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Switzerland

Avalanches, Landslides and Rock fall Switzerland

Vulnerabilities - Now: rock fall

Trees appear to be good witnesses to the increase in rock avalanches over time. If a rock hits and damages a tree, the tree repairs that damage. The time of the damage can be deduced from growth rings at the repaired wound. At a site in the Swiss Alps, scientists looked at hundreds of repaired wounds on trees. The number of rock avalanches appeared to have increased sharply in the mid-1980s due to the breakdown of permafrost (50).

The occurrence of rockfall has been observed at high resolution and high frequency in Switzerland during the period 2017–2021. These observations were made at a height in the Alps near the lower limit of permafrost occurrence. All major observed rockfall events occurred in summer, and many of them in the second half of summer and in the (late) afternoon. Rapid permafrost degradation is viewed as a triggering factor of these events, causing progressive failure of the rock wall. This indicates that climate change may already be an important factor in triggering rockfall. The cementing effect of the ice-bonded discontinuities in the rock decreases progressively during the summer at higher temperatures. The observed temporal clustering of the rockfall events in late summer has an important implication for hazard management, potentially endangering hikers making use of the hiking trail in summer (49).

Since the mid-1980s there have been five major rock slides of more than 1 million m3 in the Alps: Veltlin in 1987, Randa in 1991, Mont Blanc-Brenvaflanke in 1997, Thurwiserspitze/Ortler in 2004, and Eiger in 2006. The slide
path sometimes reached far below the forest line (Veltlin, Randa, Mont Blanc) and all except Eiger affected tourism areas (roads, ski slopes, hiking trails). The relationship to glaciers and permafrost has been proven for three of these cases (Mont Blanc, Ortler, Eiger), in the other two it is probable (Veltlin) or likely, but uncertain (Randa) (16).

In the summer of 2003, the 0°C limit rose above 4500 meters elevation for 10 days. This unusual duration increased impacts, especially on shady rock walls at high altitudes, where thaw penetrated considerably deeper than in previous (warm) years and some areas may have been exposed to thawing for the first time. … Thaw penetration below the surface was up to 2 meters deeper than in previous years. These extreme conditions caused widespread but relatively small rock falls, such as the one which forced the evacuation of 90 persons on the Matterhorn. However, deep penetration of permafrost warming and thawing over longer time periods (decades, centuries) might cause larger landslides and rock falls at high altitudes (3).

During the last century, Alpine permafrost in Europe has warmed by 0.5 to 0.8⁰C in the upper tens of meters (5). The stability of steep rock slopes can be reduced due to melting of ice-filled crevices and subsequent build-up of hydrostatic pressure (6). Even prior to thaw, frozen rock joints have been demonstrated to destabilize with rising temperatures, entering a zone of minimal stability between -1.5 and 0⁰C (7). The exceptional rock fall activity during the summer 2003 is likely an indication of this rapid destabilization that takes place as an almost immediate reaction to extreme warming.

In northern slopes, the depth of thaw is mainly controlled by the influence of air temperature (mostly via long-wave radiation) on surface temperatures, whereas southern slopes additionally receive high amounts of shortwave radiation. As a consequence, southern slopes exhibit greater inter-annual variability of thaw depth, larger pre-2003 maxima and, therefore, a smaller 2003 anomaly. … The observed domination of events in northern slopes can be explained by the strong effect of 2003 as well as the greater extent of perennially frozen northern slopes (1).

Vulnerabilities - Now: landslides

Significant trends have not been found in the number of landslides and their impacts (24).  An inventory of 2966 landslides in the French and Swiss portion of the European Alps over the period 1970–2002 (28) shows that the majority of landslides recorded occurred during the spring (March/April/May, 29%) and summer (June/July/August, 36%), with the lowest numbers recorded during autumn (September/October/November, 15%) and winter (December/January/February, 20%).

It is hard to predict changes in landslide occurrence from projected changes in precipitation due to climate change since changes in precipitation patterns are hard to predict at the small-scale. As an alternative approach, changes in weather types can be used as a predictive tool for landslide events under differing future climate scenarios. One should be aware, however, that other factors (such as rainfall persistence, geology and topography) play an important role in the occurrence of landslides as well (28).

