Multiple Effects of Changes in Arctic Snow Cover
Snow cover plays a major role in the climate, hydrological and ecological systems of the Arctic and other regions through its influence on the surface energy balance (e.g. reflectivity), water balance (e.g. water storage and release), thermal regimes (e.g. insulation), vegetation and trace gas fluxes. Feedbacks to the climate system have global consequences. The livelihoods and well-being of Arctic residents and many services for the wider population depend on snow conditions so changes have important consequences. Already, changing snow conditions, particularly reduced summer soil moisture, winter thaw events and rain-on-snow conditions have negatively affected commercial forestry, reindeer herding, some wild animal populations and vegetation. Reductions in snow cover are also adversely impacting indigenous peoples’ access to traditional foods with negative impacts on human health and well-being. However, there are likely to be some benefits from a changing Arctic snow regime such as more even run-off from melting snow that favours hydropower operations.
KeywordsSnow Arctic Climate Albedo Hydrology Ecology Biogeochemical cycling Geochemical processes Forestry Infrastructure Tourism Indigenous cultures Human health
Snow is a dominant feature of the Arctic covering its land, sea, lake and river ice surfaces for 8–10 months each year. Arctic climate has entered a unique period relative to the instrumental record and, in the case of summer temperatures, relative to 2000-year reconstructions of past variations: this trend is expected to continue (Walsh et al. 2011a, b [this issue]). Analysis of in situ and satellite data show evidence of different regional snow cover responses to this warming and increasing winter precipitation over the past 40–50 years. Snow cover over the Arctic is projected to increase in the range of 0–15% for maximum snow water equivalent (SWE) but decreases in snow cover duration (SCD) by about 10–20% are projected over much of the Arctic (Callaghan et al. 2011a, b [this issue] and references therein).
The purpose of this article is to summarize key findings from the SWIPA (Snow, Water, Ice, Permafrost in the Arctic) Assessment (AMAP 2011) related to the impacts of changing snow cover in the Arctic. Part I of the summary focusing on observed snow cover changes, was presented in Callaghan et al. (2011b [this issue]); in this article, we focus specifically on the various impacts of recently observed and projected changes in Arctic snow conditions on the climate system, hydrology, ecology, biogeochemical cycling and socio-economics.
The Surface Energy Budget
Snow cover has a number of important physical properties that exert an influence on climate or moderate its effects. It has high short-wave albedo, high thermal emissivity, low heat conductivity, large latent heat of fusion and low surface roughness whilst it stores and then rapidly releases water in the melt season. The combination of high albedo (as high as 0.8–0.9 for dry snow) and low thermal conductivity promotes low surface temperatures and low-level temperature inversions (On-line Supplementary Material A). The low thermal conductivity of snow allows it to insulate the surface from large energy losses in winter, and this has major implications for the energy and moisture fluxes in the near-surface layers. Consequently, the insulating effect has a strong impact on ice growth rates and ice thickness and on the development of seasonally frozen ground and permafrost. The surface energy exchanges are further modified by the low aerodynamic roughness of snow cover, which can reduce turbulence and, hence, vertical transfer of energy.
The insulating properties of snow affect both the surface and the near-surface temperature regime. Soil surface temperature in mid-winter under 50 cm of snow may be around zero, whilst the air temperature above the snowpack is as low as −20°C (Pomeroy and Brun 2001). The insulating role of snow prevents deep freezing of near-surface ground, which has important implications for the active layer and for permafrost (see Callaghan et al. 2011c), as well as for the runoff response in spring and for ecological and biogeochemical processes (see below). In the permafrost areas of the Arctic, variations in snow cover depth (rather than surface air temperature) are a major factor controlling temperature variability in the upper 3 m of soil. For example, Bulygina et al. (2007, 2009, 2011) observed soil warming trends at some locations where air temperatures were cooling due to increases in winter snow depths.
