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Article

Slope Failure in a Period of Increased Landslide Activity: Sennwald Rock Avalanche, Switzerland

by
Selçuk Aksay
1,2,3,*,
Susan Ivy-Ochs
1,2,
Kristina Hippe
2,
Lorenz Grämiger
1 and
Christof Vockenhuber
2
1
Department of Earth Sciences, ETH Zürich, Sonneggstrasse 5, CH-8092 Zürich, Switzerland
2
Laboratory of Ion Beam Physics, ETH Zürich, Otto-Stern-Weg 5, CH-8093 Zürich, Switzerland
3
Soil Geography and Landscape Group, Wageningen University, P.O. Box 47, NL-6700 AA Wageningen, The Netherlands
*
Author to whom correspondence should be addressed.
Geosciences 2021, 11(8), 331; https://doi.org/10.3390/geosciences11080331
Submission received: 7 July 2021 / Revised: 31 July 2021 / Accepted: 2 August 2021 / Published: 5 August 2021
(This article belongs to the Special Issue Cutting Edge Earth Sciences: Three Decades of Cosmogenic Nuclides)
Browse Figures
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Abstract

:
The Säntis nappe is a complex fold-and-thrust structure in eastern Switzerland, consisting of numerous tectonic discontinuities and a range of hillslopes prone to landsliding and large slope failures that modify the topography irreversibly. A slope failure, namely the Sennwald rock avalanche, occurred in the southeast wall of this fold-and-thrust structure due to the rock failure of Lower Cretaceous Helvetic limestones along the Rhine River valley. In this research, this palaeolandslide is examined in a multidisciplinary approach for the first time with detection and mapping of avalanche deposits, dynamic run-out modelling and cosmogenic nuclide dating. During the rock failure, the avalanche deposits were transported down the hillslope in a spreading-deck fashion, roughly preserving the original stratigraphic sequence. The distribution of landslide deposits and surface exposure age of the rock failure support the hypothesis that the landslide was a single catastrophic event. The 36Cl surface exposure age of avalanche deposits indicates an age of 4.3 ± 0.5 ka. This time coincides with a notably wet climate period, noted as a conditioning factor for landslides across the Alps in the mid-Holocene. The contemporaneity of our event at its location in the Eastern Alps provide additional support for the contention of increased regional seismic activity in mid-Holocene.

1. Introduction

The Sennwald landslide is a rock avalanche associated with the Lower Cretaceous Helvetic limestones in the southeast wall of the Säntis nappe along the Rhine River valley. Similar catastrophic events constantly reshape the topography and permanently change landscapes, constituting a threat for human life in mountainous terrains such as the European Alps [1,2,3,4]. Understanding the patterns, triggering factors and failure mechanisms of landslides is a challenge, particularly for palaeolandslides as they exhibit insufficient topographic evidence to detect the fingerprints of landsliding [5]. It is well-known today that several factors can provide favourable conditions for slope failures and increase in landslide activity regionally, yet the final trigger is often strong ground shaking [2,6], or lengthy wet periods associated with heavy rainfall or storm events [7]. Although individual research on several landslides indicates both climate and seismic triggers, conditioning and triggering factors for landsliding at an Alpine scale are still under debate [7,8,9,10,11,12,13]. To address this problem and understand the landslide patterns, more palaeolandslide sites in the Alps such as the Sennwald landslide should be examined with field mapping, geochronological dating techniques and numerical modelling.
In the past decades, various types of landslides with different triggers have been examined with the recent development of age determination techniques [11]. The first dated catastrophic landslide using cosmogenic nuclides was the Koefels landslide in Austria [14,15], and it was followed by the Flims, Switzerland [16], and Fernpass, Austria [17], landslides. The investigation of landforms with dating techniques has contributed key aspects in our understanding of spatio-temporal landslide distribution patterns and their interaction with climate change in the Alps [9,11]. In particular, dating of mass movements with volumes larger than one million cubic meters using one or a combination of geochronological dating techniques brought a new dimension to the examination of past occurrences and allowed us to forecast future trigger events with respect to their frequency and size [5,11].
Earlier research showed that the inherited rock structure also plays an important role in rock slope stability and occurrence of landslides in various tectonic scales [18,19]. The position and geometry of the hillslope, rock type, orientation of bedding and sliding planes with respect to topographic surface and faults also influence the slope failure type and behaviour [20]. Regarding the rock type, high water supply due to heavy rainfall may result in fluid infiltration through faults and fractures [21] particularly in karstic rocks. In rocks affected by karstification, the maximum fluid pressure on the clay and mud permeability barrier on the sliding plane might generate gravitational catastrophic failures [7]. Understanding the structural complexity and geology of slope failure therefore is of great importance for modelling such occurrences with better accuracy. The modelling of such rock failures should be supported with meticulous reporting of field mapping data of both release and deposition areas. Mapping of landslide-related morphological features such as toma hills or the distribution pattern of landslide deposits in the deposition area is another key aspect in landslide research. A toma (i.e., cone-shaped hill) is a typical hill structure at various sizes made of landslide deposits and commonly seen in rock avalanche related events in the Alps [22]. Identifying such geomorphological features provides useful information in establishing landsliding patterns on a regional scale.
In landslides, both the release and deposition areas, and hillslope morphology are irreversibly affected in different ways depending on whether the landslide is triggered by storm and rainfall events, or earthquakes [23]. The permanent change in the topography can be identified for bedrock landslides triggered by different events at an orogen scale [2,13,23]. Earlier studies established that the topographic fingerprints of storm- and earthquake-related landslides can be distinguished with respect to the distribution of the landsliding in the hillslope at the time of the failure, whether sliding material clusters at ridge crests, toes of the hillslope or is uniformly distributed in the entire hillslope. Most Alpine landslides have not been investigated in terms of the topographic fingerprint identification for landslides with different triggers including the Sennwald landslide.
The Sennwald landslide area has been a site of curiosity for engineers and geologists over the last few decades. This site has been studied by geological companies previously, and they provided a good understanding of the subsurface of the landslide deposition area by borehole data. However, the timing and run-out behaviour of this palaeolandslide were not entirely investigated previously and there is a lack of a comprehensive field mapping. To address some of these open questions, we introduce a multidisciplinary examination of the Sennwald landslide with mapping of the landslide deposits, dynamic run-out modelling using DAN3D and surface exposure dating using cosmogenic 36Cl as well as an analysis of potential triggers and causes of the landslide. We also present the estimated landslide volume and role of the stratigraphic position in slope failure. We believe that including this palaeolandslide in the inventory of Alpine landslides and rock avalanches with volumes larger than one million cubic meters is quite essential, especially with detailed field reporting and age control (i.e., cosmogenic nuclide dating). Additionally, the landscape change in the hillslope and Rhine River valley with respect to erosional processes and landsliding are explained in this work.

