A Simplified Classification of the Relative Tsunami Potential in Swiss Perialpine Lakes Caused by Subaqueous and Subaerial Mass-Movements

Historical reports and recent studies have shown that tsunamis can also occur in lakes where they may cause large damages and casualties. Among the historical reports are many tsunamis in Swiss lakes that have been triggered both by subaerial and subaqueous mass movements (SAEMM and SAQMM). In this study, we present a simplified classification of lakes with respect to their relative tsunami potential. The classification uses basic topographic, bathymetric, and seismologic input parameters to assess the relative tsunami potential on the 28 Swiss alpine and perialpine lakes with a surface area >1 km2. The investigated lakes are located in the three main regions “Alps,” “Swiss Plateau,” and “Jura Mountains.” The input parameters are normalized by their range and a k-means algorithm is used to classify the lakes according to their main expected tsunami source. Results indicate that lakes located within the Alps show generally a higher potential for SAEMM and SAQMM, due to the often steep surrounding rock-walls, and the fjord-type topography of the lake basins with a high amount of lateral slopes with inclinations favoring instabilities. In contrast, the missing steep walls surrounding lakeshores of the “Swiss Plateau” and “Jura Mountains” lakes result in a lower potential for SAEMM but favor inundation caused by potential tsunamis in these lakes. The results of this study may serve as a starting point for more detailed investigations, considering field data.


INTRODUCTION Background
Historical reports and recent studies have shown that tsunamis do not only occur in the ocean, but also in lakes where they may cause large damages and casualties. The cause for the displacement of large amounts of water can be due to a large variety of triggers, including subaqueous and subaerial massmovements (SAQMM and SAEMM, respectively) triggered by earthquakes. The occurrence of tsunami events within Swiss lakes of various size and depths is documented in several reports ( Table 1).  (Huber, 1982) SAEMM AD 1982: 2-3 m Kehrsiten (Huber, 1982) SAEMM AD 1982: 3-4 m Gersau (Huber, 1982) SAEMM AD 1963: 4 m Obermatt (Huber, 1982) SAEMM AD 1964: 15 m Obermatt (Huber, 1982) SAEMM AD 2007: 5-6 m Obermatt, 1-1.5 m Weggis (Fuchs and Boes, 2010 A well investigated example in Lake Lucerne with wave runup heights of 3-4 m triggered by SAQMM is the 1601 event assigned to the Mw ∼ 5.9 Unterwalden earthquake (Siegenthaler et al., 1987;Schnellmann et al., 2002;Monecke et al., 2004;Fäh et al., 2011). Another documented example is a tsunami (run-up > 5 m) triggered by a spontaneous river delta collapse in Lake Lucerne in 1687 (Siegenthaler and Sturm, 1991;Hilbe and Anselmetti, 2014;Hilbe and Anselmetti, 2015). A more recent event of a rockfalltriggered tsunami (also called impulse-wave) has been reported by Fuchs and Boes (2010): On July 20, 2007, a SAEMM with a total volume of 35,000 m 3 occurred in multiple phases at a closed quarry that is located directly at the shore. The resulting waves with observed heights between 1 and 1.5 m caused some damage at the opposite lake shore (∼3.5 km away from the tsunami source). Fuchs and Boes (2010) estimated the maximum wave height close to the tsunami source to 5-6 m ( Table 1). Shore collapses, mostly triggered by human activity in the past ∼150 years, have also been responsible for triggering impulse waves on many Swiss lakes (Huber, 1980;Huber, 1982 and references therein). In addition to single mechanisms identified as tsunami triggers, cascading effects have also caused tsunamis, such as in the case of the "Rossberg" subaerial landslide that mobilized soft sediments on a swamp plane laterally, which, in turn caused a tsunami with an estimated wave height of ∼15 m on Lake Lauerz in 1806 AD (Bussmann and Anselmetti, 2010). Similarly, in Lake Geneva, a subaerial rockfall is assumed to have triggered a partial collapse of the Rhone Delta, which led to the 563 AD tsunami with modeled wave heights of ∼8 m arriving at the city of Geneva (Kremer et al., 2012).
Potential lake tsunamis resulting from mass-movements as well as the tsunami hazard to date can only be estimated with models. Case studies on tsunamis triggered by SAEMM and SAQMM exist for selected sites in specific lakes (Fuchs and Boes, 2010;Hilbe and Anselmetti, 2015;Strupler et al., 2018c). These studies indicate clearly that there is a potential for future tsunamis on Swiss perialpine lakes. As detailed assessments of the tsunami hazard caused by mass movements require the acquisition of vast amounts of high-resolution geophysical and geological data, it is important to make a preselection of the lakes to be investigated, before evaluating the tsunami potential on a specific lake in detail and with considerable costs. The main aim of this study is therefore to classify all Swiss lakes >1 km 2 (engineered reservoirs excluded) according to their relative tsunami potential caused by SAQMM and SAEMM. Results of such a rapid classification will be used to prioritize lakes for a detailed data acquisition and numerical modeling. Lakes with a relatively low tsunami potential can then be excluded from further analyses. In the following paragraphs, an overview about characteristics of tsunamis that are triggered by SAQMM and SAEMM is given. In the term "mass movements," we include both landslides and rockfalls.