Changes in snow cover over the Arctic region, particularly in spring, have a strong impact on regional energy budgets owing to the large amount of incoming solar energy reaching the snow surface (e.g. Déry and Brown 2007). Euskirchen et al. (2007) estimated that a pan-Arctic reduction in snow cover of 0.22 day year−1 over the 1970–2000 period of warming contributed an additional 0.8 W m−2 per decade of energy. Their simulation also showed evidence of regional asymmetry in Arctic snow-albedo feedback with stronger heating contributions over the North American sector from loss of snow cover. Fernandes et al. (2009) highlighted the importance of snow metamorphism (or ageing) in the albedo feedback with their satellite-based analysis showing that snow metamorphism was as important as loss of snow cover in determining the total terrestrial snow-albedo feedback over Eurasia.
The Atmospheric Moisture Budget
The atmospheric moisture budget is changing and will continue to evolve in response to a warming climate, changes in sea ice and snow cover and altered atmospheric circulation (Rawlins et al. 2010). Increased winter snowfall over land areas may keep soil moisture levels higher in spring, working with increased precipitation to promote more evaporation. On the other hand, under a warming climate, earlier loss of the snow cover over Arctic and sub-Arctic lands, by exposing the dark underlying surface, will promote surface heating, and hence, an earlier transition to the summer-type convective precipitation regime over Arctic and sub-Arctic lands (Groisman et al. 1994b). A warmer Arctic atmosphere also provides more energy for sublimation. King et al. (2008) estimated Arctic blowing snow sublimation losses to be ~20% of annual snowfall.
A number of studies have shown that large-scale snow cover anomalies can play a significant role in global scale atmospheric circulations that act over timescales of seasons to years (Groisman et al. 1994a: Gong et al. 2004; Fletcher et al. 2009a, b). For example, there is evidence both from models (e.g. Walland and Simmonds 1997) and observations (Clark and Serreze 2000) that variability in Eurasian snow cover extent modulates atmospheric circulation patterns over the North Pacific Ocean.
Simulations from most coupled GCMs point to intensification of the northern high-latitude freshwater cycle through the twenty-first century (e.g. Holland et al. 2006; Kattsov et al. 2007). A warmer atmosphere carries more water vapour and with efficient precipitation-generating mechanisms (convergence and uplift), precipitation increases. The regional and seasonal variability in sources of moisture for precipitation are described in On-line Supplementary Material B. Whilst evaporation also increases, the precipitation change dominates such that there is an increase in net precipitation and hence river discharge.
The Role of Snow Cover in the Seasonal Hydrological Cycle and Expected Changes
Snow cover has a direct impact on the hydrological cycle in its redistribution of water between cold and warm seasons, with limited water availability during the cold season and an abundance of water during snowmelt. The snow-generated runoff in the Arctic drainage basin is up to 75% of total annual flow in some northern regions of Siberia and North America (Woo 1980). The indirect snow cover impact has its effects on the surface energy budget. That is, on the latent heat flux to the atmosphere (suppressed by low surface temperatures associated with snow cover and the absence of transpiration) and to the soil (by intercepting precipitation and meltwater and sending a significant part downstream during the snowmelt period instead of contributing to the base flow; Dingman 2002). Therefore, future variations in snow accumulation may dramatically change the hydrological regime of the Arctic (Adam et al. 2009) but there will be regional variations (On-line Supplementary Material B).
Changes in streamflow will be expressed mostly through the high and low flows. At present, spring floods usually represent the highest flow of the year, generated by rapid melting of the snowpack. A shortened snow accumulation season interrupted by mid-winter melt events will diminish the water supply and moderate its rate of delivery. Streamflow data from northern Canada show that there are detectable trends towards an earlier and decreased spring freshet (the peak spring runoff from snowmelt) (Aziz and Burn 2006).
Snow is currently the principal promoter of river flow, but in the future the number and magnitude of rainfall events may increase, whilst the contribution of snow may decline, notably in the sub-Arctic. Small basins with polar desert conditions may find a total cessation of their summer flow except during heavy rains. The seasonal flow pattern may then be replaced by a pluvial or a nivo-pluvial regime.
