Mountain Permafrost

What is Permafrost?

Permafrost is an important widespread thermal phenomenon in the subsurface of cold polar and high-mountain regions. Permafrost is defined as ground material that remains at or below 0 °C throughout the year. Mountain permafrost occurs in high mountain areas. 

Permafrost is found in all types of ground materials (rock, sediments or soil) and can contain varying quantities of ice (0–100%) and organic material (0–100%). In the Swiss Alps, permafrost is found hidden in scree and bedrock slopes above the treeline. Massive ice lenses of several metres' thickness can exist in loose sediments within scree slopes and rock glaciers. In steep bedrock slopes, ground ice is restricted to rock pores and clefts. Organic material is very limited in mountain permafrost since it is generally above the areas where abundant vegetation can grow.

The occurrence of permafrost depends on the temperature at the ground surface, which is determined by the local climatic conditions (i.e. the surface energy balance). The uppermost layer of the ground thaws during summer and is called the active layer. Below its lower boundary – the permafrost table – the actual permafrost body starts, which reaches down to the permafrost base. 

The thickness of the permafrost body in the Swiss Alps ranges from a few decametres at the lower limit of permafrost occurrence to several hundreds of metres below the highest mountain peaks. In the coldest polar regions, the depth of permafrost can extend as far as 1.7 km.



The most important factor controlling the occurrence and evolution of permafrost is the ground surface temperature (GST). The GST results from the energy balance at the ground surface, which mainly depends on the air temperature and solar radiation during the snow-free season as well as the amount and duration of the winter snow cover. The GST controls the amount of energy transferred into the ground and thus the temperature of the permafrost. For permafrost studies, typically the mean annual ground surface temperature (MAGST) is calculated. In complex mountain topography, MAGST can vary considerably over short distances leading to a high spatial variability of the permafrost distribution. For example, the difference in MAGST between steep south and north faces at the same elevation can be as high as 8 °C. Fine scale variations can be a few degrees Celsius over a few metres in homogeneous terrain. 

Permafrost is overlain by a layer that thaws each summer and freezes again in winter – the active layer. The thickness of this layer, the active layer thickness (ALT) typically reaches 15–100 centimeters in continuous polar permafrost and several meters in warmer mountain permafrost. The ALT varies from year to year and reflects the short-term climate fluctuations such as winter snow conditions, intensity of the summer warming and winter cooling. Inter-annual variations are smaller for ice-rich permafrost than for bedrock slopes with low ground ice content.

Temperature fluctuations in the ground are greatest close to the surface and become smaller and temporally delayed with increasing depth. For example, temperature variations arrive with a delay of around half a year at about 10 m depth and only seasonal variations over several months can be seen. From a given depth, also seasonal fluctuations are no longer observed and temperature changes reflect long-term climatic changes. This is the so-called depth of zero annual amplitude (ZAA). Here, intra-annual temperature variations are smaller than 0.1 °C. In the Swiss Alps, the ZAA is typically around 15–20 m depth. 


Permafrost is relevant! It is a good climate indicator and below 0°C temperatures as well as ice containted in the ground change its geotechnical properties. Find out more:

In the Swiss Alps, the permafrost conditions and their changes are not only relevant as a climate indicator but also for mountain ecosystems as well as for the management of mountain areas in terms of natural hazards, infrastructure and land use in general. Warming or melting of the permafrost ice in the ground or in fissures of rock faces can decrease the stability of steep mountain slopes, eventually resulting in an increase in rock fall and debris flow activities.

Debris flow initiated at the front of the Ritigraben rock glacier (top, SLF Camera) that landed on the cantonal road down in the Mattervalley (bottom).

In the Swiss Alps, infrastructures at higher elevation such as mountain huts, avalanche protection structures, or cable cars are often built on permafrost. Construction in permafrost regions has to consider the special characteristics of permanently frozen ground. Increasing active layer thickness, permafrost warming or increasing slope deformation can further cause stress on the structures resulting in increased maintenance costs or a shorter service life.

In polar regions, permafrost relevance and the impacts of its warming are somewhat different. Here, people are living on the permafrost and have been using it for generations to store food. Due to the ongoing permafrost warming and thaw, buildings, roads, pipelines built on permafrost may deform and become instable. Unlike in mid-latitude mountain regions, vegetation grows in the Arctic tundra regions above the permafrost. Permafrost thaw in these large permafrost regions enables carbon and methane previously stored within the permafrost to be released into the atmosphere. Both components are important greenhouse gases with the potential to increase the ongoing climate warming.


The short webvideo by SRF Kultur below illustrates and summarizes what mountain permafrost is, where it can be found and why it is important to us:


In the Swiss Alps, all observations from PERMOS show a consistent trend of continued permafrost warming and degradation in the past two decades. Permafrost temperatures below the depth of the ZAA have significantly increased, active layer thicknesses have deepened and geophysical measurements indicate an overall decrease of the ground ice content.

If you are interested to read and browse more on permafrost in mountain areas – as well as on permafrost in polar areas – we compiled a number of links and publications.


Permafrost is found in polar and high-mountain environments. It iunderlies approximately 20% of the land area of the northern hemisphere and about 3–5% of the area of Switzerland.

Permafrost is found in all polar and high mountain regions of the world and is most abundant on the Northern Hemisphere in the Arctic and High Arctic of Canada and Russia. In the coldest regions, continuous permafrost is found (i.e. 90 to 100% of the area is affected), whereas in warmer or mountain regions the permafrost occurrence is discontinuous (50–90%) or sporadic (0–50%).

