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In geology, permafrost is ground,[1] including rock or (cryotic) soil, at or below the freezing point of water 0 °C (32 °F) for two or more years. Most permafrost is located in high latitudes (in and around the Arctic and Antarctic regions), but at lower latitudes alpine permafrost occurs at higher elevations. Ground ice is not always present, as may be in the case of non-porous bedrock, but it frequently occurs and it may be in amounts exceeding the potential hydraulic saturation of the ground material. Permafrost
Permafrost
accounts for 0.022% of total water on Earth[2] and exists in 24% of exposed land in the Northern Hemisphere.[3][4] It also occurs subsea on the continental shelves of the continents surrounding the Arctic Ocean, portions of which were exposed during the last glacial period,[5] with global weather implications.[6] A global temperature rise of 1.5 °C (2.7 °F) above current levels would be enough to start the thawing of permafrost in Siberia, according to one group of scientists.[4][7]

Contents

1 Extent

1.1 Continuity of coverage

1.1.1 Discontinuous permafrost 1.1.2 Continuous permafrost

1.2 Alpine permafrost 1.3 Subsea permafrost

2 Manifestations

2.1 Base depth 2.2 Massive ground ice 2.3 Landforms 2.4 Carbon
Carbon
cycle in permafrost

3 Climate
Climate
change effects

3.1 Historical changes 3.2 Thaw 3.3 Effect on slope stability 3.4 Ecological consequences 3.5 Predicted rate of change in the Arctic

4 Other issues

4.1 Construction on permafrost 4.2 Revival of organisms preserved in permafrost

5 References 6 External links

Extent[edit]

Red lines: Seasonal temperature extremes (dotted=average).

Permafrost
Permafrost
is soil, rock or sediment that is frozen for more than two consecutive years. In areas not overlain by ice, it exists beneath a layer of soil, rock or sediment, which freezes and thaws annually and is called the "active layer".[8] In practice, this means that permafrost occurs at an average air temperature of -2 °C or colder. Active layer
Active layer
thickness varies with the season, but is 0.3 to 4 meters thick (shallow along the Arctic coast; deep in southern Siberia and the Qinghai-Tibetan Plateau). In the Northern Hemisphere, 24% of the ice-free land area, equivalent to 19 million square kilometers,[9] is more or less influenced by permafrost. Most of this area is found in Siberia, northern Canada, Alaska
Alaska
and Greenland. Beneath the active layer annual temperature swings of permafrost become smaller with depth. The deepest depth of permafrost occurs where geothermal heat maintains a temperature above freezing. Above that bottom limit there may be permafrost, whose temperature doesn't change annually—"isothermal permafrost".[10] The extent of permafrost varies with the climate. Today, a considerable area of the Arctic is covered by permafrost (including discontinuous permafrost). Overlying permafrost is a thin active layer that seasonally thaws during the summer. Plant
Plant
life can be supported only within the active layer since growth can occur only in soil that is fully thawed for some part of the year. Thickness of the active layer varies by year and location, but is typically 0.6–4 m (2.0–13.1 ft) thick. In areas of continuous permafrost and harsh winters, the depth of the permafrost can exceed 1,400 m (4,600 ft).[11] Permafrost
Permafrost
can also store carbon, both as peat and as methane. Work investigating the permafrost carbon pool size estimates that 1400–1700 Gt of carbon is stored in the northern circumpolar permafrost region.[12] While a recent study that includes stores of the Tibetan Plateau, estimates total carbon pools in the permafrost of the Northern Hemisphere
Northern Hemisphere
to be 1832 Gt.[13] This large carbon pool represents more carbon than currently exists in all living things.

Excavating ice-rich permafrost with a jackhammer in Alaska.