Tectonic Setting and Geology

The Sennwald landslide occurred in the Säntis nappe at the eastern end of the Helvetic nappes, which formed as a result of collision between the European and Adriatic plates [24] (Figure 1). The Helvetic nappe consists of allochthonous sediments on top that were overthrust in a northerly direction [25]. The entire nappe system was cut into two nappe systems by a major thrust, namely the Glarus thrust; the upper Glarus known as the Säntis nappe and the lower Glarus nappe [26,27]. The Säntis nappe is a complex fold-and-thrust (i.e., anticline-syncline folding) structure with axial planes dipping dominantly NW-SE in eastern Switzerland (Figure 1). It consists of numerous tectonic discontinuities [26,28,29] that form a range of hillslopes prone to large slope failures. The parallel-striking thrust and detachment faults of this complex structure caused propagation and folding mostly following the same parallel trend as the mountain chain [28]. The internal variety of the nappe structure is also due to the influence of numerous strike-slip faults and thrusts [28].
The release area of the landslide is within the Lower Cretaceous Helvetic limestones. The simplified stratigraphic unit from bottom to top is Vitznau Marl, Betliskalk, Helvetischer Kieselkalk, Drusberg Formation, Schrattenkalk, and Helvetischer Gault. The stratigraphic description of each rock unit in the landslide area is given below.
  • Vitznau Marl (Valanginian) [29] consists of mainly marly limestones and is a fossiliferous and clay-rich unit at the base.
  • Betliskalk (formerly Valanginienkalk) [29] is mostly bio-pelsparites and biomicrites with fine grain, brownish to greyish and weathered sand with chert nodules. The weathering colour is grey. Betliskalk is stratigraphically on top of Öhrlikalk and Vitznau-Mergel.
  • Helvetischer Kieselkalk (Valanginian-Hauterivian) [30,31] consists of siliceous limestone from dark grey to bluish grey colour and is known to be rich in glauconite and pyrite. It shows a mixture of calcareous particles, calcified sponge spicules and detrital quartz in a matrix of micritic to microsparitic calcite.
  • Drusberg Formation (Barremian) consists of dark blue-grey calcareous shales regularly alternating with thin-bedded light-brownish limestones. Drusberg layers represent autochthonous fauna that consists of sponge spicules, echinoderm fragments and some radiolarians [32]. Oysters and other bivalves, ammonites and nautilids are also noted [33].
  • Schrattenkalk (Early Barremian-Early Aptian) [34] is a grey to light grey marine limestone with bioclastic wackestone-packstone, and well-sorted grainstones. Coral, rudist, Nerinea, brachiopod, Porifera, Orbitolinid, echinoid, bivalve and brachiopod are noted in Schrattenkalk [33]. In some parts, detrital quartz and sometimes brecciated lithoclasts are seen in this formation.
  • Helvetischer Gault (Late Aptian-Middle Cenomanian), Reference [29], also known as Garschella Formation, consists of greenish to greyish glauconitic sandstones, marls and nodular and sparitic carbonates. Ammonoids, bivalve, belemnite, nautilids, brachiopods and planktonic foraminifera are identified.

2. The Sennwald Landslide

2.1. The Release and Deposition Areas

The examination of the release and deposition areas in the landslide site was conducted with field mapping supported by the GIS analysis using high resolution (2 m ± 0.5 resolution) swissALTI3D digital elevation models, local geological map of the Säntis sheet of the Swiss Geological Atlas Nr. 78 with explanatory notes [35,36] and literature [26,28]. The analysis of the stratigraphy and rock structure was also made available to provide an insight to demonstrate the failure type of the landslide [37,38,39,40].
The cross section of the inherited rock structure shows that the dip angle of the bedding plane of limestone units in the release area varies between 50–65° SE, and each unit is parallel to each other (Figure 2). The dip angle of the sliding plane is also 50° SE, which is almost parallel to the bedding plane. The parallel position of the bedding and sliding planes to the surface topography is a major component that works for the favour of slope failure as shown in Figure 2.
The landslide material covers an area of about 6 km2 on the alluvial plain along the Rhine River valley (Figure 3). Landslide boulders and blocks of different rock units from the Lower Cretaceous Helvetic limestone are identified at various dimensions at different locations in the landslide deposition site (Figure 4); 2 × 2 × 1 m3 being the smallest and 9 × 8 × 7 m3 the largest boulder. Most of them are covered with lichen and vegetation (Figure 4). As mentioned in the introduction, several hill-like structures, namely toma, are also observed in several locations in the alluvial terrace [41,42,43] (Figure 4). Tomas are thought to have formed due to the interaction of the spreading moving mass with the substrate in Alpine rock avalanche events. A wet alluvial substrate, as here in the Rhine River plain, is especially conducive to the formation of such extensional surface features [22].
Sediments of the post-failure ongoing erosional activity on the hillslope cover most of the deposition area today. Soft sediments and loose material were continuously transported from the mountain slope since the failure event forming alluvial fans and gullies at the toe of the hillslope. Forestation and vegetation dominate the general landscape in the entire landslide deposition area as well as swamps in places. Fourteen samples from limestone boulders in the deposition area were collected during the field mapping for lithological analysis and 36Cl surface exposure dating (Figure 5). Further explanation on sampling and sample processing is given in “surface exposure dating using cosmogenic nuclide 36Cl” section.