In Switzerland, permafrost is mostly sporadic or discontinuous and is estimated to underly 3–5% of the country. The majority of permafrost is located above 2600 m asl. with temperatures between –3 and 0 °C. As a thermal subsurface phenomenon, permafrost is mostly invisible in the landscape.

Several typical environments and landforms, however, can help to detect the presence of permafrost. Most commonly, permafrost is found in talus or debris slopes, moraines, rock walls and fractured bedrock environments. The most prominent indicator of mountain permafrost is a rock glacier. Rock glaciers are geomorphological landforms composed of a mixture of ice, debris and rocks, which move downslope under the effect of permafrost creep and build strinking tongue-shaped landforms. Rock glaciers are not actually glaciers.


Permafrost distribution can be estimated based on modelling studies. It is important to note that permafrost maps show the potential distribution of the subsurface phenomenon and provide a probability, index or alike about  its occurrence at a location. However, in-situ measurements are needed for a definitive assessment of permafrost in the subsurface. We provide you with the links to two frequently used maps of the potential permafrost distribution in Switzerland.

The map by the Federal Office for the Environment (FOEN) from the year 2005 is based on the rules of thumb for permafrost distribution in Switzerland developed in the 1970ies. Details about the map can be found on the website of the FOEN. The direct link to browse the map is:

Potential permafrost distribution (BAFU)

The SLF map produced in 2019 distinguishes between bedrock permafrost and ice-rich permafrost in loose sediments below. A description of the map is provided on the website of the SLF or in the corresponding scientific publication. It can also be browsed in 3D on The direct link to browse the map is:



As permafrost is not visible and is hidden below the ground surface, observations rely on field measurements.

Permafrost responds to changes in climate with a high degree of sensitivity. It is therefore considered an Essential Climate Variable (ECVs) by the Global Climate Observing System (GCOS). ECVs are a defined set of variables required for the observation of the Earth’s climate change. 

The assessment of the long-term changes of permafrost requires reliable and comparable data measured at representative sites over decades. Such data also provide a basis for research, decision makers and society to improve the understanding of permafrost processes, to assess impacts of changing permafrost on infrastructure, natural hazards and ecosystems, or to validate and calibrate models.

As permafrost is a thermal subsurface phenomenon, it’s observation primarily relies on field data. The PERMOS monitoring setup includes a set of variables that complement each other for a comprehensive picture of state and changes of mountain permafrost in the Swiss Alps. We measure ground temperatures at the surface and at depth in boreholes, meteorological variables, changes in ground ice content and rock glacier creep velocities. 


The measurement of ground temperatures in boreholes – called permafrost temperatures – is the basis of permafrost monitoring because it is the only direct observation method. Permafrost temperatures are measured at 15 sites in 30 boreholes of 20 to 100 m depth. A logger continuously records temperatures at multiple depths with a temperature sensor string installed in the borehole. Ground temperatures measured at multiple depths also allow to determine the annual active layer thickness (ALT) by linear interpolation between neighbouring temperature sensors. We compiled our best practices for borehole temperature measurements in mountain permafrost in a methods paper in 2021

Spatially distributed ground surface temperature (GST) measurements complement the point information obtained from the boreholes. We installed 10–20 loggers at 22 of our sites. GST measurements allow to capture the influence of topography and surface cover. 

Photo: Christophe Lambiel.

Electrical Resistivity Tomography (ERT) measurements allow the detection of changes in liquid water and ground ice content within the permafrost body. This complementary information is particularly important for ice-bearing permafrost because temperature changes are significantly reduced by latent heat uptake during ground ice melt. ERT measurements are performed annually along five fixed installed profiles close to boreholes.

Photo: Christophe Lambiel.

Changes in the downslope movement of permafrost landforms such as rock glaciers are important in view of slope stability and sediment transfer. They also provide indirect information on the thermal state of permafrost within the landform. Rock glacier velocity (RGV) was included in 2021 as a product of the ECV permafrost. RGV monitoring is performed on 18 rock glaciers by annual terrestrial geodetic surveys (TGS), which are complemented by continuous GNSS recordings at 8 sites to capture the intra-annual variations.

Photo: Cristian Scapozza.

Meteorological data measured directly at the borehole sites are crucial to interpret the permafrost evolution, which is mainly driven by changes in the surface energy balance. The complex topography introduces high uncertainties when extrapolating data from operational weather stations. Automatic weather stations (AWS) including full radiation balance measurements at 6 borehole sites are part of the network. 

Photo: Andi Hasler.

Rock fall events originating from permafrost slopes are documented based on observations received from various sources (e.g., mountain guides, climbers, hazard managers or seismic signals detected by the Swiss Seismological Service). 
To collect as many data as possible, you can help! Please report your observations via the questionnaire of the SLF or the MountaiNow App!

Photo: Robert Kenner.


The monitoring strategy of PERMOS is continuously adapted, based on new findings from research. We also work on the documentation of our approach and collaborate with global permafrost monitoring strategies and recommendations. Some information is linked below:


Browse through a collection of photos illustrating permafrost in mountain regions and the measurements performed in the framework of the PERMOS Network.

The pictures in the gallery can be downloaded and used according to the CC BY NC SA 4.0 license. For all other use of the photos, the PERMOS Office or the photographer have to be contacted. The name of the photographer and a description of the photos can be found in the gallery.