Tsunami Generation by SAEMM
Due to the alpine and perialpine environment, several Swiss lakes are surrounded by steep slopes that may trigger SAEMM. Volumes of reported SAEMM in Swiss lakes have been mostly in the range between a few 1′000 to 1 million m 3 (Huber, 1980). Impulse waves generated by SAEMM have been extensively studied for decades with hydraulic scale-model experiments (Hager and Evers, 2020). Compared to field surveys in the aftermath of an event, where only maximum run-up heights may be tracked along the shores (Roberts et al., 2013), this approach allows for measuring wave characteristics under controlled laboratory conditions (Heller et al., 2008;Evers et al., 2019b). Among the experimental studies conducted in 2D wave channels, Heller and Hager (2010) covered the most extensive range of experimental parameters, including slide volume, slide density, slide thickness, slide porosity, slide impact velocity, slide impact angle, and still-water depth. The slide impact velocity, slide thickness, slide mass, and slide impact angle were found to be the governing 2D parameters: Generally, greater slide impact velocities and masses, i.e., slide volumes for constant slide density, as well as flat impact angles, lead to larger wave heights. Considering a simple block slide model as proposed by Körner (1976), the slide impact velocity is mainly controlled by the drop height, the slope angle, the dynamic bed friction angle, and the gravitational acceleration. A maximum wave height therefore requires an optimal balancing between impact velocity and impact angle when all other slide parameters are considered constant. Heller and Hager (2014) identified a slide impact angle of 51.6°to provide the best conditions for efficient wave generation on a constantly inclined slope. A vertical impact of a SAEMM leads to smaller waves compared to the optimal slide impact angle, due to a less efficient slide to wave energy transfer. Considering only the parameters imposed by the topography, large drop heights and steep slope angles induce high slide velocities. Based on experiments in a wave basin, Evers et al. (2019a) found the slide width to be an additional governing parameter for 3D wave generation and propagation: The wider a slide, the larger the wave.
Tsunami Generation by SAQMM SAQMM include subaqueous landslides and delta collapses. The occurrence of SAQMM is mainly dependent on a favourable topography, a necessary amount of sediments, and a trigger mechanism (Nadim et al., 1996). Previous work on Swiss lakes has shown that most documented landslides occur on slopes with inclinations between ∼10 and 25° (Schnellmann et al., 2006;Hilbe et al., 2011;Strasser et al., 2011;Strupler et al., 2018b). Many of these slides are initiated within a weak layer at the transition from Late Glacial to Holocene sediments (e.g., Strasser et al., 2007;Strasser et al., 2011;Strupler et al., 2017). To date, the yet unfailed lateral slopes of the investigated lakes are covered with a ∼3-10 m of potentially mobile, Holocene sediment drape.
Important properties of SAQMM to estimate the characteristic amplitude of resulting waves (i.e., directly above the landslide source area) are the landslide volume, the landslide acceleration, and the submergence depth of the centroid of the landslide below lake level (Watts et al., 2005;Tappin et al., 2008). Generally, a larger slide volume leads to larger wave amplitudes, and a greater central submergence depth of a landslide leads to smaller wave amplitudes.
The basin depth can have an influence on the wave amplitude during generation, as the amplitude is also dependent on the Froude number Fr [i.e., ratio between landslide velocity u and the shallow-water wave celerity c (Løvholt et al., 2015;Glimsdal et al., 2016, Eq. 1 Slides that move at velocities close to the shallow-water wave celerity (i.e., Fr ≈ 1) will generally increase the wave amplitudes (Ward, 2001).

Tsunami propagation and Inundation
After its generation, the wave will propagate across the basin. Dispersion (i.e., the spreading of energy due to different wave celerities for waves with different wavelengths) can cause wave trains that change their shape with distance from the tsunami source and the geometry of the water body (e.g., Glimsdal et al., 2013;Evers et al., 2019b). In zones where the wave amplitudes are much smaller and the wavelengths are much larger than the stillwater depth h, the tsunami propagation velocity c can be modeled with the linear shallow water theory: In very narrow valleys, the wave cannot spread radially. During propagation into shallow areas in proximity of shores, the wave develops an increased surface elevation (due to shoaling) and can have devastating effects onshore (e.g., Hafsteinsson et al., 2017).