Continuity of coverage[edit] Permafrost
Permafrost
typically forms in any climate where the mean annual air temperature is less than the freezing point of water. Exceptions are found in moist-wintered forest climates, such as in Northern Scandinavia and the North-Eastern part of European Russia west of the Urals, where snow acts as an insulating blanket. Glaciated areas may be exceptions. Since all glaciers are warmed at their base by geothermal heat, temperate glaciers, which are near the pressure-melting point throughout, may have liquid water at the interface with the ground and are therefore free of underlying permafrost.[14] "Fossil" cold anomalies in the Geothermal gradient
Geothermal gradient
in areas where deep permafrost developed during the Pleistocene
Pleistocene
persist down to several hundred metres. This is evident from temperature measurements in boreholes in North America
North America
and Europe.[15] Discontinuous permafrost[edit] Typically, the below-ground temperature varies less from season to season than the air temperature, with mean annual temperatures tending to increase with depth. Thus, if the mean annual air temperature is only slightly below 0 °C (32 °F), permafrost will form only in spots that are sheltered—usually with a northerly aspect—creating discontinuous permafrost. Usually, permafrost will remain discontinuous in a climate where the mean annual soil surface temperature is between −5 and 0 °C (23 and 32 °F). In the moist-wintered areas mentioned before, there may not be even discontinuous permafrost down to −2 °C (28 °F). Discontinuous permafrost is often further divided into extensive discontinuous permafrost, where permafrost covers between 50 and 90 percent of the landscape and is usually found in areas with mean annual temperatures between −2 and −4 °C (28 and 25 °F), and sporadic permafrost, where permafrost cover is less than 50 percent of the landscape and typically occurs at mean annual temperatures between 0 and −2 °C (32 and 28 °F).[16] In soil science, the sporadic permafrost zone is abbreviated SPZ and the extensive discontinuous permafrost zone DPZ.[17] Exceptions occur in un-glaciated Siberia
Siberia
and Alaska
Alaska
where the present depth of permafrost is a relic of climatic conditions during glacial ages where winters were up to 11 °C (20 °F) colder than those of today. Continuous permafrost[edit]

Estimated extent of alpine permafrost by region[18]

Locality Area (×1,000)

Qinghai- Tibet
Tibet
Plateau 1,300 km2 (500 sq mi)

Khangai-Altai Mountains 1,000 km2 (390 sq mi)

Brooks Range 263 km2 (102 sq mi)

Siberian
Siberian
Mountains 255 km2 (98 sq mi)

Greenland 251 km2 (97 sq mi)

Ural Mountains 125 km2 (48 sq mi)

Andes 100 km2 (39 sq mi)

Rocky Mountains
Rocky Mountains
(US and Canada) 100 km2 (39 sq mi)

Fennoscandian
Fennoscandian
mountains 75 km2 (29 sq mi)

Remaining <100 km2 (39 sq mi)

At mean annual soil surface temperatures below −5 °C (23 °F) the influence of aspect can never be sufficient to thaw permafrost and a zone of continuous permafrost (abbreviated to CPZ) forms. A line of continuous permafrost in the Northern Hemisphere[19] represents the most southerly border where land is covered by continuous permafrost or glacial ice. The line of continuous permafrost varies around the world northward or southward due to regional climatic changes. In the southern hemisphere, most of the equivalent line would fall within the Southern Ocean
Southern Ocean
if there were land there. Most of the Antarctic continent is overlain by glaciers, under which much of the terrain is subject to basal melting.[20] The exposed land of Antarctica
Antarctica
is substantially underlain with permafrost,[21] some of which is subject to warming and thawing along the coastline.[22] Alpine permafrost[edit] Estimates of the total area of alpine permafrost vary. Bockheim and Munroe[18] combined three sources and made the tabulated estimates by region, totaling 3,560,000 km2 (1,370,000 sq mi). Alpine permafrost in the Andes
Andes
has not been mapped.[23] Its extent has been modeled to assess the amount of water bound up in these areas.[24] In 2009, a researcher from Alaska
Alaska
found permafrost at the 4,700 m (15,400 ft) level on Africa's highest peak, Mount Kilimanjaro, approximately 3° north of the equator.[25] Subsea permafrost[edit] Subsea permafrost occurs beneath the seabed and exists in the continental shelves of the polar regions.[5] These areas formed during the last ice age, when a larger portion of Earth's water was bound up in ice sheets on land and when sea levels were low. As the ice sheets melted to again become seawater, the permafrost became submerged shelves under relatively warm and salty boundary conditions, compared to surface permafrost. Therefore, subsea permafrost exists in conditions that lead to its diminishment. According to Osterkamp, subsea permafrost is a factor in the "design, construction, and operation of coastal facilities, structures founded on the seabed, artificial islands, sub-sea pipelines, and wells drilled for exploration and production."[1] It also contains gas hydrates in places, which are both a "potential abundant source of energy", but also may destabilize, as subsea permafrost warms and thaws, producing large amounts of methane gas, which is a potent green-house gas.[1][26] Manifestations[edit]

