Mountain permafrost distribution in Dovrefjell and Jotunheimen, southern Norway, based on BTS and DC resistivity tomography data

Isaksen, Ketil; Hauck, Christian; Gudevang, Espen; Ødegârd, Rune Strand; Sollid, Johan Ludvig

doi:10.1080/002919502760056459

Cited by 115 publications

(152 citation statements)

References 33 publications

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“…A similar pattern would be expected for regions such as the European Alps (e.g. Gruber and Hoelzle, 2001) and the mountains of southern Norway (Isaksen et al, 2002). Areas that display SUSL in the regional model include the intensive study site of Haines Summit as well as the majority of the ESW where the largest 942 P. P. Bonnaventure and A. G. Lewkowicz: Impacts of mean annual air temperature glaciated areas, the highest mountains and the most annual precipitation all occur (Figs.…”

Section: Loss Morphology Typesmentioning

confidence: 76%

Impacts of mean annual air temperature change on a regional permafrost probability model for the southern Yukon and northern British Columbia, Canada

Bonnaventure

Lewkowicz

2013

The Cryosphere

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Abstract. Air temperature changes were applied to a regional model of permafrost probability under equilibrium conditions for an area of nearly 0.5 × 10 6 km 2 in the southern Yukon and northwestern British Columbia, Canada. Associated environmental changes, including snow cover and vegetation, were not considered in the modelling. Permafrost extent increases from 58 % of the area (present day: 1971-2000) to 76 % under a −1 K cooling scenario, whereas warming scenarios decrease the percentage of permafrost area exponentially to 38 % (+ 1 K), 24 % (+ 2 K), 17% (+ 3 K), 12 % (+ 4 K) and 9 % (+ 5 K) of the area. The morphology of permafrost gain/loss under these scenarios is controlled by the surface lapse rate (SLR, i.e. air temperature elevation gradient), which varies across the region below treeline. Areas that are maritime exhibit SLRs characteristically similar above and below treeline resulting in low probabilities of permafrost in valley bottoms. When warming scenarios are applied, a loss front moves to upper elevations (simple unidirectional spatial loss). Areas where SLRs are gently negative below treeline and normal above treeline exhibit a loss front moving up-mountain at different rates according to two separate SLRs (complex unidirectional spatial loss). Areas that display high continentally exhibit bidirectional spatial loss in which the loss front moves up-mountain above treeline and down-mountain below treeline. The parts of the region most affected by changes in MAAT (mean annual air temperature) have SLRs close to 0 K km −1 and extensive discontinuous permafrost, whereas the least sensitive in terms of areal loss are sites above the treeline where permafrost presence is strongly elevation dependent.

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Section: Loss Morphology Typesmentioning

confidence: 76%

Impacts of mean annual air temperature change on a regional permafrost probability model for the southern Yukon and northern British Columbia, Canada

Bonnaventure

Lewkowicz

2013

The Cryosphere

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“…visible in the data published in Isaksen et al, 2002) and Iceland Farbrot et al, 2007). Furthermore, they are documented from Alaska, Arctic Canada (Grenfell and Putkonen, 2008) and the western-and easternmost parts of Siberia, e.g.…”

Section: Introductionmentioning

confidence: 79%

Modeling the impact of wintertime rain events on the thermal regime of permafrost

et al. 2011

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Abstract. In this study, we present field measurements and numerical process modeling from western Svalbard showing that the ground surface temperature below the snow is impacted by strong wintertime rain events. During such events, rain water percolates to the bottom of the snow pack, where it freezes and releases latent heat. In the winter season 2005/2006, on the order of 20 to 50 % of the wintertime precipitation fell as rain, thus confining the surface temperature to close to 0 • C for several weeks. The measured average ground surface temperature during the snow-covered period is −0.6 • C, despite of a snow surface temperature of on average −8.5 • C. For the considered period, the temperature threshold below which permafrost is sustainable on long timescales is exceeded. We present a simplified model of rain water infiltration in the snow coupled to a transient permafrost model. While small amounts of rain have only minor impact on the ground surface temperature, strong rain events have a long-lasting impact. We show that consecutively applying the conditions encountered in the winter season 2005/2006 results in the formation of an unfrozen zone in the soil after three to five years, depending on the prescribed soil properties. If water infiltration in the snow is disabled in the model, more time is required for the permafrost to reach a similar state of degradation.

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“…for the two periods 1982-1986 and 2008-2010 were −2.2 • C (Ødegård et al, 1992) and −1.6 • C (Farbrot et al, 2011), respectively. At the top of Juvvasshøe, data from a 129 m deep borehole (Sollid et al, 2000) show a very low geothermal gradient and indicate permafrost extending below a depth of 300 m (Isaksen et al, 2001(Isaksen et al, , 2007 and a close relation of permafrost, ground surface and air temperatures (Isaksen et al, 2003). An altitudinal transect of shallow boreholes (10 m deep) was established in 2008 (Farbrot et al, 2011;Hipp et al, 2012).…”

Section: Study Areasmentioning

confidence: 99%

A statistical approach to represent small-scale variability of permafrost temperatures due to snow cover

et al. 2014

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Abstract. In permafrost environments exposed to strong winds, drifting snow can create a small-scale pattern of strongly variable snow heights, which has profound implications for the thermal regime of the ground. Arrays of 26 to more than 100 temperature loggers were installed to record the distribution of ground surface temperatures within three study areas across a climatic gradient from continuous to sporadic permafrost in Norway. A variability of the mean annual ground surface temperature of up to 6 • C was documented within areas of 0.5 km 2 . The observed variation can, to a large degree, be explained by variation in snow height. Permafrost models, employing averages of snow height for grid cells of, e.g., 1 km 2 , are not capable of representing such sub-grid variability. We propose a statistical representation of the sub-grid variability of ground surface temperatures and demonstrate that a simple equilibrium permafrost model can reproduce the temperature distribution within a grid cell based on the distribution of snow heights.

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Mountain permafrost distribution in Dovrefjell and Jotunheimen, southern Norway, based on BTS and DC resistivity tomography data

Cited by 115 publications

References 33 publications

Impacts of mean annual air temperature change on a regional permafrost probability model for the southern Yukon and northern British Columbia, Canada

Impacts of mean annual air temperature change on a regional permafrost probability model for the southern Yukon and northern British Columbia, Canada

Modeling the impact of wintertime rain events on the thermal regime of permafrost

A statistical approach to represent small-scale variability of permafrost temperatures due to snow cover

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