Existing Approaches for Comparing Tsunami Hazard
Different approaches for comparing the tsunami hazard on multiple lakes and fjords exist. Romstad et al. (2009) conducted a geospatial assessment of the relative rockslide-induced tsunami hazard for Norwegian lakes larger than 0.1 km 2 by calculating a (tsunamigenerating) topographic rock slide potential for 18,976 lakes. They assume that all subaerial cells with slope inclinations larger than 30°a re potential landslide-release cells, and that only landslides with volumes >5,000 m 3 entering a lake causes a tsunami, based on empirical knowledge and numerical simulations. The volumes of the potential landslides possibly reaching the lake are estimated from an empirical relationship involving the required mobility of each cell, which is represented by a head to horizontal distance of a travel path ratio. Hermanns et al. (2012Hermanns et al. ( , 2013 propose a hazard and risk classification system for large unstable rock slopes, which includes structural site investigations and analysis of the activity of the slopes. Based on this classification methodology, Hermanns et al. (2016) classify 22 mapped rock slopes and do i) a volume computation, ii) run-out assessments, iii) assessment of possible wave propagation and run-up if a rockfall enters a water body, and iv) an estimation of people exposed to rock avalanches and rockfall-induced tsunami waves. The results of these studies build on multiple years of systematical mapping of unstable rock-slopes and are to be used as support tool for risk management.
In contrast to these studies, our goal is to estimate the relative tsunami potential on peri-alpine lakes that is caused both by FIGURE 1 | Location of the Swiss (non-reservoir) lakes with surface areas <1 km. Labels refer to Table 1. Geodata used with permission from swisstopo.
Frontiers in Earth Science | www.frontiersin.org September 2020 | Volume 8 | Article 564783 SAEMM and SAQMM. In this study, we do not aim at including site-specific field measurements. Rather, we conduct a desktop analysis of the tsunami potential and the related consequences, based on parameters that are derived mainly from previous studies on peri-alpine lakes. In contrast to the workflow of Strupler et al. (2019), that estimates the location and characteristics of potential SAQMM within a specific perialpine lake basin, the methodology presented uses a countrylevel scale, comparing the tsunami potential on various lakes.

Regional Setting
In Switzerland, a total of 28 lakes with surface areas greater than 1 km 2 (engineered reservoirs excluded) exist ( Figure 1; Table 1). Of these lakes, Lake Geneva has the largest surface area (∼580 km 2 ), while Lake Maggiore has the greatest water depth (372 m). Four of the lakes share borders with neighboring countries, i.e., France (Lake Geneva), Germany, and Austria (Lake Constance), and Italy (Lakes Maggiore and Lugano). Of the investigated lakes, 14 are located in the Alps, 13 on the Swiss Plateau, and one in the Jura Mountains. The origin of these lakes is related to subglacial erosion as they represent glacial overdeepenings. Since de-glaciation after the Last Glacial Maximum, deposition of sediments has been ongoing in the lake-basins.
The lakes with the largest surface area are found in the "Swiss Plateau" region, which is geologically formed by sediments from the Molasse basin and which is characterized by a relatively smooth topography. The "Swiss Plateau" is the region in Switzerland with the highest population density (e.g., Henriod et al., 2016).
Geologically, the Central and Southern Alps consist mainly of crystalline rocks, the Northern Alps of limestones and marls, and the Molasse basin consists mainly of conglomerates and sandstones. The Jura mountains are rich in limestones.
It is estimated that earthquakes with a magnitude 6 or greater are expected to occur every 50-150 years in Switzerland (Wiemer et al., 2016). The highest earthquake hazard can be found in the regions Valais, Basel, and Grisons. Earthquakes in these regions are generally a result of the collision between the European and African plates.

METHODOLOGY AND DATA General Methodology and Data
In the following, a methodology for the classification of the tsunami potential is presented and applied to Swiss lakes with surface areas greater than 1 km 2 (engineered reservoirs excluded). The automated workflow is implemented in R (R Core Team 2018). Geospatial operations are either conducted directly in R or calculated in ArcGIS, which can be steered from within R using the package "RPyGeo" (Brenning et al., 2018).
First, five input parameters (IP1-IP5; Table 2) contributing to the tsunami potential are calculated for each lake. These parameters are discussed in detail in Parametrization below. After their calculation, the parameters are normalized by their range (Normalization of the Input Parameters). In general, a larger input value means a larger contribution to the tsunami potential. Next, a classification of investigated lakes, according to  (Aronow, 1982): Inverse of the actual shoreline length divided by a hypothetical shoreline length for a perfect circle with the actual lake area The more complex a lake shape (i.e., the larger the ratio between the actual shoreline and the hypothetical shoreline length for a perfect circle), the lower the general tsunami potential on the whole lake. This is assumed as for complex lakes with many basins only a few basins may be affected