2.2. Distribution of the Landslide Material in the Deposition Area

A comprehensive lithological identification of limestone units was necessary to understand the post-failure distribution pattern of these units in the landslide deposition area. The identification of different limestone units was made based on the textural properties of each limestone unit with hand specimens in the field and thin sections under the microscope (Figure 6). The textural and lithological properties are correlated with the published data in the literature for cross validation (also see “tectonic setting and geology” section). The examination of thin sections and hand specimens shows that five limestone units were involved in the rock failure, namely (stratigraphically from bottom to top), Betliskalk, Kieselkalk, Drusberg, Schrattenkalk and Helvetischer Gault (Figure 2 and Figure 5).
Based on field observations, landslide deposits form radial and linear hills (i.e., longitudinal ridges) in plan view in the deposition area (Figure 3) (also see [12,44]). The linear hills are orientated radial and transverse to the direction of the flow. Hills range up to 5–10 m in height above the general ground surface. Further, the landslide material deposited in a spreading-deck fashion, preserving the original stratigraphic positions between strata [45]. Blocks from stratigraphically the top layer (i.e., Schrattenkalk) in the rock formation travelled the farthest, and blocks derived from stratigraphically the lowest layer (i.e., Betliskalk) travelled the least during the landslide. This release pattern results from shearing along boundaries between geological units (e.g., zones of weakness). This information provides a good understanding for the slope failure pattern and distribution of the landslide material.
The spreading-deck distribution of the landslide deposits might also indicate a single and rapid failure. If the failure would have occurred in multiple events, limestones of various lithological units would form an irregularly distributed mass of lithologies in the deposition area rather than forming a pattern preserving the original stratigraphic position after the failure. Some irregularly distributed smaller rock bodies of different limestone lithologies are found in the landslide deposition site, which might contradict the spreading-deck distribution style hypothesis of the landslide material. However, this might be due to the rapid movement of the rock mass which entangled and dragged relatively smaller limestone blocks of different lithologies.

2.3. Cross Profiles for the Release and Deposition Areas

Previously produced cross section of the landslide deposition area based on borehole data [46] shows earlier depositional environments in the landslide deposition area (Figure 7). These data provide useful information for our understanding of the past landscape and sediment transport dynamics from the hillslope to the valley as well as the impact of landsliding on reshaping the topography.
After slope failure, the rapid mass movement in Sennwald changed the morphology of the Rhine River valley as landslide deposits ploughed into the existing pre-landslide Rhine gravels and fluvial/lacustrine sediments. Similar events, where landslide deposits block river valleys and change fluvial regimes, are addressed with case studies in the literature [47,48]. Consequently, the river channel shifted towards E-SE, which enabled post-landslide Rhine gravels to be deposited along the present-day riverbank and the channel (Figure 7).
As shown in the cross section, the debris spreads over fluvial and lacustrine sediments during the landslide event. Afterwards, younger fluvial sediments continuously accumulated on landslide deposits around the present-day valley channel. These marked fluvial fluctuations below and above the landslide deposits indicate an ongoing sediment discharge and load levels of the Rhine River for that time. The slope material (i.e., alluvial fan and debris flow) both below and above the landslide deposits indicates pre- and post-failure ongoing erosional processes (i.e., annual sediment transfer via mountain creeks). The borehole data indicates some sediments with unknown thickness of lacustrine environment below the fluvial and lacustrine sediments, possibly indicating that the valley floor used to be lacustrine environment with transitions to delta and fluvial environments before the landslide event. This information is also consistent with suggested palaeo-lake and -river levels of Quaternary valleys in northern and eastern Switzerland [49].
Extensive work to reconstruct the shape of the overdeepened valleys in the Swiss Alps, formed during the course of glacial/interglacial cycles, provides a good overview of solid rock surface-Quaternary cover boundaries [50,51]. Despite the lack of seismic reflection data in the Sennwald area [52,53], the bedrock surface-Quaternary cover boundary (i.e., depth of the rock surface) for the Sennwald area along the Rhine valley is fairly well-known based on both the reconstructions mentioned above (Figure 8). The geological cross section, which shows the complexity of the rock structure, was made available based on the local geological map, the Säntis sheet of the Swiss Geological Atlas No. 78 [35,36]. As shown in the geological cross section and indicated in those overdeepening reconstructions, the bedrock in the region of the landslide is 10–50 m below the ground surface.

