start was obtained by computing the release length corresponding to each simulation using Equation (10). Then each set of input variables was propagated, which provides, using Equation (25), the joint distribution of the output variables . The notations v_xt and h_xt indicate that, for each simulation, a velocity and a flow depth are computed for each abscissa and each time-step. Note that the random noise σ _num is not considered in this predictive phase, so the runout distance distribution obtained is discrete with a 5 m discretization step.

Subsequently, the samples obtained were reworked to compute return periods and extract the distributions of friction coefficients, maximal velocities , and maximal flow depths at abscissas corresponding to different return periods. The associated distributions of Froude numbers, Reynolds numbers, drag coefficients and impact pressures were computed using these maximal values. The Froude numbers, Reynolds numbers and impact pressures considered are not rigorously maximal values, since maximal values for these quantities are not necessarily concomitant with maximal velocities and maximal flow depths. Nevertheless, tests were done to compare the values obtained with this simplified simulation set-up and the ‘true’ maximal values for a few events, showing very few differences. Moreover, recent experimental data concerning velocity and flow depth profiles in real avalanche flows (Reference Sovilla, Schaer, Kern and BarteltSovilla and others, 2008) and avalanche simulations (Reference Naaim, Faug, Naaim and EckertNaaim and others, 2010) suggest that the Froude number is relatively constant in the avalanche body, so the distributions obtained with our simplified set-up may well be close to the distribution of the ‘real’ maxima of the different quantities at the abscissas considered. Total computations took approximately 5 days on a standard PC.

4.2. Distribution of input variables

Figure 7 shows the distribution of the ‘input’ variables of the propagation model given . Most avalanches are released in the upper part of the path, with release depths of 0.77–2.54 m at the 95% confidence level (Table 8). Corresponding release lengths range predominantly between 100 and 250 m. The distribution of the friction coefficient μ is slightly skewed to the left, but very close to a Gaussian distribution with a mean and a standard deviation . This comes from the low correlation between μ and the other input variables inferred on the data for this case study. The posterior correlation between μ and x _start and between μ and the release dimensions (h _start, L _start) is therefore very low (Table 9; see section 5.4.2 for discussion). Other a posteriori correlation coefficients are close to those obtained from the data. Given the large simulated sample, all these correlation coefficients, even the very small ones, are nonzero at the 95% significance level.

Fig. 7.

Distribution of the input variables of the propagation model: (a) release abscissa, (b) release depth, (c) release length and (d) friction coefficient μ. Parameters of the magnitude model equal their posterior mean . Release lengths are derived from release depths using Equation (10).

Table 8.

Distribution of model variables given

Table 9.

Intervariable correlations (posterior mean)

4.3. Runout distances and return periods

Figure 8a shows the simulated runout distance distribution. It is strongly multimodal, with its main mode around x = 2000 m, a secondary mode around x = 1700 m and a tertiary mode around x = 900 m. This is in good agreement with the path’s complex geometry: the main mode corresponds to the gentle slopes at the bottom of the path, just before the arrival at the valley floor, where most of the observed avalanches have stopped. The secondary mode corresponds to the segment of the path where the slope decreases to ∼23° before increasing again to 40°, where a few of the observed avalanches have stopped. The third small mode in the middle of the path corresponds to a change in the path’s concavity that stops minor avalanches characterized by a very high level of friction. Due to their small size, such avalanches are not recorded in the French avalanche database.

Fig. 8.

(a) Runout distance distribution and (b) return periods.

Table 10 confirms the fairly good agreement between the simulated sample and the data. For the median, the difference between observed and predicted samples is 45 m, and for the 90% quantile it is <30 m. Nevertheless, a systematic difference exists, with a lower exceedance probability associated with a given abscissa in the simulated sample than in the data. The simulated sample is also much more dispersed and skewed on the left than the dataset. These effects are presumably due to the absence of records of very small avalanches in the database, which causes the runout distance corresponding to a given exceedance probability to be overestimated with the empirical distribution. The simulated sample is thus arguably closer to reality. However, it is not possible to check this assumption since the basis on which certain small events were ignored in the past (threshold altitude or minimal deposit volume, etc.) is not precisely known.

