Annual mean ground temperatures (Tg) decline northward from approximately −3.0°C in the boreal forest to −7.0°C in dwarf-shrub tundra in the Tuktoyuktuk Coastlands and Anderson Plain, NWT, Canada. The latitudinal decrease in Tg from forest to tundra is accompanied by an increase in the range of values measured in the central, tall-shrub tundra zone. Field measurements from 124 sites across this ecotone indicate that in undisturbed terrain Tg may approach 0°C in the forest and −4°C in dwarf-shrub tundra. The greatest range of local variation in Tg (~7°C) was observed in the tall-shrub transition zone. Undisturbed terrain units with relatively high Tg include riparian areas and slopes with drifting snow, saturated soils in polygonal peatlands and areas near lakes. Across the region, the warmest permafrost is associated with disturbances such as thaw slumps, drained lakes, areas burned by wildfires, drilling-mud sumps and roadsides. Soil saturation following terrain subsidence may increase the latent heat content of the active layer, while increases in snow depth decrease the rate of ground heat loss in autumn and winter. Such disturbances increase freezeback duration and reduce the period of conductive ground cooling, resulting in higher Tg and, in some cases, permafrost thaw. The field measurements reported here confirm that minimum Tg values in the uppermost 10 m of permafrost have increased by ~2°C since the 1970s. The widespread occurrence of Tg above −3°C indicates warm permafrost exists in disturbed and undisturbed settings across the transition from forest to tundra. Copyright

active layer, climate change, ground temperature, Mackenzie Delta area, terrain disturbance, tree line
dx.doi.org/10.1002/ppp.1934
Permafrost and Periglacial Processes
Department of Geography and Environmental Studies

Kokelj, S.V. (S. V.), Palmer, M.J. (M. J.), Lantz, T.C. (T. C.), & Burn, C. (2017). Ground Temperatures and Permafrost Warming from Forest to Tundra, Tuktoyaktuk Coastlands and Anderson Plain, NWT, Canada. Permafrost and Periglacial Processes, 28(3), 543–551. doi:10.1002/ppp.1934