3. Surface Exposure Dating Using Cosmogenic 36Cl

Sampling locations for cosmogenic nuclide dating (Figure 5) were chosen uniformly in the deposition area to evaluate the surface exposure age distribution of landslide boulders. Following the sampling with criterion given by Ivy-Ochs and Kober (2008) [54], samples were prepared as suggested by Ivy-Ochs et al. (2004) [55]. Total Cl and 36Cl were determined at ETH AMS facility with isotope dilution methods as suggested in the literature [56]. The ETH internal standard K381/4N with a value of 17.36 × 10−12 is used to normalise 36Cl/35Cl ratios, and the stable 37Cl/35Cl ratios are standardised to the natural 37Cl/35Cl ratio 31.98% [57,58]. Surface exposure ages are calculated with a numerical code [59]. The production rate of 54 ± 3.5 36Cl atoms g(Ca)−1yr−1 defined for limestones, with a muon contribution of 9.6%, is used for exposure age calculations [60,61]. We used a surface erosion rate for karstified limestones of 0.5 cm/ka for all samples [62,63,64].
Cl concentrations vary between 4.45 ppm and 19.56 ppm as shown in Table 1. These are rather low total Cl concentration values, which means that the production of 36Cl was dominantly from Ca. Thus, the low energy neutron capture 36Cl production pathway was negligible. The elemental analysis (XRF) is performed to reveal the trace and major element concentrations, and thus the influence of major and trace elements to 36Cl production. The results of XRF analysis also show that trace element concentrations are not significant in 36Cl production in our samples (see Appendix A Table A1). Samples SW-5, 6, 7 and 8 (i.e., rocks of Helvetischer Kieselkalk) showed no reaction with the 2M nitric acid (HNO3). Therefore, these four samples were not considered for further procedure.
The mean 36Cl surface exposure age is 4.3 ka with a mean error margin ±0.5 ka. Calculated ages show a uniform distribution in the deposition area with similar ages ranging from 3.7 ka to 5.0 ka except for two samples. Sample SW-2 reveals a relatively shorter exposure age, 2.3 ± 0.1 ka, whereas sample SW-9 reveals a longer exposure age, 6.5 ± 0.4 ka. SW-9, Helvetischer Gault stratigraphically the top layer, was possibly exposed to cosmic rays previously due to its position on the hillslope before the rock failure. The surface exposure age of sample SW-10, Betliskalk (stratigraphically bottom layer), is 4.4 ± 0.3 ka. This indicates that samples (except for SW-2 and 9) show similar surface exposure ages regardless of their (i) distribution in the deposition area and (ii) original stratigraphic position on the hillslope. The similarity of exposure ages provides support for the hypothesis that the Sennwald landslide was a single rock failure.
The mean surface exposure age is also in agreement with the 14C age, 4150 ± 80 14C yr [65], which we calibrated using OxCal online v4.2.4 [66,67]. Our calibration of 14C ages from previously dated wood pieces taken from the 21–21.5 m depth of borehole VI-21 (for borehole location see Figure 5, Figure 6 and Figure 7) reveal 4852–4442 cal BP with 95.4% probability. The consistency of surface exposure ages and radiocarbon age also supports the single rock failure hypothesis.

4. Dynamic Run-Out Modelling

4.1. Pre-Failure Topography and Volume Estimation

Reconstruction of the pre-failure topography is a key step for volume estimation and dynamic run-out modelling. Our reconstruction of the pre-failure surface is based on the modern topography in the release and deposition areas with fieldwork observations, thickness estimates from the borehole data and GIS examination. The borehole data and our field measurements show that present-day maximum elevation in the deposition area is 460 m a.s.l., and the average thickness of the landslide deposits is ca. 35 m a.s.l., whereas the maximum thickness is ca. 85 m a.s.l. This shows that the maximum elevation of the pre-failure topography in the deposition area in the Rhine Valley was 425 m a.s.l. Furthermore, using the borehole data, reconstruction of pre-failure elevations and boundaries of the deposition area was made with transitional steps as we adjusted each chosen point based on each neighbouring point accordingly.
For the reconstruction of the pre-failure topography, we estimated the volume of the landslide material by subtracting the reconstructed pre-failure topography from the post-failure (present) topography using the borehole data. The subtraction between the pre- and post-failure topographies reveals the height difference (i.e., deposit thickness). The estimated volume of landslide material in the deposition area is 123 million m3 and 92 million m3 in the release area. About 25% of fragmentation bulking factor was calculated following the volume estimates for the deposition and release areas. The bulking factor describes the volume increase due to material dispersion or incorporated material during the run-out on a rock failure and is often suggested to be between 25–30% for similar rock movements [68,69,70].

4.2. Run-Out Simulation

The numerical run-out modelling is performed for the Sennwald landslide using a dynamic simulation modelling software, namely DAN3D, which is generated for mass movements such as landslides and debris flows [71]. DAN3D is a well-tested tool used for constructing landslide events by simulating the landslide material like a flowing rock avalanche [70,72,73,74,75,76]. The software works on the basis of certain inputs such as the elevation and rheology of rock [71]. The purpose of dynamic modelling is to understand the run-out behaviour, acquire and compare landslide deposit thickness with our estimates and confirm our single rock failure hypothesis.
Parameters used for the landslide simulation following criteria in the literature (References therein [70]) have been listed alongside the modelling results in Table 2. We assumed a unit weight of 24 kN m−3 for limestone to perform the modelling in DAN3D. Rheology parameters such as the internal friction angle (which affects the degree of the spreading material) and the friction angle (which represents the basal flow resistance) have been adjusted by trial-and-error to find the best fit for the total run-out distance and lateral spreading of the landslide material in the deposition area [77]. We set the basal friction angle to 16° and internal friction angle 30° after numerous trial runs. The basal friction angle that we applied is within the range of commonly used values for rock avalanches on the basis of earlier research [73,77] (also see [70]).
Figure 9 shows the visual run-out modelling results of selected time-steps with simulated deposit thicknesses and landslide deposition area. The landslide run-out direction is to the southeast. The duration of the simulated run-out is 150 s. The maximum velocity is 93 m/s, and mean velocity is approximately 50 m/s. From the top of the hillslope to the farthest point that landslide deposits reached is 4500 m.
The mean deposit thickness retrieved from the simulation, 24 m a.s.l., is within the expected range of present-day mean thickness in the deposition area measured from the borehole data. Although, the observed mean deposit thickness spatially varies in the deposition area and is slightly greater than the simulated deposit thickness. The thickness variation in observed deposits could be explained by inherited pre-existing morphological features of the pre-landslide topography and estimated bulking factor (i.e., 25%). Additionally, simulated deposits show a more evenly distributed pattern, since DAN3D simulates landslide deposits like a whole flowing material. To partially justify these differences, simulated and estimated velocities have been compared. The minimum velocity (vmin) required to reach the observed runup height (h) has been estimated following the equation below [78]:
vmin = √ (2gh)
where g is gravitational acceleration, and h is the observed maximum deposits thickness (h = 85 m). Our estimated vmin is 41 m/s, which agrees well with the simulated model velocity of 50 m/s. This shows that the simulated velocity and deposit thickness are consistent with our predicted model and observed thickness.
The lateral spreading of simulated landslide deposits does not entirely resemble the field observations in given time-steps in Figure 9. This difference between the simulated and observed extents is partly due to the bulking factor. DAN3D does not take the bulking factor into account for simulation. Therefore, the spread in the present-day topography is greater than the simulated results. Additionally, there were artefact deposits that move independently from the defined run-out path in the simulation particularly after 90 s (also see [76]). Therefore, only representative visual results have been shown in Figure 9. These artefacts are due to the adjustable parameters (e.g., stiffness coefficient, margin cut-off thickness) within the code to provide flexibility to modify the simulation until the best fit is found, and they, in fact, do not indicate any change in the volume. Overall, the results of our run-out simulation support the hypothesis of a catastrophic single failure for the Sennwald rock avalanche.