IP5: Potential for inundation
Low-lying shore zones. Ratio of zones below lake level up to <5 m above mean lake level within 1,000 m shore-strip around shoreline to total area of 1,000 m shore-strip Lakes surrounded by a greater percentage of low-lying areas can be affected by larger inundated areas SDR, shoreline development ratio.
Frontiers in Earth Science | www.frontiersin.org September 2020 | Volume 8 | Article 564783 their potential for SAEMM (IP1) and SAQMM (IP2) is conducted. Shorelines used in the workflow are taken from SwissTLM3D (swisstopo). Only the outer shorelines are considered, shorelines of islands in lakes are not considered. As topographic elevation model, SRTM (Shuttle Radar Topography Mission) data is used (Jarvis et al., 2008). The dataset has a spatial resolution of 90 m and is used due to the data availability also alongshore border lakes in non-Swiss territory. For a large part of the investigated lakes, highresolution digital bathymetric datasets SwissBATHY3D (swisstopo) are available. For various lakes, however, bathymetric data has to be interpolated from isobaths (SwissMap Vector 10/25 data; swisstopo). For comparability reasons, both datasets are resampled to a grid resolution of 20 m.

Parametrization
Five different input parameters ("IP1"-"IP5") are identified as crucial for the estimation of the tsunami potential ( Table 2). As we ultimately aim at (de)selecting lakes for further investigations, depending on the potential for tsunami generation and the potential for consequences of tsunamis, we include both these aspects in the term "tsunami potential." "IP1"-"IP3" focus on the tsunami-generating potential, while "IP4" and "IP5" focus on the tsunami consequences. The five parameters are selected to represent the first-order tsunami potential derived from basic topographical, bathymetrical, and seismological input parameters, due to their simplicity.

IP1: Potential for SAEMM
For the parameterization of the potential for tsunamis generated by SAEMM for each lake, it is important to assess i) the potential for SAEMM that enter the water, and ii) their potential to generate a tsunami. To answer ii), estimations of expected volumes entering the water are crucial. Making statements about likely locations of mass failures requires an understanding of factors and processes relevant for slope instabilities as well as their spatial variability (Fischer et al., 2012). Without knowing the local site conditions, topography is often used as a proxy for potential mass movements (e.g., Coe et al., 2004;Fernandes et al., 2004;Cauzzi et al., 2018). The Fahrböschung (Heim 1932) is defined as where H equals the fall height and L the horizontal runout distance. The Fahrböschung can thus be interpreted as the slope angle from the top of a slide to its runout. Equation 3 is often used to estimate the travel distance of a mass movement, depending on its volume. As the volumes of such potential SAEMM alongshore the investigated lakes are unknown, our model is based on a very simple assumption: Rocks tend to mobilize for Fahrböschung >30° (Gerber, 1994;Heinimann et al., 1998), therefore we calculate the Fahrböschung for each pixel of the SRTM DEM down to its closest point on the shoreline. These calculations are made for each pixel within the watershed around each lake, which we limit to a buffer zone of 5 km around each lake's shoreline (in order not to get very large watersheds in the relatively flat zones of the Swiss Plateau). This value of 5 km corresponds also to the runout distance of the Rossberg landslide, one of the major historic landslides in Switzerland (volume: ∼40 Million m 3 ; Thuro et al., 2006). The input parameter representing the relative tsunami potential posed by SAEMM for each lake (IP1; before normalization) is then estimated by calculating the ratio of pixels with Fahrböschung >30°to the total amount of pixels in the watershed area. Hence, due to the lack of landslide-volume information, we assume here that any potential landslide entering the water may generate a tsunami (which is a conservative assumption). By calculating the Fahrböschung for each pixel of the DEM to the shoreline, potential landslide source zones with locally steep slope inclinations that are too far away from the shoreline (and thus getting a low Fahrböschung value) are not considered as sources of landslides that may reach the lake.

IP2: Potential for SAQMM
The parametrization of the potential for SAQMM is quite simple and straightforward: As subaqueous landslide source areas in Swiss perialpine lakes tend to occur on slopes with inclinations between 10 and 25° (Schnellmann et al., 2006;Hilbe et al., 2011;Strasser et al., 2011;Strupler et al., 2018b), the ratio between the amount of pixels with inclinations between 10 and 25°to the amount of pixels belonging to the lake's slopes (here defined as slope inclinations >5°) is used as input parameter representing the potential for SAQMM (IP2). For the lakes Lugano and Maggiore, which share boundaries with Italy, SwissMap Vector 10/25 data (swisstopo) to interpolate bathymetries is partly not available for the Italian territory (∼12% and ∼43% of the respective lake's area are not covered; see Supplementary Table S1; Supplementary  Figures S1 and S2). Therefore, potential SAQMM that may occur in these zones of missing bathymetry data are not considered. The omission of these zones is discussed in Quality and Limitations of the Relative Tsunami-Potential Classification.