Reduced snow accumulation, earlier snow melt and increased evaporation (and sublimation) have consequences for seasonal and longer term storage of water and ice. Many late-lying and semi-permanent snowbanks will shrink or disappear from the Arctic landscape. Snow storage on glaciers will change with negative consequences for their mass balance (Sharp et al. 2011). The loss of snowbeds will lead to the demise of many patchy wetlands and the deterioration of others in the Arctic that depend on the late-lying snow to sustain wetland saturation (e.g. Woo and Guan 2006). However, thawing permafrost and associated thermokarst could provide a new source of water. The critically important balance between the two processes is unknown, and areas of drying tundra as well as of increased waterlogging are both being reported (AMAP 2011).
Ecological Processes and the Role of Snow Cover
Snow is probably one of the most important climatic drivers affecting Arctic biology and its environment (Callaghan et al. 2011a and references therein).
Interactions between snow and vegetation are complex. Whereas, vegetation has strong and complex influences on the accumulation and ablation of snow (Pomeroy et al. 2006), snow provides protection for vegetation from extreme low temperatures, large temperature fluctuations, ice crystal blast, desiccation and herbivory.
Vegetation affects the vertical profile of a snow cover. Snow falling onto shrubs and trees is partitioned into interception by the canopy and throughfall to the ground (Hedstrom and Pomeroy 1998). Snow can remain in a forest canopy for some time before being removed by direct unloading, drip of meltwater and sublimation (e.g. Molotch et al. 2007). Vegetation also reduces the horizontal redistribution of snow and can therefore have greater snow depths than open areas. Snow trapping depends on the height, density and distribution of vegetation, all of which are currently changing in some Arctic areas (e.g. Callaghan and Tweedie 2011).
Vegetation can increase or decrease snowmelt rates relative to open areas (e.g. Pomeroy et al. 2006). However, many processes are involved, and the net outcome in the context of vegetation changes is difficult to model (e.g. Bewley et al. 2007). Whereas vegetation can shade snow on the ground from solar radiation, it can also greatly increase the net thermal radiation absorbed by snow (Sicart et al. 2004). Moreover, sun-lit vegetation can have temperatures well in excess of the air and snow temperatures, further increasing the thermal radiation emitted to the snow (Pomeroy et al. 2009).
Snow, in turn, affects vegetation. There is a close relationship between snow distribution and vegetation type (Evans et al. 1989). Exposed areas typically have low-growing plants whose forms provide protection from wind abrasion and summer drought stress (Walker et al. 2001). Plants covered by snow in winter often have the capacity to burst bud quickly after snow melt to maximize their use of the short Arctic growing season (Walker et al. 2001). Changes in snow conditions (presented in Callaghan et al. 2011a, b [this issue]) will affect the future distribution of vegetation, biodiversity and productivity. Although remote sensing shows that the Arctic is generally greening (Bhatt et al. 2010), snow manipulation experiments suggest that responses of vegetation to earlier snowmelt timing may not always be an increase in productivity (Starr et al. 2008). However, in the longer term, when species with more southern distributions invade, the system is likely to become more productive (Sitch et al. 2008; Wolf et al. 2008).
Interactions between snow and animals are determined by the varying abilities of Arctic species to migrate (Forchhammer et al. 2008; Robinson et al. 2009). Whereas species resident in the Arctic (lemming, musk ox, stoat) and that migrate locally (fox, caribou/reindeer, ptarmigan) will experience varying snow conditions throughout the year, long-distance migrating species (waders, geese, gulls, skuas, terns) are influenced only by the conditions when they arrive at their Arctic breeding grounds in spring. A 10% decrease in snow cover, advances egg laying by the pink-footed goose (Anser brachyrhynchus) by 5–6 days, corresponding to a 20% increase in probability of nesting success (Madsen et al. 2007) but climate across the entire range of a species are pivotal in estimating effects taking place in the Arctic.