5. Discussion: Potential Triggers

Examining the spatio-temporal clustering of landslides of similar size is a key aspect for a better understanding of potential enhancing causes of landslides in the context of Alpine (palaeo)landsliding, such as the Sennwald landslide. Most palaeolandslides in the Alpine setting had previously been associated with the after effects of the last deglaciation (i.e., after around 18,000 years ago) before geochronological dating techniques have been widely used [79]. However, examination of around 40 landslides with dating techniques in the Alps showed that they in fact occurred within two periods; around 11−9 ka year (i.e., within the Preboreal period) and around 5−3 ka year (i.e., within the Subboreal period) (Figure 10) [7,12]. In addition, two major climate fluctuations are identified at a European scale: (i) the mostly dry period at 8.2 ka and (ii) the period of long-lasting heavy rainfall at 4.2 ka [80]. Based on 36Cl and 14C data in our work, the Sennwald landslide occurred at 4.3 ± 0.5 ka, which shows a link with this suggested heavy rainfall period. Although there is a debate for the 4.2 ka period as a trigger for mass movements (see [7]), the remote spatial distribution of similar landslide events in various geographical locations in the Alps around this time [12] indicates a climate change influence possibly as a conditioning factor.
In Sennwald, landslide deposits were stratigraphically on top of the Vitznau Marl (i.e., the sliding plane of the landslide), a Valanginian clay-rich limestone-marl alternation [29], on pre-failure state (as indicated in the “tectonic setting and geology” section). Clays are the weakest and most unstable material on slopes at >10° angle due to the parallel internal realignment of the clay particles which reduces the internal friction over time. The contact between this unstable barrier and weakened (i.e., karstified) limestone package might have prepared the conditions for a slope failure with the presence of water possibly with heavy rainfall influence. It should be noted that heavy rainfall periods should occur over a long period of time to be considered as a trigger or enhancing factor for such large landslides [10,106]. As pointed out, mid-Holocene climate changes have had significant effects on hydrological processes in Europe [107,108], influencing the European Alps as a trigger or enhancing factor for large landslides [7].
Although spatio-temporal clustering of landslides is well-identified at an Alpine scale, especially with the research on the past few decades, seismic triggers leading to large-scale slope failures remain not fully understood. Earthquakes may influence the slope stability reportedly in a number of ways based on field research in various landslide sites since the 18th century [6]. Earlier research suggested a link between landsliding and periods of increased neotectonic activity in Eastern Alps in the mid-Holocene [9,13]. Moreover, it is not impossible to associate palaeolandslides with earthquakes using historical earthquake data or seismic interpretation and core analysis on specific layers in lake sediments (see Figure 10) [109,110]. In a recent study, a spatial correlation between large rock avalanches (i.e., Eibsee and Fernpass) and the largest palaeoearthquake imprints recorded in the lakes was made in the Eastern Alps corresponding to 4.1 ± 0.1 ka BP [13]. This site is about 100 km away from Sennwald. In fact, moderate earthquakes occur around Sennwald even today (Figure 5) [111,112]. The earthquake catalogue [81,82] shows several moderate earthquakes (ML = 4–5) with 5–10 km depth associated with the Säntis Thrust in Sennwald (Figure 5 and Figure 10). The spatio-temporal contemporaneity of the Sennwald landslide with other palaeolandslides in the Eastern Alps support our hypothesis for an earthquake-triggered landslide.
The inherited rock structure plays an important role in rock slope stability and occurrence of rock slides as shown in earlier research [18,19]. The position of the hillslope, orientation of bedding and sliding planes and lithological differences may also contribute to the rock failure in various mountainous settings. The vulnerability to fragmentation has mostly been observed in large earthquake-related areas with thrusting, and it especially increases in slopes located on the hanging wall of fault systems [113]. The landslide material in Sennwald similarly originated from the hanging wall (Figure 2) of the Säntis thrust during the rock failure. The seismic shaking most likely caused the reduction of the frictional strength along the southeast dipping sliding plane (i.e., almost parallel to the southeast dipping hillslope) in the hanging wall. Therefore, it was crucial to examine the rock structure and geology with meticulous field mapping for a better understanding of our landslide event.
Furthermore, examining the topographic fingerprints of landslides is of importance to understand landsliding patterns and map palaeolandslides with far greater accuracy and in far greater numbers by using topographic as well as image data. Previous studies statistically examined topographic fingerprints of various landslides associated with climate and earthquake triggers on hillslopes, and they identified different patterns for storm and seismic shaking related events [2]. For example, as mentioned in the introduction, it is suggested that slope failures related to permafrost degradation would have high elevation release areas [114,115], whereas earthquake-triggered landslides may have their bedrock niche along ridge crests (seismic amplification) rather than down in the slope [23]. Heavy precipitation related landslides are expected to originate lower down in the slope [23], and rainfall-induced landslides may originate from the entire slope [2]. These landslide-trigger patterns provide useful insights to distinguish earthquake-triggered landslides from climate-triggered landslides. Our observation on present day topography and analysis on the position of rocks in the pre-failure state with respect to surface topography in the hillslope shows that the landsliding was originated in the ridge crest on the entire slope where the susceptibility to slope failure was greatest. This might support our hypothesis that the Sennwald landslide was possibly linked to heavy rainfall as an enhancing factor in a period of increased earthquake activity.