IP3: Potential for Seismicity
The potential for seismicity at each lake site is given by the seismic hazard levels in terms of elastic 5%-damped Spectral Acceleration at vibration period T 0.3s − SA(0.3s) for a mean exceedance probability of 10% in 50 years (SuiHaz2015; Wiemer et al., 2016) at each lake center point. The SA(0.3s) values at each lake center were obtained through interpolation of the data of the national Swiss hazard map using ordinary kriging. The seismic hazard values are valid for a reference rock with an average shear-wave velocity of the uppermost 30 m of the soil (Vs 30 ) of 1,100 m/sec. Potential site amplification due to the lake sediments was not considered, as models are still being developed. We did not use Peak Ground Acceleration due to its intrinsic strong saturation with magnitude and distance, that implies comparatively poorer representation of the earthquake sources dominating the hazard at a given location. Mid-to-long period spectral ordinates should be preferred as seismic shaking parameters for the exercise at hand; however, SuiHaz2015 results for T > 1s should be used with caution, as some of the ground motion models used for SuiHaz2015 are better constrained at short and mid periods Frontiers in Earth Science | www.frontiersin.org September 2020 | Volume 8 | Article 564783 (due to the larger number of records used for calibration.) With this background, we finally opted for SA(0.3s), that has the additional advantage of showing a good correlation with macroseismic intensity shaking for damaging events in Switzerland (Panzera et al., under review).

IP4: Inverse Shoreline Development Ratio
It is assumed that for tsunamis occurring in lakes featuring complex shapes with multiple basins, geometric effects could limit the main damage to a single basin. The amount of wave energy transferred around bends also depends on the wave length relative to the lake width. For narrow lakes, long wavelengths can be transmitted without loss of energy (Harbitz, 1992). Oppikofer et al. (2019) state that numerical simulations of SAEMM-induced tsunamis show reductions in wave heights by 30% or more for perpendicular changes in wave direction, which is often the case for fjord-type lakes with multiple basins. To account for the complexity of a lake's shape, an input parameter calculating the inverse of the "shoreline development ratio (SDR)" (Aronow, 1982) is calculated for each lake (IP4). The SDR is calculated from the ratio of the shoreline length for a hypothetical, perfectly circular lake with the same surface area to the actual shoreline length. Higher values mean less complex lake shapes and thus higher potential damage for large parts of the lake shores.

IP5: Inundation Potential
The second parameter related to the tsunami-damage potential ( Table 2), is called inundation potential (IP5).
The assumption made here for parameterization is that low-lying areas (here defined as <5 m above mean lake level) are particularly prone to tsunami inundation. IP5 is obtained by calculating the ratio of the number of pixels that are located in the elevation range from below lake level up to 5 m above lake level to the total amount of pixels within a buffer zone of 1,000 m around the lakeshore. The 1,000 m buffer is arbitrarily chosen, based on modeled inundation distances caused by potential Lake Lucerne landslidetsunamis (Hilbe and Anselmetti, 2015).

Normalization of the Input Parameters
In order to obtain similar ranges for each IP, each IP is normalized by the range of the values for all lakes (i.e., the minimum value of each IP equals 0 and the maximum value of each IP equals 1). For the IPs that represent ratios (i.e., all IPs except IP3), it is thus important to note that this normalization does not mean that a value of 1 corresponds to a calculated ratio of 100%. Non-normalized IP values can be found in the Supplementary Table S2.

Classification by Main Tsunami Sources
Classification by main tsunami sources (IP1 and IP2) is done with a k-means cluster analysis algorithm (Hartigan and Wong, 1979). The goal of this approach is to construct different lake classes that share common characteristics, i.e., similar combinations of IP1 and IP2 values.

Prioritization by Additional Preconditioning Parameters (IP3-IP5)
The lakes in each class are further prioritized by the additional input parameters IP3-IP5. As the tsunami potential for each lake needs to be assessed with regard to a specific purpose, we do the prioritization for each class by sorting it according to IP3-IP5 separately (i.e., we do not aggregate IP3-IP5).