Changes in the micro-topical snow conditions may also influence the dynamics of northern rodents (Kausrud et al. 2008). The hardness of the snowpack is increasing (Johansson et al. 2011). This decreases the available subnivean space, causing a decline in rodent population growth rates. A collapse in rodent population size has cascading effects on predators such as the Tengmalm’s owl (Aegolius funereus) (Hörnfeldt et al. 2005) and their alternative prey, such as ground-nesting birds (Kausrud et al. 2008).
Ice crusts, ice layers and rain-on-snow events have been implicated in population crashes of reindeer on Svalbard (Aanes et al. 2000), the near extirpation of Peary’s caribou (Rangifer tarandus pearyi) in High Arctic Canada (Barry et al. 2007), population crashes in caribou on the Queen Elizabeth Islands, Canadian High Arctic (Miller and Barry 2009) and the deaths of 20 000 musk ox on Banks Island in October 2003 (Rennert et al. 2009). The Sámi (Moen 2008; Helle and Kojola 2008) and Nenets (e.g. Bartsch et al. 2010) have experienced the increasing frequency of extreme weather events and effects on reindeer mortality and calf production. Declining polar bear populations are also partly due to changing snow conditions as female polar bears make dens in snow to shelter and give birth to young during winter. Rains early in the breeding season can melt the under-snow lairs and increase cub mortality (Stirling and Smith 2004).
Future warming could be associated with events that cause sudden and dramatic step changes, rather than progressive trends, in both animal and plant biodiversity.
Interactions between snow and biogeochemical cycles
Winter respiration of CO2 is a significant portion of the annual carbon budget (e.g. Fahnestock et al. 1998). Snow acts as an insulator and increases ground temperature, which is one of the main drivers of winter respiration rates in the Arctic (Grogan and Jonasson 2006). Experimental increases of snow depth in High Arctic Canada (Nobrega and Grogan 2007) and sub-Arctic Sweden (Larsen et al. 2007) increased ecosystem respiration rates by 60% and 157% compared with control plots. Their results suggest that a moderate increase in snow depth can enhance winter respiration sufficiently to alter the ecosystem annual net carbon exchange from a sink to a source, resulting in a net release of CO2 to the atmosphere.
The depth of snow that affects hydrology at the onset of the growing season will have strong impacts on the degree of waterlogging and, hence, the potential emissions of other important greenhouse gases, such as methane (CH4) and nitrous oxide (N2O), in that emissions will increase with the extent of waterlogging. Also, the date of snow melt is important for the growing season accumulated uptake of carbon, as solar radiation input is high at this time compared with the period in autumn when the snowpack is formed. Euskirchen et al. (2006) estimated that for each day that the growing season increased across the pan-Arctic region over the period 2001–2100 the carbon drawdown increased by 9.5 g C m−2 year−1.
Geochemical Processes in the Snow Cover
The effects of heavy metals are many and varied depending on factors such as the particular metal, the organism and the mode of uptake (Dietz et al. 1998). Their greatest toxic impacts occur in animals at the higher trophic levels where bioaccumulation through the food chain can result in high concentrations. The few available data on heavy metal concentrations in snow on ice surfaces in the Russian Arctic seas (e.g. Golubeva 2007; Callaghan et al. 2011a, references therein) mostly show no evidence of pollution, except in areas near the large industrial centers of the Kola Peninsula (Monchegorsk, Nikel) and Siberia (Norilsk) and along the Northern Sea Route.
A significant reduction in on-ice snow volume has led to changes in the size of the storage reservoirs for contaminants such as heavy metals (especially mercury), as well as persistent organic pollutants, such as PCBs (polychlorinated biphenyls) and DDT (Kallenborn et al. 2011). Changes in the size of the storage reservoirs, and in the processes driving these changes, could increase the delivery of heavy metals to the tundra and coastal ecosystems through changes in dry deposition and wet deposition through rainfall and fog. At the same time, heavy metal accumulation in snow cover on drifting ice will decrease, resulting in a redistribution of heavy metal pollution (see On-line Supplementary Material D).