6. Conclusions

This research is a multidisciplinary examination of a palaeolandslide-related surface change in the southeast slope of the Säntis nappe in eastern Switzerland. The detailed investigation of the time, failure and run-out behaviour of the Sennwald palaeolandslide in this overdeepened Alpine valley are presented for the first time in this work.
Our analysis indicates that the orientation of the bedding and sliding planes worked in the favour of rock failure in Sennwald. Surface exposure ages, performed using cosmogenic nuclide 36Cl from eight samples in the landslide deposition area, reveal that the rock failure occurred in the mid-Holocene with the calculated mean age of 4.3 ± 0.5 ka. The radiocarbon dating age, ca. 4.9−4.4 ka cal BP, supports the surface exposure age of the rock failure. The numerical 3D simulation of the landslide, made based on estimated volume, slope angle and friction angle, shows that 92 × 106 m3 of material moved down the slope in 150 s. The landslide material travelled ca. 2000 m with a maximum velocity of 93 m/s and currently covers an area of about 6 km2 in the deposition area.
The spreading-deck-like release mechanism of the landslide material with almost preserved stratigraphy, results of the DAN3D simulation and the uniform distribution of surface exposure ages in the deposition area support the single-failure hypothesis. The topographic fingerprint of the Sennwald landslide points out earthquake and heavy rainfall influence. Coincidentally, the time of the rock failure corresponds to the increased neotectonic activity in Eastern Alps, which increases our confidence for the hypothesis that the Sennwald landslide was associated with earthquake activity during a heavy rainfall period.

Author Contributions

Conceptualization, S.A. and S.I.-O.; methodology, S.A, S.I.-O., K.H., L.G. and C.V.; validation, S.A., S.I.-O., K.H., L.G. and C.V.; formal analysis, S.A. and S.I.-O.; investigation, S.A. and S.I.-O.; resources, S.I.-O.; data curation, S.A.; writing—original draft preparation, S.A.; writing—review and editing, S.A., S.I.-O., K.H. and L.G.; visualization, S.A.; supervision, S.I.-O.; project administration, S.I.-O.; funding acquisition, S.I.-O. All authors have read and agreed to the published version of the manuscript.

Funding

Fieldwork, laboratory work and AMS measurements were funded by the Laboratory of Ion Beam Physics, ETH Zürich.

Institutional Review Board Statement

Not applicable.

Informed Consent Statement

Not applicable.

Data Availability Statement

The authors declare that the data supporting the findings of this study are available within the article.

Acknowledgments

All members of the Ion Beam Physics group of ETHZ, led by Arno Synal, are thanked for their support of this work, especially those who did shifts during the measurements. We thank Peter Zwahlen for sharing his unpublished 14C dating data taken from boreholes in the Sennwald area.

Conflicts of Interest

The authors declare no conflict of interest.

Appendix A

Table
Table A1. XRF results for chemical compounds with LOI corrected values and trace elements with LOI corrected values used in the age calculations.
Table A1. XRF results for chemical compounds with LOI corrected values and trace elements with LOI corrected values used in the age calculations.
SampleSW-1SW-2SW-4SW-9SW-10SW-12SW-13SW-14
SiO21.3241911.6140.698530.860710.88940.713561.12391.36607
TiO20.009090.025810.011760.009050.009050.008460.00850.0161
Al2O30.094830.584970.097470.098960.095050.103790.085020.24805
Fe2O30.755220.351470.101950.12950.142010.163580.132620.1437
MnO0.012490.009830.00280.005090.006790.003950.003970.00477
MgO0.265180.465770.290730.556470.476950.382450.470980.4973
CaO54.89648.041455.374155.38355.417855.528855.344357.7568
Na2O0.097670.024580.010080.020920.036210.010720.052140.01491
K2O0.023850.146240.015680.020360.022070.018610.021540.05188
P2O50.007380.025810.010080.013570.010750.010150.0170.00716
Cr2O300000000.00012
NiO0.001370.001270.001130.000960.00110.001330.001250.00122
LOI43.752238.455944.452743.869143.828844.006943.7740.6972
Total101.23999.7471101.067100.968100.936100.952101.031100.805
B0.000000.000000.000000.000000.000300.000300.000300.00030
Sm0.000000.000000.000000.000000.000060.000060.000040.00004
Gd0.000000.000000.000000.000000.000060.000060.000050.00005
U0.000000.000000.000000.000000.000400.000400.000500.00050
Th0.0032100.0033100.0039400.0034900.0000200.0000200.0000500.000050