Input parameters for Each Lake
The input parameters for each lake are shown in Table 3 and their spatial distribution are shown in Figure 2. Table 3 and Figure 2 show that: •

Main Tsunami Source Classes
Four different clusters have been created with the k-means clustering algorithm applied to IP1 and IP2 (Figure 3): One cluster with a low potential for both SAEMM (IP1) and SAQMM (IP2) ("class I," gray, amount (n) 8), one cluster with a high potential for SAQMM (IP2) but low potential for SAEMM (IP1) ("class II," cyan, n 11), one cluster with a medium potential for SAEMM (IP1) and high potential for SAQMM (IP2) ("class III," brown, n 7), and one cluster with a very high potential for SAEMM (IP1) and high potential for SAQMM (IP2) ("class IV," purple, n 2). No cluster exists for the combination of a high potential of SAEMM (IP1) but low potential of SAQMM (IP2) (Figure 3).
The spatial distribution of the lakes, colored according to the identified main tsunami potential classes, is shown in Figure 4. Lakes of class I only exist north of the Alps (Swiss Plateau and Jura Mountains). Lakes of class II predominate on the Swiss Plateau, but also occur in the Alps. All class III and IV lakes are located in the Alps.

Prioritization by IP3-IP5
Results of the prioritization of the lakes in classes I-IV (cf. Figure 4) according to IP3, IP4, and IP5, respectively (Table 4), are shown in the following:

DISCUSSION
The proposed workflow allows for a classification of lakes to be investigated more in depth with regard to the respective tsunami triggers. Although landslide-generated waves are complex hazards (e.g., Bullard et al., 2019), the simple parametrization of inputs contributing to SAEMM and SAQMM-induced tsunamis should facilitate identifying the relative tsunami potential for each lake.

Tsunami Potential on the Investigated Lakes
The definition of four different lake classes according to their main tsunami-source (i.e., SAEMM, SAQMM, or a combination of both) gives a first overview on what potential source to consider for each lake. In the Alps, class III [i.e., medium potential for SAEMM (IP1) FIGURE 2 | Spatial distribution of the normalized input parameters.
Frontiers in Earth Science | www.frontiersin.org September 2020 | Volume 8 | Article 564783 and high potential for SAQMM (IP2)] and class IV [i.e., very high potential for SAEMM (IP1) and high potential for SAQMM (IP2)] lakes dominate (Figures 1, 4). Both parameters IP1 and IP2 express the abundance of favourable topographic conditions for massmovements (i.e., Fahrböschung > 30°for SAEMM and subaquatic slope ranges 10-25°for SAQMM, respectively). The high values of IP1 are related to the fact that many alpine lakes are surrounded by relatively steep slopes. For Lake Oeschinen ( Figure 5), which is evaluated as having the greatest potential for SAEMM-induced tsunamis, traces of 11 rock-falls that have occurred during the last 2,500 years could be identified at the bottom of the lake (Knapp et al., 2018). The high mean recurrence rate of 200-300 years between the single events supports the high score in our simple model. Also, the SAEMM-induced tsunamis described in Huber (1982) have occurred in Lake Walen and Lake Lucerne. Both lakes show a relatively high potential for SAEMM (IP1) according to our approach. The comparison of the evaluated potential for SAQMM with documented events show that traces of underwater landslides were found in most of the lakes with a high IP2 score. On the one hand, this can be interpreted as validation of the approach. On the other hand, relatively recent (i.e., younger than a few thousand years) mass movements have decreased the potential for SAQMM occurring in the near future at the same locations, as the slopes need to be re-charged with sediment to become unstable again. It is therefore important for a hazard assessment to further investigate if lakes with historically documented tsunamis that were triggered by SAQMM still have a high potential for such events to recur. However, for comparability reasons between all investigated lakes that build on different dataset qualities (e.g., high-resolution bathymetric and seismic data are not available for all investigated lakes), the history of SAQMM on the lateral slopes is not considered in our simple approach.
The observation that no class for lakes with a high potential for SAEMM but low potential for SAQMM exists, and that lakes closer to the Alps show a generally higher potential for SAQMM,  may be related to the topographic and geologic predisposition during the glacial excavation of the subsurface: In alpine valleys that are surrounded by steep rock walls, the ice masses were laterally confined and thus the glaciers were thick (Bini et al., 2009), exerting considerable pressure on the substratum, leading to a steep bedrock topography. In contrast, for lakes located on the Swiss Plateau, further from the Alps, the glaciers were able to spread laterally due to the absence of steep rockwalls, which resulted in thinner local ice thicknesses of piedmont-style glaciers, and probably smoother excavations of the bedrock. Certainly, the local geological and geotechnical variability (i.e., relatively soft rocks of the "Molasse" vs. mainly harder rocks of the "Alpine nappes") must have contributed as well to these differences. On class III/IV lakes, detailed investigations on potential tsunamis generated by SAEMM and SAQMM are recommended. In lakes of class II the potential for SAQMMgenerated tsunamis needs to be analyzed more in-depth. For lakes of class I, we do not see an urgent need for further tsunami investigations. Therefore, class I lakes are not considered further in this paper.
Whereas IP1 and IP2 indicate a general predisposition for SAEMM and SAQMM, which was used for the classification into four classes, IP3-IP5 can be used to prioritize between lakes within each class.
The purpose of this study is not to identify and decide on which specific lake should be investigated in more detail, but rather to indicate lakes with a high potential for tsunamis caused by different tsunami sources. The presented results are intended as a guideline for the selection of lakes for further studies, and prioritization of lakes should be based on additional parameters that include IP3-IP5 (Table 4), as well as practical considerations (e.g., acquisition time, funding, and inclusion of risk aspects, such as vulnerability and exposure). • If we assume that most of the mass-movements are triggered seismically, then the prioritization could be made based on IP3 for each class. In this case, lakes that need to be investigated first are lakes Oeschinen, Sils, and Walen for class III and IV, and lakes Silvaplana, Thun, and Sarnen for class II. • If we focus on whether a potential tsunami could mainly affect single basins and not necessarily entire lakes, then prioritization could be made based on IP4 for each class. In class III/IV, lakes that need to be investigated first in this case are lakes Oeschinen, Poschiavo, and Brienz. In class II, lakes Baldegg, Aegeri, Hallwil, and Sarnen would have priority for further investigations. • If we focus on the consequences of potential tsunamis, here characterized by the potentially inundated fractions of each lake's shore zone (up to 1 km inland), then the prioritization could be based on IP5 for each class. No lake in class III, which indicates a high potential for SAEMM and SAQMM, has a high inundation potential (IP5). This makes sense, as for a high SAEMM potential (IP1) large parts of the lakeshore needs to be surrounded by a steep topography, which, in turn conflicts with a high inundation potential (IP5), which is parametrized by low-lying areas along the shore. However, lakes in class II (which are characterized by a high potential for SAQMM) that have a relatively high inundation potential are the lakes Constance, Baldegg, and Hallwil. Fortunately, the lakes with the highest inundation potential are the lakes of class I, which do not show a high tsunamigenic potential.