Socio-Economic Processes and the Role of Snow Cover
Water resources and hydropower will be affected by projected changes in snow cover and duration that will affect the capacity and operations of current and future hydroelectric developments and might resolve some of the rising energy needs (Furgal and Prowse 2008). In areas where winter precipitation is expected to increase (Callaghan et al. 2011a, 2011b [this issue]), an increase in runoff is expected (On-line Supplementary Material E), (Gode et al. 2007). Projected increases in winter rainfall, increased freeze–thaw cycles and increased glacier melt are expected to lead to an enhanced winter snow melt and a decline in winter storage and, hence, a more even runoff over the year (Gode et al. 2007; Furgal and Prowse 2008). This will reduce the need for peak reservoir levels without generating maximum electricity (Gode et al. 2007: On-line Supplementary Material E). Large variation between the results for two GCMs used to provide runoff projections provides a challenge for economic forecasting (On-line Supplementary Material E, Table E2), whilst changes in climate will alter the conditions for the power plants. For example, in some regions reservoir capacities may need to be expanded to offset changes in runoff, both for seasonal and total annual runoff. In addition, the construction of hydropower dams needs to take into account the different future projections for ice conditions (Prowse et al. 2011a, b [this issue]).
Transport in the Arctic often depends on snow conditions: snow is required for transport by Arctic residents, particularly Indigenous Peoples, during winter whereas it can be problematic for transport by rail, road and air. Rising temperatures in the Arctic, particularly decreases in very cold days, later onset of seasonal freezes and earlier onset of seasonal thaws projected for many Arctic areas, could mean reduced costs of snow and ice control, as is the case in the mid-latitudes with seasonal snow cover. A projected shortening of the snow cover season over most of the Arctic will decrease the operational period of winter road networks that are important for low cost re-supply of many northern communities in Canada (Furgal and Prowse 2008) and shorten the period that snowmobiles can be used for hunting and reindeer herding.
Forestry will be affected by changing snow conditions and evidence is already accumulating of detrimental impacts. Where precipitation in the boreal region is most abundant (eastern Canada, western Russia and Fennoscandia), an increase in temperature can often result in increased growth in healthy trees (Saxe et al. 2001) and a northward and upward extension in range as projected by many models (see Callaghan et al. 2011a, references therein). However, the moisture regime in much of the boreal region is only marginally suitable for forest growth and development. Consequently, reduced growth of boreal trees during warming was widespread over much of the past century in nearly all regions and tree species (see Callaghan et al. 2011a, references therein). Under warmer climatic conditions, the northern treeline would probably not advance uniformly into regions that were formerly too cold (as generally perceived), but would advance in a fragmented manner by occupying parts of the landscape with sufficient moisture, for example from snow accumulations.
New direct experimental results demonstrate that at least some boreal evergreen conifers largely grow by moisture supplied from winter snowpack melt (Yarie 2008). In most of the boreal forest region, temperature increases have made the snow accumulation season shorter, so that less of the annual water budget is introduced into the ground in the spring pulse of snowmelt. Broadleaf trees can use the variable summer rains more effectively than most conifers, so this change in the seasonal type of moisture (less snow, more rain) now favours the broadleaf trees over conifers (Juday 2009). Boreal broadleaf tree ecosystems are characterized by less storage of carbon than conifer-dominated forests and the coniferous trees are more widely used in the timber industry.
In contrast to the benefits of a deep snow cover by providing water, heavy snowfall causes damage to forests in Finland. A modelling assessment of risk projected that compared with the baseline period 1961–1990, the amount of damaging snowfalls and risk of snow-induced forest damage will decrease, particularly in the north of Finland (Kilpelainen et al. 2010).