Table 10.

Comparison between data and simulated runout distances

The abscissas corresponding to any return periods (e.g. the classic periods of 10, 30, 100 or 300 years) are obtained simply by considering the associated quantile of the runout distance distribution using Equation (27). Agreement between data and the one-to-one relationship between runout distance and return period derived from the simulated sample is quite good, except for the data corresponding to the highest recorded runout distance (Fig. 8b). This is because the empirical return period computed for this latter avalanche is highly unrealistic, as it necessarily nearly corresponds to the length of the observation period. The simulated sample gives a return period of 340 years for this event, which seems much more realistic and is consistent with the calibrated value of μ = 0.16.

Monte Carlo confidence intervals have been computed for a few return periods using Equation (28). Their width ranges from 5 to 10 m depending on the abscissa considered (Table 11). This indicates that the number of simulations performed is sufficient, even for evaluating runout distances corresponding to return periods >100 years. Indeed, such widths are within the order of magnitude of the discretization step of the numerical propagation, so better precision cannot be expected with a larger number of simulations. The variable width of the confidence interval is worth special mention. On a regular slope, it increases with the return period, since more and more simulations are required to precisely evaluate decreasing exceedance probabilities. Here, however, this is not the case, because of the irregular topography in the runout zone: when the local geometry constrains avalanches to stop because of a slope increase, the exceedance probability is precisely estimated, so the confidence interval is small (e.g. 3 m for T = 5 years and 5 m for T = 30 years). By contrast, when the local slope remains constant or increases, different runouts can be obtained for avalanches with very close dynamical properties, so the corresponding exceedance probability is harder to evaluate and the confidence interval is larger (e.g. 10 m for T = 10 years).

Table 11.

Runout distance versus return period: posterior mean and Monte Carlo confidence interval

4.4. Coulombian friction coefficient

Figure 9 presents the distributions of μ_T , the Coulombian friction coefficient of the avalanches exceeding runout abscissas corresponding to return periods of T = 10, 30 and 100 years. Note that these distributions become more irregular as the return period increases because few avalanches obviously exceed high-return-period abscissas, thus increasing Monte Carlo error. With 20 000 simulations, there are slightly more than 200 centennial avalanches since the mean avalanche frequency is slightly lower than one event per year for the case study. The three distributions are skewed to the left, because avalanches that reach a high abscissa have predominantly low friction coefficients. This also explains why the mean of the distribution decreases with the return period, ranging from 0.314 for a 10 year return period to 0.2 for a 300 year return period. This confirms that the lowest calibrated value of 0.16 is due to an extreme avalanche, with a return period greater than 300 years. Finally, the standard deviation of μ_T remains constant whatever the return period and is approximately 0.07, little more than half the overall standard deviation .

Fig. 9.

Distribution of the Coulombian friction coefficient versus return periods of (a) 10 years, (b) 30 years and (c) 100 years. Only the exceedances of the corresponding abscissa are retained (e.g. for T = 30 years, the abscissa has a 0.033 annual probability of being reached).

4.5. Flow velocities, flow depths and Froude numbers

Figure 10 presents the distribution of maximal velocities, maximal flow depths and Froude numbers at the abscissa corresponding to a return period of 10 years. Predicted maximal flow depths are nearly uniformly distributed between 0 and 3.5 m, but major decennial avalanches show flow depths up to 10 m. Corresponding maximal velocities range between 0 and 20 m s⁻¹,with a well-marked modal value close to 5 m s⁻¹,but a probability of 0.2 to observe maximal velocities higher than 10 m s⁻¹ (Table 12). This latter value is of practical interest since it corresponds to the probability of observing a dynamic pressure in the free-surface snow flow higher than the classic threshold of 30 kPa with the chosen mean snow density of 300 kg m⁻³. Finally, decennial avalanches are mainly associated with Froude numbers between 1 and 2.5, but much more dynamical flows are also possible, with Froude numbers >4. This is related to the slope at the 10 year abscissa, which is still significantly steep.

Fig. 10.

Distribution of (a) velocity, (b) flow depth and (c) Froude number for a decennial avalanche.

Table 12.