Quality and Limitations of the Relative Tsunami-potential Classification
Due to the limited amount of local site data available for each lake (e.g., no information about expected volumes of potential SAEMM), the nation-wide approach presented here is only based on basic topographical, bathymetrical, and seismological input parameters and thus gives only a broad overview of the relative tsunami potential and main expected triggers. For a full assessment, sitespecific geological characteristics (such as acquired for potential SAEMM in Norway; Hermanns et al., 2016) are required. However, despite its simplicity, the method presented here is able to identify lakes with priority for further investigations. Nevertheless, the presented methodology to calculate the various input parameters certainly oversimplifies certain aspects: • As the volumes of mass movements displacing the water are crucial for the estimation of potential tsunami waveamplitudes, our simplified methodology is not able to estimate wave heights. At this scale of investigation and with the limited area-wide information available, it is out of scope to assess potential wave heights for each lake, considering the complex interplay between multiple landslide characteristics (see Background). • Additionally, it would be difficult to compare estimated wave heights with the heights documented in historical sources, as, unfortunately, it is rarely documented where and how the waves or their run-up were measured. For assessing the impact at the shore, it is crucial to know whether the wave in the deep water, nearshore, or after shoaling has been described (e.g., Huber, 1980;Fuchs and Boes, 2010). • Sensitivity analyses showed that the prioritization according to IP3 depends on the selected hazard parameter. If, for example, Peak Ground Acceleration instead of SA(0.3s) is chosen, a few lakes will slightly change positions in the ranking (Supplementary Figure S60). This however has no impact on the lakes tsunami classes discussed in the paper. Also, soft sediments, such as occurring on the lake bottom, may amplify seismic shaking considerably. These amplification effects have been neglected in the present study, as consolidated experimental results are not yet available. An ongoing project of the Swiss Seismological Service at Swiss Federal Institute of Technology Zurich is collecting amplification values at the subaqueous slopes and expects them to be remarkably different from those observed onshore. • To calculate IP5, the ratio of zones lower than 5 m above lake level within the zone of 1 km inland along the shore is calculated. A downside of this approach is that it neglects the micro-topography, e.g., a moraine ridge around the lake may limit the potential inundation, and thus a low-lying area within this shore zone that is located behind such a micro-topographic elevation may contribute to the inundation potential of a lake, but in reality the moraine ridge would hinder the flow (unless overtopping occurred) (c.f. figures in Section 6 of Supplementary Material). • The relatively coarse resolution of the topographic and bathymetric datasets used (SRTM data with 90 m grid resolution) and resampled SwissBathy3D/interpolation from SMV10/25 data (20 m grid resolution) are in our opinion sufficient for such a categorical analysis. Simple tests with a topographic elevation model of better resolution (DHM25) surrounding lakes where existing showed that the relative ranking of the lakes of IP1 did not change. • The fact that small parts of the SMV 10/25 isobaths of Lakes Lugano and Maggiore are missing on the Italian territory (Supplementary Figures S1 and S2) is not expected to change the results of our classification, as the input parameter (IP2) is calculated by the ratio of the pixels with a slope inclination between 10-25°to the total slope area (defined as pixels with inclinations >5°). Both lakes Lugano and Maggiore have a high value of IP2. The missing parts are not likely to lower the IP values considerably, regarding the general morphology of the lakes (Supplementary Figures S43 and S45), and their Alpine setting on both the Swiss and Italian side.
The documented historical tsunami events in Swiss perialpine lakes can be used to validate our simplified classification approach. It is worth noting that the historical SAEMM-and SAQMM-tsunami events have occurred on lakes that are evaluated as lakes of classes II and III in our approach, indicating lakes with a high SAQMM-or combined SAEMMand SAQMM-tsunami potential, with the exception of the tsunami that occurred on Lake Lauerz (Table 1; Bussmann and Anselmetti, 2010 and references therein). According to our classification, Lake Lauerz shows a low tsunamigenic potential posed by SAEMM and SAQMM ( and 4). However, the Rossberg landslide significantly changed the lake's shape and size; it has become much smaller with a center further away from the failed mountain slope (Bussmann and Anselmetti, 2010). It would be interesting to compare the tsunami potential for the pre-Rossberg-slide bathymetry to the bathymetry to date and to analyze if the tsunami potential has been reduced. Furthermore, Bussmann and Anselmetti (2010) interpret the tsunami originating from a cascading event, as the mass movement itself did not reach the lake. The subaerial landslide mobilized soft sediments on a swamp plane laterally, which, in turn formed an indenter into the lake causing a tsunami wave. Such cascading effects are not considered in our simplified classification. A cascading effect is also assumed to have caused the AD 563 Tsunami in Lake Geneva (Kremer et al., 2012).