Snow anomalies, as they interact with rising temperatures, also affect the insects that feed on boreal tree species and these can damage millions of cubic metres of timber (On-line Supplementary Material F).
Natural hazards related to snow result mainly from avalanches. Snow avalanches are well understood and safety measures are taken in many alpine regions, but the distribution, frequency and impacts are less well known in the Arctic. Likely increases in snowfall amounts during extreme events may change avalanche potential in some regions of the Arctic. A number of physically based snowpack models exist that can be used to estimate change in avalanche potential (e.g. Lehning et al. 1999). However, to date, there has been no systematic assessment of change in avalanche potential over the Arctic in response to climate change as the snowpack models require very detailed site-specific input data (e.g. SNTHERM; Lazar and Williams 2008).
Tourism and leisure pursuits are based on scenery (ice- and snow-scapes, mountains and tundra, vistas), unique Arctic wildlife (including guided hunting) and traditional indigenous cultures. Climate change and its effects such as changing snow conditions could dramatically alter all of these, but snow conditions and their impacts on tourism are not well addressed in the climate change literature.
Snow accumulation, duration and consistency will have an effect on access to attractions and snow-based activities such as dog sledding, skiing, reindeer sledding, skidoo touring and winter activities in general. Greater snow accumulation leads to access difficulties, but also to new opportunities for snow-based activities (Dawson et al. 2007). Shorter snow duration leads to seasonal challenges for some activities. Change in consistency of the snowpack, including more tundra ice versus snow leads to winter tourism challenges (such as for dog sledding, skidoo touring), and the unpredictability of snow conditions (e.g. winter thaws) could lead to negative experiences for tourists and even hazards, such as avalanches, slush torrents and floods. Snow conditions affect ecosystems, biodiversity and landscape amenity value. However, Stewart (2007) and Stewart et al. (2007) speculated that land-based tourism activities, such as sport hunting, eco- and nature tourism, retreat tourism, conference tourism and winter-based tourist activities, could play a more prominent role in western Canadian Arctic communities in the future.
Indigenous cultures, indigenous knowledge and traditional land use are intimately related to snow conditions. Climate change and its consequences are of critical importance to the cultural and economic well-being of Arctic peoples (Snyder and Stonehouse 2007). Because snow is persistent and dominant in the Arctic landscape, it plays a fundamentally important role that shapes day-to-day life, transport and resource use (such as reindeer herding and hunting).
An extensive and detailed indigenous knowledge of snow and ice conditions and their effects is sometimes complementary to scientific knowledge. This traditional understanding is reflected in indigenous languages (Callaghan et al. 2011a). Concepts of different types of snow range from new, light types of snow; to snow transformed by wind and weather and by grazing, digging and trampling; to ice-related types of snow (Riseth et al. 2010). An additional concept not yet addressed in snow and ecological research is the ground conditions during the formation of the durable snow of winter, already recorded in 1910 by Turi (cited in Riseth et al. 2010). Kumpula and Colpaert (2003) reinforced the importance of these conditions by maintaining that a hard snow or ice layer (bottom crust) that hampers foraging throughout winter is probably more important than actual snow accumulation in open, high pasture areas. In contrast, mould formation that is harmful to animals and can kill calves occurs especially after mild, rainy autumns, when the soil does not have time to freeze before the snow falls (Turunen et al. 2009).
As changes in climate and snow conditions render reindeer herding more insecure and less economically productive, there is likely to be a climate-induced shift from a mixed economy to a market-based economy. This would have significant cultural implications for indigenous peoples in the Arctic, even though the current general low-profit situation does not seem to limit the cultural value of herding (e.g. Forbes 2008).
Human health status reflects the complex interaction of all the individual, social, cultural, nutritional and socio-economic factors together with the environment (e.g. landscape and snow cover affect the health and well-being of Arctic populations). There are two categories of climate-related effects on human health: direct impacts (such as temperature and ultraviolet light), and indirect impacts (such as climate-induced changes in wildlife and zoonotic diseases; Parkinson and Butler 2005). Other important issues include contaminant concentrations which can compromise the immune system in animals and humans and thus increase risk of disease (Hansen et al. 2008), traditional food security, community adaptation to stress and community-based monitoring. The impact of climate change on wildlife species is critical to the diet of indigenous residents following a traditional way of life.