Large landslides near glaciers

Ice volume reduction of retreating glaciers leads to debuttressing of oversteepened valley flanks, causing landslides (39) and catastrophic rock falls (40). Failure of such landslides poses significant risks to surrounding settlements and critical infrastructure, because of the formation, and possible breakout of landslide dams, as well as enhanced sediment production, which can lead to debris and mud flows (38). The Great Aletsch Glacier in southwest Switzerland is one of these glaciers where large landslides directly respond to glacier ice loss. Since 1870, the glacier retreated 3 km to its present-day position with a length of about 22 km. For one of these landslides it was found that changes in glacier ice height spatially correlate to rock failures and deformation features at the toe of the landslide. Over a large area the mountain slope reacts to glacier retreat once debuttressing through glacier ice height reduction reaches a critical threshold (38). Outburst floods from landslide-dammed lakes are reported worldwide in areas that undergo deglaciation (41). Knowledge on landslides near the Great Aletsch Glacier suggests that these floods may occur more frequent as a result of on-going rapid deglaciation and destabilization of critical rock slopes (38). 

Vulnerabilities - Now: water and sediment yields in Alpine watersheds

In the face of rapid climate warming, the hydrological and geomorphological dynamics of small (<3 km2) and partially glaciated Swiss Alpine watersheds seem to be changing (35). The change began with the considerable increase in temperature in the second part of the 1980s. As a result the glaciers started to recede (mid-1980s-ongoing) and the contribution of ice melt and snowmelt to river flow increased. Whereas precipitation was the widely dominant water source for streams until the mid-1980s, its relative contribution then started decreasing, although its absolute input remained stable. In addition to ice melt, the snowpack no longer contributes to glacier growth but becomes a subsidy of water yield. Also, thawing of permafrost-related landforms contribute to stream discharge. These changes have caused discharge to almost double in the studied watersheds through the last five decades (35). An increase in annual runoff in similar watersheds is a frequent outcome of rapid climate warming (36).

Along with its discharge the stream’s sediment transport capacity increased, but sediment export did not respond in the same way. The impact of stream discharge increase on sediment transport is not straightforward. Sediment transport depends on the volumes of sediment upstream that are available for transport. If this sediment cannot reach the stream, than discharge may increase but sediment transport increase is lagging behind. This ineffectiveness of available sediment upstream reaching the stream may reduce the extent to which climate forcing of landscape response can be detected in valley-bottom sediment delivery and deposits. Rather, increasing sediment export is a function of extreme events that can move sediments to the streams (35).

As for the future, water yield is likely to increase further, at least until it becomes limited by available ice to melt, and with it sediment transport capacity in the drainage network. According to research (37) maximum annual runoff in Alpine watersheds may be reached by 2050, followed by a tendency to decreasing and/or more variable water yield, although it is still unclear how this timing applies to small, heavily debris-covered glaciers. 

Vulnerabilities – In the future

For the Alps, the main trigger of debris flows is high intensity, short duration rainfall (30). Under future climate change, it is likely that increases in extreme rainfall will alter debris flow frequency (31). Previously, a limited number of climate change impact studies focused on debris flows, with inconsistent results: some indicating less debris flows in the future (32), others more (33), or concluding that accurate quantification of changes in the number of debris flows is not possible (34).

Projections of climate change between 2010 and 2100 have been translated into future debris flow activity for two Alpine catchments, one in France (Barcelonnette Basin) and one in Italy (Fella River catchment) (29). These projections are based on a number of regional climate models (driven by general circulation models) and both an intermediate and high-end scenario of climate change (the so-called RCP4.5 and RCP8.5 scenarios, respectively). From the model outcomes two meteorological proxies for debris flow activity were derived and translated into future debris flow activity: one using 1-day rainfall amounts and one being representative of short-lasting convective rainfall systems. The 1-day rain-proxy was chosen as precipitation is a dominant trigger of debris flows. As rain gauges are very local and often non-catchment representative, the second proxy was used to mimic the mesoscale atmospheric conditions leading to heavy local convective precipitation. All of these projections show either an increase or little change in the number of days with debris flows between now and 2100 (29). 

The overall frequency of debris flows may decrease in absolute terms, but the magnitude of events may increase. This was concluded from an analysis of debris flow events in the past 150 years and using this information for future projections on climate change (regional climate model runs driven by the A1B emission scenario) (26). According to this research, the overall absolute number of days with conditions favorable for the release of debris flows will likely decrease in the second half of the century. A prolongation of the debris-flow season is projected, however, in line with what has been observed as a result of climate warming since 1864 (27). Events might become possible in March, especially in the late 21st century, and in November and December (26).