CONCLUSIONS AND OUTLOOK
In this study, a simplified workflow for the classification of the tsunami potential, caused by SAEMM and SAQMM, respectively, in Swiss perialpine lakes, was presented. The results of this study may serve as a starting point for more detailed investigations (e.g., numerical modeling), also considering more field data. Findings show that lakes located within the Alps show generally a higher potential for SAEMM and SAQMM, due to the often steep surrounding rock-walls, and the fjord-type topography of the lake basins with large portions of the lateral slopes lying in the unstable range (i.e., ∼10-25°). In contrast, the low lying topography along the shores of the lakes in the Swiss Plateau and Jura Mountains favor inundation caused by potential tsunamis on these lakes. Our results further indicate that all investigated lakes with high potential for SAEMM also have a high potential for SAQMM. The converse is not true, not all lakes with a high potential for SAQMM do have a high potential for SAEMM. We recommend that detailed investigations of the SAQMM-caused tsunami hazard should focus on lakes of classes II-IV (n 20), and of the SAEMM-caused tsunami hazard on the classes III and IV (n 9), prioritized by the additional input parameter (IP3-IP5) according to the main purpose of a potential study.
Due to its simplicity, this methodology could also be applied to other lakes worldwide. The minimum of required inputs include digital-elevation raster data, bathymetric raster data, shoreline vector data, and earthquake accelerations. The approach presented herein can be extended by adding further input parameters (e.g., considering cascading hazards). In the context of global warming and thawing of permafrost regions, the parametrization of the potential for subaerial massmovement may include data extracted from permafrost maps. Furthermore, information about vulnerability and exposure (e.g., degree of building development and type of building) along the shores may be included, when prioritizing specific lakes for more in-depth investigations, especially when considering potential economic damage.

DATA AVAILABILITY STATEMENT
The data analyzed in this study is subject to the following licenses/restrictions: The swisstopo geodata that were used to extract the various Input parameters are copyrighted by swisstopo. However, they can be viewed by everyone for free on maps.geo.admin.ch, but not downloaded. Requests to access these datasets should be directed to the Swiss federal geoportal: maps.geo.admin.ch.

AUTHOR CONTRIBUTIONS
MS: formal analysis, methodology, visualization, and writing-original draft (lead); FE, KK, CC, PB, DV, RB, and DF,: review and editing. FA and SW: funding acquisition, review, and editing.