Changes in climate, such as changes in snow conditions, are likely to add to the ongoing negative impacts of general societal change and modernization in the Arctic (Bjerregaard et al. 2004). The psychosocial stress is reflected in alcohol abuse, violence and suicide, and these have all been shown to be associated with changes in lifestyle and living conditions (Curtis et al. 2005) that are affected by the impacts of changing snow conditions on traditional activities (subsistence hunting and gathering as well as recreational activities). Currently, many Arctic indigenous and other resident populations are experiencing high mortality rates from injury and suicide and higher hospitalization rates for infants with pneumonia, meningitis and respiratory infections (Heikkinen et al. 2008; Meyer et al. 2008). Wintertime mortality and morbidity will decrease with higher environmental temperatures (Näyhä 2005). However, extreme weather events, such as storms including blizzards and weather variability, will probably cause adverse health outcomes, especially for the elderly, those with chronic diseases, and children.
Reindeer herding includes many hazardous tasks in potentially dangerous climates and environments. Most Sámi reindeer herding men spend more than 800 h per year on snowmobiles (Daerga et al. 2004) and the number of deaths caused by snowmobiles and terrain vehicles tripled between 1961 and 2000 (Hassler et al. 2004). Reductions in snow cover would eventually lead to less use of snowmobiles and, perhaps, a shift away from reindeer herding in a warmer Arctic. This would result in fewer accidents. However, the psychological results might offset this, and adaptation during the transition period of changing snow conditions could be particularly difficult.
Changing Arctic snow climate is having widespread impacts and future changes will probably intensify these. Impacts can be beneficial or deleterious depending on the snow cover sensitivities involved. As snow plays a vital role in the climate system, for example through its reflectivity and by affecting moisture and hydrology, changes in snow conditions will lead to changes in climate in the Arctic and other regions. Diminished spring floods and a longer snow-free season increase the potential for evaporation and threats to wetlands, but this may be offset by new sources of water from thawing permafrost and associated thermokarst.
Snow-vegetation interactions are expected to play an important role in the future evolution of northern hydrology and thermal regimes. A shorter SCD is likely to increase plant productivity and carbon capture where soil moisture is adequate. However, reductions in the amount of water stored in the winter snowpack are already increasing the moisture stress of northern coniferous forests in summer with commercial implications. Winter thaws and rain-on-snow events that are projected to increase in frequency are already damaging vegetation and Arctic animal populations and will lead to additional challenges for commercial reindeer herding, forestry and conservation. In contrast, longer snow-free periods are likely to lead to increased breeding success for some animal species.
Changes in the snow-scape and iconic wildlife species are likely to affect Arctic tourism which has relatively little ability to diversify. As Arctic Indigenous Cultures and traditional land use are strongly dependent on snow conditions, changes in these conditions could affect the livelihoods, health and well-being of Arctic residents.
Reduced SCD is leading to changes in the storage reservoirs for contaminants and a redistribution of heavy metal pollution. Although snow-related hazards could increase in areas with projected increases in annual maximum snow accumulation, increased winter precipitation and a more even seasonal distribution of runoff may prove beneficial to the hydropower industry.
The authors wish to thank the various national funding agencies that made this review possible, specifically the Swedish Environmental Protection Agency (grant number 08/210) and the Swedish Research Council FORMAS (grant number 204-2009-45) who helped directly support this publication. The authors also gratefully acknowledge the Arctic Monitoring and Assessment Program Secretariat and the SWIPA Integration Team in helping to produce the original SWIPA report and the various contributing SWIPA chapter authors. Finally, the authors thank reviewers of the SWIPA snow chapter, particularly Barry Goodison.
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