Rising temperatures and melting permafrost will destabilise mountain walls and increase the frequency of rock falls, threatening mountain valleys (3,5). Besides, higher temperatures might lead to changes in the frequency and intensity of snow and ice avalanches (2).

The vulnerability of settlements and infrastructure to natural hazards, such as flash-floods, avalanches, landslides, rock fall and mudflows will increase due to heavy rain- and snowfalls and the upward shift of the permafrost line. Retreat of permafrost also destabilises the infrastructure in high altitudes like lodges, lifts and top stations (3).

Past and modeled future climatic change is likely more pronounced in mountain areas than the global or hemispheric average (8). … The extreme summer of 2003 and its impact on mountain permafrost may be seen as a first manifestation of the projections of climate change. Wide-spread rock fall and geotechnical problems with human infrastructure are likely to be recurrent consequences of warming permafrost in rock walls due to predicted climatic changes (1).

In wintertime, the seasonal freezing level (altitude, where surface air temperature is 0°C) has risen by about 200 m per degree of warming from approximately 600 m in the 1960s to approximately 900 m in the 1990s (14). If warming in winter continues as expected, the freezing level will further rise by about 180 m until 2050 in case of moderate warming (+0.9°C), by about 360 m in case of medium warming (+1.8°C), and by about 680 m in case of strong warming (+3.4°C) (15). The freezing level roughly corresponds to the height of the snow line (the lower limit of the snow cap). The zone of warm permafrost (mean annual rock temperature approximately -2 to 0°C), which is more susceptible to slope failures than cold permafrost, may rise in elevation a few hundred meters during the next 100 years (18). This in turn may shift the zone of enhanced instability and landslide initiation toward higher-elevation slopes that in many regions are steeper, and therefore predisposed to failure.

Natural hazards in the Alpine countries have resulted in economic losses of EUR 57 billion over the 1982-2005 period (insured losses EUR 10,5 billion). This is without counting the large investments made by Alpine countries in protection and prevention measures (9).

Avalanches have claimed an average of 100 victims per year in the Alps over the last 30 years (11). Victims are primarily skiers. There is no clear trend in the frequency of avalanches (9). A change in avalanche hazards in connection with climate change is uncertain. In general, it is assumed that the possible change would follow the snow cover evolution. A decrease in avalanche hazards is likely at low and medium altitudes. Yet, heavy precipitation events might counterbalance this trend by triggering general avalanche situations (17).

Landslides and mudflows are expected to increase due to more intense precipitations during summertime. On the other hand, the possible future decrease of total summer precipitation may have a positive effect by reducing the deep and shallow landslides activity (17). Frequency of rock falls is also expected to increase due to changes in the spring thawing process (9,13).

The projected glacier retreat in the 21st century may form new potentially unstable lakes. Probable sites of new lakes have been identified for some alpine glaciers (19). Rock slope and moraine failures may trigger damaging surge waves and outburst floods from these lakes. In the short-term, increased summer floods are expected from glacier melt. In the long-term, reduced summer river flows are expected (9).

IPCC conclusions in 2012

In 2012 the IPCC concluded that there is high confidence that changes in heat waves, glacial retreat, and/or permafrost degradation will affect high mountain phenomena such as slope instabilities, mass movements, and glacial lake outburst floods, and medium confidence that temperature-related changes will influence bedrock stability. There is also high confidence that changes in heavy precipitation will affect landslides in some regions (20). There has been an apparent increase in large rock slides during the past two decades, and especially during the first years of the 21st century in the European Alps (21) in combination with temperature increases, glacier shrinkage, and permafrost degradation.

There is medium confidence that high-mountain debris flows will begin earlier in the year because of earlier snowmelt, and that continued mountain permafrost degradation and glacier retreat will further decrease the stability of rock slopes. There is  low confidence regarding future locations and timing of large rock avalanches, as these depend on local geological conditions and other non-climatic factors (20). Research has not yet provided any clear indication of a change in the frequency of debris flows due to recent deglaciation. In the French Alps, for instance, no significant change in debris flow frequency has been observed since the 1950s in terrain above elevations of 2,200 m (22). Processes not, or not directly, driven by climate, such as sediment yield, can also be important for changes in the magnitude or frequency of alpine debris flows (23).

