2.2.5.3 Permafrost
About 25% of the land mass of the Northern Hemisphere is underlain by permafrost,
including large regions of Canada, China, Russia and Alaska, with smaller permafrost
areas in mountain chains of many other countries in both the Northern and Southern
Hemisphere (Brown et al., 1997; Zhang et al., 1999). Permafrost in large part
depends on climate. Over half of the world’s permafrost is at temperatures
a few degrees below 0°C. Temperature variations in near-surface permafrost
(20 to 200 m depth) can be used as a sensitive indicator of the inter-annual
and decade-to-century climatic variability and long-term changes in the surface
energy balance (Lachenbruch and Marshall, 1986; Lachenbruch et al., 1988; Clow
et al., 1991; Beltrami and Taylor, 1994; Majorowicz and Judge, 1994). Very small
changes in surface climate can produce important changes in permafrost temperatures.
Lachenbruch and Marshall (1986) used climate reconstructions from deep (>125
m depth) temperature measurements in permafrost to show that there has been
a general warming of the permafrost in the Alaskan Arctic of 2 to 4°C over
the last century.
Evidence of change in the southern extent of the discontinuous permafrost zone
in the last century has also been recorded. In North America, the southern boundary
of the discontinuous permafrost zone has migrated northward in response to warming
after the Little Ice Age, and continues to do so today (Thie, 1974; Vitt et
al., 1994; Halsey et al., 1995; Laberge and Payette, 1995; French and Egorov,
1998). In China both an increase in the lower altitudinal limit of mountain
permafrost and a decrease in areal extent have been observed (Wang et al., 2000).
Long-term monitoring of shallow permafrost began in earnest in the last few
decades. Recent analyses indicate that permafrost in many regions of the earth
is currently warming (Gravis et al., 1988; Haeberli et al., 1993; Osterkamp,
1994; Pavlov, 1994; Wang and French, 1994; Ding, 1998; Sharkhuu, 1998; Vonder
Mühll et al., 1998; Weller and Anderson, 1998; Osterkamp and Romanovsky,
1999; Romanovsky and Osterkamp, 1999). However, the onset, magnitude (from a
few tenths to a few degrees centigrade) and rate of warming varies regionally,
and not all sites in a given region show the same trend (Osterkamp and Romanovsky,
1999). This variability, as well as short-term (decadal or less) trends superimposed
on long-term (century) trends, is briefly discussed in Serreze et al. (2000).
There has also been evidence of recent permafrost cooling into the mid-1990s
in parts of north-eastern and north-western Canada (Allard et al., 1995; Burn,
1998). However, there are regional data gaps, such as in the central and high
Arctic in North America. A new international permafrost thermal monitoring network
(Burgess et al., 2000) is being developed to help address these gaps and document
the spatial and temporal variability across the globe.
Properties of the surface and the active layer (that having seasonal freezing
and thawing) affect surface heat exchanges in permafrost regions. Other conditions
remaining constant, the thickness of the active layer could be expected to increase
in response to warming of the climate. A circumpolar network to monitor active-layer
thickness at representative locations was developed in the 1990s to track long-term
trends in active layer thickness (Nelson and Brown, 1997). Active layer thickness
time-series are becoming available (Nelson et al., 1998; Nixon and Taylor, 1998),
and evidence of increasing thaw depths is starting to be reported (Pavlov, 1998;
Wolfe et al., 2000).
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