Maximal velocity versus return period

For higher return periods, a few avalanches still exhibit high velocities, flow depths and Froude numbers. However, these quantities globally decrease as the return period increases. For instance, most of the avalanches that exceed return period abscissas >30 years show low flow depths and low velocities (Table 12). The low velocities occur because the slope globally decreases with the abscissa, which decreases the dynamics of the flow and stops more and more avalanches. The low flow depths associated with high runouts are explained by the low friction coefficients of the avalanches reaching these high abscissas (Fig. 9), dry fluid flows being rather thin. Finally, for return periods of 30 and 100 years, the mean of the Froude number distribution is very close to 1, and few avalanches still show Froude numbers >3 (Table 13). Because of the slope profile, the mean and maximal values are slightly higher at the 100 year than at the 30 year return period abscissa.

Table 13.

Froude number versus return period

4.6. Reynolds numbers and drag coefficients

Reynolds numbers can be derived from Froude numbers using Equation (5). The distribution obtained depends strongly on the diameter of the obstacle considered. With a small obstacle (d ₀ = 0.25 m), the distribution shows an exponential tail at a decennial abscissa (Fig. 11b), with a mean value around 10. However, for a few avalanches the Reynolds number given by Equation (5) is unrealistically high and had to be set at 200 to allow realistic drag coefficient and impact pressure computations. For a larger obstacle (d ₀ = 5 m), Reynolds numbers are much more dispersed, so for many avalanches they had to be set at 200 (Fig. 11c). As for Froude numbers, lower Reynolds numbers are observed at the 30 year return period abscissa than at the centennial abscissa because of the topography of the path (Table 14).

Fig. 11.

Drag coefficient versus Reynolds number (a) and Reynolds number for a decennial avalanche for two sizes of obstacle, 0.25 m (b) and 5 m (c). The relationship between Reynolds number and drag coefficient is for a prismatic obstacle shape.

Table 14.

Reynolds number versus return period

With Reference Naaim, Faug, Thibert, Eckert, Chambon and NaaimNaaim and others’ (2008) formula, the Cx distribution is a direct consequence of the distribution of Reynolds numbers. With a large obstacle, the assumptions of hydrodynamics for a prismatic shape are nearly fulfilled at the decennial abscissa, with all values very close to 2 and maximal values not higher than 2.4 (Fig. 12c). For a small obstacle, this is not true, with drag coefficients ranging between 2 and 12 and with a modal value around 6 (Fig. 12b). With Reference Sovilla, Schaer, Kern and BarteltSovilla and others’ (2008) formula (Fig. 12a), the results obtained are very close, which is not illogical since the experimental measurements were done on a pylon, which is in fact a small obstacle. The main drawback using this instead of Reference Naaim, Faug, Thibert, Eckert, Chambon and NaaimNaaim and others’ (2008) formula is that drag coefficients <2 are generated for certain avalanches, which is unrealistic in the studied case of a prismatic obstacle.

Fig. 12.

Drag coefficient for a decennial avalanche, evaluated with Savilla’s experimental formula (a) and Naaim’s semi-empirical formula for two sizes of obstacle, 0.25 m (b) and 5 m (c).

4.7. Impact pressures

At all the abscissas considered and whatever the formula used, the pressure distributions obtained are very strongly skewed to the right, with a modal value close to zero and an exponential tail because of the velocity square dependency (Fig. 13). Most of the avalanches are therefore characterized by low pressures in the runout zone, but very high values can be obtained for a few events. This is critical for hazard mitigation and indicates that, for the structural design of a defense structure or of an exposed building, very high impact pressures must be considered even if such events are very rare.

Fig. 13.

Dynamic pressure in the free surface flow (a) versus impact pressure evaluated with Naaim’s formula (b) for a decennial avalanche.