IPCC conclusions in 2019

Rock fall

The IPCC concluded in 2019 that there is high confidence that the frequency of rocks detaching and falling from steep slopes (rock fall) has increased within zones of degrading permafrost over the past half-century, for instance in high mountains in Europe (42). Available field evidence agrees with theoretical considerations and calculations that permafrost thaw increases the likelihood of rock fall (and also rock avalanches, which have larger volumes compared to rock falls) (43). Summer heat waves have in recent years triggered rock instability with delays of only a few days or weeks in the European Alps (44). 

Snow avalanches

In the European Alps, avalanche numbers and runout distance have decreased with decreasing snow depth and increasing air temperature (45). In the European Alps and Tatras mountains, over past decades, there has been a decrease in avalanche mass and run-out distance, a decrease of avalanches with a powder part since the 1980s, a decrease of avalanche numbers below 2000 m, and an increase above (46).

Future projections mostly indicate an overall decrease in snow depth and snow cover duration at lower elevation, but the probability of occurrence of occasionally large snow precipitation events is projected to remain possible throughout most of the 21st century (42). An overall 20 and 30% decrease of natural avalanche activity in the French Alps is estimated for the mid and end of the 21st century, respectively, under a moderate (A1B) scenario of climate change, compared to the reference period 1960 – 1990 (47). The overall number and runout distance of snow avalanches is projected to decrease in regions and elevations experiencing significant reduction in snow cover (48)

Avalanches involving wet snow are projected to occur more frequently during the winter at all elevations due to surface melt or rain-on-snow (47, for the French Alps).

In summary, there is medium evidence andhigh agreement that observed changes in avalanches in mountain regions will be exacerbated in the future, with generally a decrease in hazard at lower elevation, and mixed changes at higher elevation (increase in avalanches involving wet snow, no clear direction of trend for overall avalanche activity) (42).

Adaptation strategies

Despite the clear climate change signals, only very few local examples exist where concrete measures have been implemented (9). An example is the town of Pontresina in the southeast of Switzerland (1847 inhabitants).

Pontresina is a pioneer in responding to climate change. Located at the foot of the Schafberg Mountain, famous for avalanches, the village has a long history of dealing with natural hazards. The town was originally built in two parts: the central part served as a channel for avalanches. But the expansion of the town led to the development of the central part of the city, thus increasing the exposure to avalanche threats (9).

The Swiss resort of Pontresina sits right below a mass of warming permafrost. When the permafrost melts in the debris-covered areas, at first moment nothing happens, but strong rainfalls increase the danger of debris flows. Flooding and rock falls have drawn Switzerland's attention about the natural hazards the country faces as a result of global warming. Pontresina has taken a proactive approach to protect itself against the effects of climate change. Four years ago a dam was built. The project was expensive and no one knows if it will stand if it ever sees a landslide, but is regarded as an insurance. The dam is estimated to stop 100,000 cubic meters of stone or 250,000 cubic meters of snow (10).

Integrated cryospheric observation and modelling approaches of glaciers, permafrost and related impacts are needed. Such work is greatly facilitated by new earth observation and geoinformatics technologies. Interdisciplinary collaboration between modelling and earth observation experts, field-oriented scientists, and practitioners is best suited to ensure a sound response to new requirements for the monitoring and modelling of mountain glaciers and permafrost, and related hazards (12).

Varied species composition and sustainable use increase the resistance and stability of natural ecosystems, and best ensure human living space. Climate change can be influenced only slowly. However, we can change the way we use our living space more quickly. In so doing, we can also much more rapidly achieve a sustainable effect in order to maintain the protective functions of ecosystems (16).

Adaptation strategies - AdaptAlp

According to AdaptAlp, a project of the six Alpine countries on natural hazards in the Alpine region, the ten most significant actions required at this time to prepare for the risks caused by global warming in the Alps are (25):

  • Improve public preparedness and personal responsibility by encouraging participation in emergency planning. To properly inform the public, risk management plans must address both emergency preparedness and early warning systems.
  • Incorporate climate change adaptation into spatial planning. A few examples to create a sustainable regional development that is less vulnerable to natural hazards are: financial incentives, establishing hazard zones, setting appropriate construction standards of buildings and infrastructure in risk areas, keeping endangered spaces free of development, and performing hazard assessments through the use of hazard mapping.
  • Involve local stakeholders in a risk dialogue. The dialogue includes meetings between important stakeholders, such as land and real estate owners, as well as those responsible for infrastructure and the public sector.
  • Encourage cross-border networking on integrated risk management.
  • Encourage a ‘common language’ and harmonised procedures when developing and using hazard maps.
  • Increase the size of flood plains, floodwater conduits and basins. Governments need to consider multiple uses of the same land and consider strict legal binding instruments that ensure a priority for flood retention areas is given.
  • Think of flood risk management in terms of an entire river basin to find solutions that are sustainable. Horizontal and vertical cooperation between all levels of government and the private sector are essential.
  • When planning for natural hazard risks consider all the environmental risks within a defined area. Natural hazards—floods, droughts, landslides—generate risks that are interrelated and so should be addressed jointly.
  • Use risk-management tools to explore the social and economic consequences of various adaptation measures. Risk planning tools allow for the integration of a wide range of strategies that reduce the risks of natural hazards, including spatial planning instruments, technical protection structures, specific protection measures for individual buildings and early-warning systems.
  • Support the collection and interpretation of local climate change data.