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Figure 1. Tectonic map of the Säntis nappe including major tectonic structures and the landslide release and deposition area. Location bar is shown in the top left corner with the Helvetic nappes indicated with blue. Shaded relief image superimposed by a color-coded DEM (swissALTI3D) reproduced with the authorisation of swisstopo (JA100120). The tectonic map is modified following [28].
Figure 1. Tectonic map of the Säntis nappe including major tectonic structures and the landslide release and deposition area. Location bar is shown in the top left corner with the Helvetic nappes indicated with blue. Shaded relief image superimposed by a color-coded DEM (swissALTI3D) reproduced with the authorisation of swisstopo (JA100120). The tectonic map is modified following [28].
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Figure 2. Cross section across the southern wall of the Säntis nappe showing the sliding plane of the Sennwald landslide (modified from [28]). Cross section line (A-A′) is shown in the Surface Map.
Figure 2. Cross section across the southern wall of the Säntis nappe showing the sliding plane of the Sennwald landslide (modified from [28]). Cross section line (A-A′) is shown in the Surface Map.
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Figure 3. (a) Deposition area of the Sennwald landslide (green-brown) shown in detail on a shaded black and white relief image of Sennwald. (b) Transverse (blue lines) and linear (white lines) ridges indicate flow patterns. Shaded relief image superimposed by a color-coded DEM 15 (swissALTI3D) reproduced with the authorisation of swisstopo (JA100120).
Figure 3. (a) Deposition area of the Sennwald landslide (green-brown) shown in detail on a shaded black and white relief image of Sennwald. (b) Transverse (blue lines) and linear (white lines) ridges indicate flow patterns. Shaded relief image superimposed by a color-coded DEM 15 (swissALTI3D) reproduced with the authorisation of swisstopo (JA100120).
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Figure 4. Field photos showing landslide boulders of various size and surface features in the landslide deposition area. (a) Left: 47°15′29 N–9°29′03 E, 559 m a.s.l., photo direction: 241°. Left top: Sample SW-13: 47°14′39.02 N–9°29′30.02 E, 442 m a.s.l., photo direction: 210°, boulder dimension: 2 × 3 × 1 m. Left bottom: Sample SW-1: 47°15′05.72 N–9°29′54.74 E, 443 m a.s.l., Boulder dimension: 2 × 7 × 3 m. (b) Tomas located on the southwestern side of the landslide deposition area. 47°14′63.38 N–30 9°29′10.33 E, 447 m a.s.l., photo direction: 210°.
Figure 4. Field photos showing landslide boulders of various size and surface features in the landslide deposition area. (a) Left: 47°15′29 N–9°29′03 E, 559 m a.s.l., photo direction: 241°. Left top: Sample SW-13: 47°14′39.02 N–9°29′30.02 E, 442 m a.s.l., photo direction: 210°, boulder dimension: 2 × 3 × 1 m. Left bottom: Sample SW-1: 47°15′05.72 N–9°29′54.74 E, 443 m a.s.l., Boulder dimension: 2 × 7 × 3 m. (b) Tomas located on the southwestern side of the landslide deposition area. 47°14′63.38 N–30 9°29′10.33 E, 447 m a.s.l., photo direction: 210°.
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Figure 5. Surface map showing landslide deposits (grey), the dominant boulder lithologies in each sector (blue, yellow, red, green and pink) in the deposition area and the sampling locations (black asterisks indicated with sample numbers). Moderate earthquake epicentres (red asterisks) are also indicated. Altitude is given by colour code. Shaded relief image of the Sennwald region superimposed by a color-coded DEM (swissALTI3D) reproduced by the permission of Swisstopo.
Figure 5. Surface map showing landslide deposits (grey), the dominant boulder lithologies in each sector (blue, yellow, red, green and pink) in the deposition area and the sampling locations (black asterisks indicated with sample numbers). Moderate earthquake epicentres (red asterisks) are also indicated. Altitude is given by colour code. Shaded relief image of the Sennwald region superimposed by a color-coded DEM (swissALTI3D) reproduced by the permission of Swisstopo.
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Figure 6. Selection of thin sections from landslide deposits (A) Drusberg, sample no: SW-1. (B) Drusberg, SW-2. (C) Schrattenkalk, SW-3. (D) Schrattenkalk, SW-4. (E) Helvetischer Kieselkalk, SW-7. (F) Schrattenkalk, SW-9. See also text.
Figure 6. Selection of thin sections from landslide deposits (A) Drusberg, sample no: SW-1. (B) Drusberg, SW-2. (C) Schrattenkalk, SW-3. (D) Schrattenkalk, SW-4. (E) Helvetischer Kieselkalk, SW-7. (F) Schrattenkalk, SW-9. See also text.
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Figure 7. Cross section of the landslide deposition area. Cross section line (B-B′) and boreholes are shown in Figure 5. Modified after [46].
Figure 7. Cross section of the landslide deposition area. Cross section line (B-B′) and boreholes are shown in Figure 5. Modified after [46].
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Figure 8. Säntis geological cross section—bedrock surface and Quaternary deposits boundary. Cross section line C-C′ is shown in Figure 1. Modified after [36].
Figure 8. Säntis geological cross section—bedrock surface and Quaternary deposits boundary. Cross section line C-C′ is shown in Figure 1. Modified after [36].
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Figure 9. Dynamic run-out modelling showing the thickness of landslide deposits with selected time steps. The dotted area indicated the landslide deposition area determined using DEM in support of field observations. DAN3D numerical modelling code after [71,73].