The impact pressures computed using Reference Naaim, Faug, Thibert, Eckert, Chambon and NaaimNaaim and others’ (2008) formula for a large obstacle are, at a decennial abscissa, close to the dynamic pressures in the free surface flow (Fig. 13a). This is not surprising given the values of the drag coefficient at this abscissa. The impact pressures computed for a small obstacle (Fig. 13b) or with Reference Sovilla, Schaer, Kern and BarteltSovilla and others’ (2008) formula are much higher (e.g. nearly twice as high on average as using Reference Naaim, Faug, Thibert, Eckert, Chambon and NaaimNaaim and others’ (2008) formula (Table 15)). With each formula, the probability of an event producing an impact pressure higher than the classic limit of 30 kPa is easily obtained: 0.21 for a large obstacle, which nearly corresponds to the probability of observing a maximal velocity higher than 10 m s⁻¹,but 0.48 for a small obstacle (Table 15). This indicates that at the decennial abscissa the classic threshold of 30 kPa is exceeded every 50 years on average for a large obstacle, but nearly every 20 years on average for a small obstacle.

Table 15.

Impact pressure for a decennial avalanche

The differences between the formulas apply whatever the return period considered. For example, the probability of a centennial avalanche inflicting a pressure greater than 30 kPa is only 0.13 if the dynamic pressure in a free surface flow is studied, whereas it is 0.25 with Reference Naaim, Faug, Thibert, Eckert, Chambon and NaaimNaaim and others’ (2008) formula for a small obstacle (Table 16). All these results indicate that a constant drag coefficient equal to 2 can possibly be used to compute impact pressures on a large obstacle, but that a much higher drag coefficient must be used for a smaller obstacle if one wants to use a constant value. However, given the large range of variation of the drag coefficient for a small obstacle, our results also suggest that it is much more reasonable to compute the Cx value to be used for a given reference event using the flow properties.

Table 16.

Impact pressure for a centennial avalanche

5.1. Identifiability, prior information and prior sensitivity

5.2. Advantages and disadvantages of the proposed MH algorithm

Beyond the question of the theoretical feasibility of inference, there remains the difficulty of its practical implementation. Like all MCMC methods, the MH algorithm has the advantage of being consistent with the direction of an avalanche model’s specification, i.e. the candidate values are generated for the input variables and the credibility of the outputs is evaluated after the propagation. Moreover, the MH algorithm is very general, unlike the Gibbs sampler (Reference Geman and GemanGeman and Geman, 1984). In theory, Bayesian inference using the MH algorithm and suitable informative priors should therefore be able to achieve the calibration of any avalanche propagation model. In practice, however, obtaining a good numerical approximation of the posterior pdf may be extremely tricky because of a too low convergence or numerical traps.

Even if convergence for the ξ parameter is difficult because of the high autocorrelation level of the MCMC chains, the algorithm proposed in this paper has proved its efficiency in the case study. One of its main advantages is that it is sequential, which reduces for each jump the difficulty of finding a new point of relatively high credibility in the parameter space. When the algorithm is tuned, this makes relatively high jump strengths correspond to the optimal acceptance rates, thus reducing the burn-in period (only 1000 iterations for the case study). The proposed algorithm may therefore be a good starting point for any avalanche practitioner or scientist willing to use their own depth-averaged propagation model within a Bayesian statistical framework. One must, though, keep in mind that the jump functions proposed in this paper are case-study specific, and, for a new case study, the strength of the different marginal jumps must be tuned again with respect to Reference Gelman, Carlin, Stern and RubinGelman and others’ (1995) optimal acceptance rates, which can be difficult and time-consuming.

More generally, even if its sequential nature makes the proposed algorithm relatively efficient, computation times remain quite high, first to reach convergence (burn-in period) and then to obtain a good approximation of the posterior pdf. A first option to reduce these computation times would be to test even more efficient versions of the MH algorithm to explore more quickly the regions of high probability as soon as they are reached using adaptive jump strengths. A second option would be to abandon the MH algorithm and to use a noniterative numerical method such as importance sampling (Reference Parent and BernierParent and Bernier, 2007, ch. 14), with an auxiliary distribution based on the inferential results from a much simpler statistical–dynamical model (Reference Eckert, Parent and RichardEckert and others, 2007b). This would not necessarily be technically easier given the large dimension of the parameter space.

5.3. Why a depth-averaged model with a Voellmy friction law?

5.4. Stochastic modeling choices

5.5. Reference scenarios for avalanche hazard management