References

The references below are cited in full in a separate map 'References'. Please click here if you are looking for the full references for Switzerland.

  1. Gruber et al. (2004)
  2. Martin et al. (2001); Haeberli and Burn (2002), both in: European Environment Agency (EEA) (2005)
  3. Beniston (2004); UBA (2004), both in: European Environment Agency (EEA) (2005)
  4. UNEP (2004)
  5. Harris et al.(2003), in: Gruber et al. (2004)
  6. Haeberli et al. (1997), in: Gruber et al. (2004)
  7. Davies et al.(2001), in: Gruber et al. (2004)
  8. Haeberli and Beniston (1998); Beniston et al.(1997); Diaz and Bradley(1997); Barry(1992, 1990), all in: Gruber et al. (2004)
  9. Agrawala (2007)
  10. Harris, E., Swiss Town Guards Itself Against Climate Hazard”, August 27, 2007, http://www.npr.org/climateconnections, accessed on September 6, 2007.
  11. European Environment Agency (EEA) (2003)
  12. Kääb (2007)
  13. Federal Office for the Environment FOEN (Ed.) (2009)
  14. Scherrer and Appenzeller (2006), in: Federal Office for the Environment FOEN (Ed.) (2009)
  15. OcCC (2007), in: Federal Office for the Environment FOEN (Ed.) (2009)
  16. OcCC/ProClim- (2007)
  17. ESFR ClimChAlp (2008b), in: Castellari (2009)
  18. Noetzli and Gruber (2009), in: IPCC (2012)
  19. Frey et al. (2010), in: IPCC (2012)
  20. IPCC (2012)
  21. Ravanel and Deline (2011), in: IPCC (2012)
  22. Jomelli et al. (2004), in: IPCC (2012)
  23. Lugon and Stoffel (2010), in: IPCC (2012)
  24. Hilker et al. (2009), in: IPCC (2012)
  25. AdaptAlp
  26. Stoffel et al. (2014)
  27. Schneuwly-Bollschweiler and Stoffel (2012), in: Stoffel et al. (2014)
  28. Wood et al. (2016)
  29. Turkington et al. (2016)
  30. Schneuwly-Bollschweiler and Stoffel (2012); Stoffel et al. (2014); Van den Heuvel et al. (2016), all in: Turkington et al. (2016)
  31. Winter et al. (2010), in: Turkington et al. (2016)
  32. Jomelli et al. (2009), in: Turkington et al. (2016)
  33. Stoffel et al. (2014), in: Turkington et al. (2016)
  34. Melchiorre and Frattini (2012), in: Turkington et al. (2016)
  35. Micheletti and Lane (2016)
  36. Huss et al. (2008); Farinotti et al. (2012), both in: Micheletti and Lane (2016)
  37. Farinotti et al. (2012), in: Micheletti and Lane (2016)
  38. Kos et al. (2016)
  39. McColl (2012), in: Kos et al. (2016)
  40. Oppikofer et al. (2008), in: Kos et al. (2016)
  41. Deline et al. (2015), in: Kos et al. (2016)
  42. IPCC (2019)
  43. Gruber and Haeberli (2007); Krautblatter et al. (2013), both in: IPCC (2019)
  44. Allen and Huggel (2013); Ravanel et al. (2017), both in: IPCC (2019)
  45. Teich et al. (2012); Eckert et al. (2013), both in: IPCC (2019)
  46. Eckert et al. (2013); Lavigne et al. (2015); Gadek et al. (2017), all in: IPCC (2019)
  47. Castebrunet et al. (2014), in: IPCC (2019)
  48. Mock et al. (2017), in: IPCC (2019)
  49. Hendrickx et al. (2022)
  50. Stoffel et al. (2024)

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