Figure 9. Dynamic run-out modelling showing the thickness of landslide deposits with selected time steps. The dotted area indicated the landslide deposition area determined using DEM in support of field observations. DAN3D numerical modelling code after [71,73].
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Figure 10. Spatio-temporal distribution of Alpine palaeolandslides shown with instrumental and historical earthquakes epicentres indicated with red circles [81,82]. Circle size indicates the magnitude of the earthquake. Landslides are listed from the oldest to the youngest as follows: around 11–9 ka (blue star): Prättigau 11.5–10.3 ka [83], La Clapiere 10.7–7.1 ka [84,85], Klein Rinderhorn and Daubensee 9.8 ka [70], Koefels 9.5 ka [86], Flims 9.4 ka [87], Tamins 9.4 ka [12], Hochmais 9.3–8.2 [88], Rognier 8.8 ka [89], Obernberg 8.6 ka [90]; around 5–3 ka (green rectangular), Haiming and Vig Vigaun (after [91]), Sechilienne 6.4–0 ka [92], Marocca Principale 5.3 ka [12], Multiple landslides 5.1–3.3 ka [7], Malbosc 5.0–3.0 ka (Braucher, unpublished; from [7]), Lauvitel 4.7 ka [93], Eibsee 4.1 ka [94], Fernpass 4.1 ka [17], Hintersee 3.8 ka [95], Tumpen 3.6 ka [88], Kandertal 3.2 ka [96], Tschirgant 3.0 ka [97], Molveno 4.8 ka [98], Lavini di Marco 3.0–0.8 ka [58], Oeschinensee 2.3 ka [99]; historic landslides (yellow triangle), Matrei, Disentis, Castelpietra, San Giovanni, Masiere di Vedana and Val Pola (after [91]), Fadalto 365 CE [100], Varini 565–970 CE [101], Kas 1100 CE [12], Dobratsch 1348 CE [102], Diableret 1714, 1749 CE, Borta 1692 [103], Goldau 1806 CE, Elm 1881 CE, Vajont 1963 CE, Randa 1991. Multiple events are also shown: Obersee 13.4–5.1, 7.7–3.6 ka [76], Le Pra 12–11, 9–7, 5.0–2.5 ka [104], Les Arcs 11–8.5, 5.5–3.2 ka [105], Cortina and Corvara 10.7–8.4, 8.2–6.9, 5.8–4.5, 4.0–2.1 ka [10], Falli-Hölli 10–9, 5.5–3.2 ka [93]; and landslides with unknown ages (light blue hexagon), Sierre, Engelberg, Klöntal. Hillshade map based on Swisstopo (JA100120).
Figure 10. Spatio-temporal distribution of Alpine palaeolandslides shown with instrumental and historical earthquakes epicentres indicated with red circles [81,82]. Circle size indicates the magnitude of the earthquake. Landslides are listed from the oldest to the youngest as follows: around 11–9 ka (blue star): Prättigau 11.5–10.3 ka [83], La Clapiere 10.7–7.1 ka [84,85], Klein Rinderhorn and Daubensee 9.8 ka [70], Koefels 9.5 ka [86], Flims 9.4 ka [87], Tamins 9.4 ka [12], Hochmais 9.3–8.2 [88], Rognier 8.8 ka [89], Obernberg 8.6 ka [90]; around 5–3 ka (green rectangular), Haiming and Vig Vigaun (after [91]), Sechilienne 6.4–0 ka [92], Marocca Principale 5.3 ka [12], Multiple landslides 5.1–3.3 ka [7], Malbosc 5.0–3.0 ka (Braucher, unpublished; from [7]), Lauvitel 4.7 ka [93], Eibsee 4.1 ka [94], Fernpass 4.1 ka [17], Hintersee 3.8 ka [95], Tumpen 3.6 ka [88], Kandertal 3.2 ka [96], Tschirgant 3.0 ka [97], Molveno 4.8 ka [98], Lavini di Marco 3.0–0.8 ka [58], Oeschinensee 2.3 ka [99]; historic landslides (yellow triangle), Matrei, Disentis, Castelpietra, San Giovanni, Masiere di Vedana and Val Pola (after [91]), Fadalto 365 CE [100], Varini 565–970 CE [101], Kas 1100 CE [12], Dobratsch 1348 CE [102], Diableret 1714, 1749 CE, Borta 1692 [103], Goldau 1806 CE, Elm 1881 CE, Vajont 1963 CE, Randa 1991. Multiple events are also shown: Obersee 13.4–5.1, 7.7–3.6 ka [76], Le Pra 12–11, 9–7, 5.0–2.5 ka [104], Les Arcs 11–8.5, 5.5–3.2 ka [105], Cortina and Corvara 10.7–8.4, 8.2–6.9, 5.8–4.5, 4.0–2.1 ka [10], Falli-Hölli 10–9, 5.5–3.2 ka [93]; and landslides with unknown ages (light blue hexagon), Sierre, Engelberg, Klöntal. Hillshade map based on Swisstopo (JA100120).
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Table
Table 1. AMS-measured 36Cl concentrations and exposure ages with error margins for the Sennwald landslide.
Table 1. AMS-measured 36Cl concentrations and exposure ages with error margins for the Sennwald landslide.
Sample
Code		Elevation
(m)		LatitudeLongitudeShielding36Cl 106
Atoms/g Rock		Cl in Rock
(ppm)		Exposure Ages
(Years)
SW-144347.25169.49850.9920.112 ± 0.0154.5 ± 0.13850 ± 520
SW-244647.25309.49700.9910.065 ± 0.00519.6 ± 0.22340 ± 120
SW-443947.24849.50170.9850.151 ± 0.0089.7 ± 0.25030 ± 310
SW-944547.24159.49000.9900.197 ± 0.01213.6 ± 0.36480 ± 440
SW-1050347.25829.49100.9800.140 ± 0.00713.1 ± 0.24360 ± 260
SW-1244647.24589.48580.9900.114 ± 0.00611.5 ± 0.23770 ± 220
SW-1344247.24429.49170.9900.130 ± 0.00716.0 ± 0.24210 ± 260
SW-1444347.24399.49520.9900.142 ± 0.00715.5 ± 0.24440 ± 250
Table
Table 2. Parameters used for run-out simulation and results.
Table 2. Parameters used for run-out simulation and results.
ParameterValue
Release volume92 × 106 (m3)
Deposition area6 (km2)
Unit weight for limestone24.0 (kN/m3)
Internal friction angle35 (°)
Coefficient of friction0.25
Mean velocity50 (m/s)
Max-min thickness60–20 (m)
Plan travel distance1611 (m)
Total emplacement time150 (s)
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Aksay, S.; Ivy-Ochs, S.; Hippe, K.; Grämiger, L.; Vockenhuber, C. Slope Failure in a Period of Increased Landslide Activity: Sennwald Rock Avalanche, Switzerland. Geosciences 2021, 11, 331. https://doi.org/10.3390/geosciences11080331

AMA Style

Aksay S, Ivy-Ochs S, Hippe K, Grämiger L, Vockenhuber C. Slope Failure in a Period of Increased Landslide Activity: Sennwald Rock Avalanche, Switzerland. Geosciences. 2021; 11(8):331. https://doi.org/10.3390/geosciences11080331

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Aksay, Selçuk, Susan Ivy-Ochs, Kristina Hippe, Lorenz Grämiger, and Christof Vockenhuber. 2021. "Slope Failure in a Period of Increased Landslide Activity: Sennwald Rock Avalanche, Switzerland" Geosciences 11, no. 8: 331. https://doi.org/10.3390/geosciences11080331

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