Time required for permafrost to reach depth at Prudhoe Bay, Alaska[27]

Time (yr) Permafrost
Permafrost
depth

1 4.44 m (14.6 ft)

350 79.9 m (262 ft)

3,500 219.3 m (719 ft)

35,000 461.4 m (1,514 ft)

100,000 567.8 m (1,863 ft)

225,000 626.5 m (2,055 ft)

775,000 687.7 m (2,256 ft)

Base depth[edit] Permafrost
Permafrost
extends to a base depth where geothermal heat from the Earth
Earth
and the mean annual temperature at the surface achieve an equilibrium temperature of 0 °C.[28] The base depth of permafrost reaches 1,493 m (4,898 ft) in the northern Lena and Yana River
Yana River
basins in Siberia.[11] The geothermal gradient is the rate of increasing temperature with respect to increasing depth in the Earth's interior. Away from tectonic plate boundaries, it is about 25–30 °C/km (72–87 °F/mi) near the surface in most of the world.[29] It varies with the thermal conductivity of geologic material and is less for permafrost in soil than in bedrock.[28] Calculations indicate that the time required to form the deep permafrost underlying Prudhoe Bay, Alaska
Alaska
was over a half-million years.[27][30] This extended over several glacial and interglacial cycles of the Pleistocene
Pleistocene
and suggests that the present climate of Prudhoe Bay is probably considerably warmer than it has been on average over that period. Such warming over the past 15,000 years is widely accepted.[27] The table to the right shows that the first hundred metres of permafrost forms relatively quickly but that deeper levels take progressively longer. Massive ground ice[edit]

Massive blue ground ice exposure on the north shore of Herschel Island, Yukon, Canada.

When the ice content of a permafrost exceeds 250 percent (ice to dry soil by mass) it is classified as massive ice. Massive ice bodies can range in composition, in every conceivable gradation from icy mud to pure ice. Massive icy beds have a minimum thickness of at least 2 m, a short diameter of at least 10 m.[31] First recorded North American observations were by European scientists at Canning River, Alaska
Alaska
in 1919.[32] Russian literature provides an earlier date of 1735 and 1739 during the Great North Expedition by P. Lassinius and Kh. P. Laptev, respectively.[33] Two categories of massive ground ice are buried surface ice and intrasedimental ice[34] (also called constitutional ice).[33] Buried surface ice may derive from snow, frozen lake or sea ice, aufeis (stranded river ice) and—probably the most prevalent—buried glacial ice.[35] Intrasedimental ice forms by in-place freezing of subterranean waters and is dominated by segregational ice which results from the crystallizational differentiation taking place during the freezing of wet sediments, accompanied by water migrating to the freezing front.[33] Intrasedimental or constitutional ice has been widely observed and studied across Canada and also includes intrusive and injection ice.[32][33] Additionally, ice wedges—a separate type of ground ice—produce recognizable patterned ground or tundra polygons. Ice wedges form in a pre-existing geological substrate and were first described in 1919.[32][33]

Several types of massive ground ice, including ice wedges and intrasedimental ice within the cliff wall of a retrogressive thaw slump located on the southern coast of Herschel Island within an approximately 22-metre (72 ft) by 1,300-metre (4,300 ft) headwall.

Landforms[edit] Permafrost
Permafrost
processes manifest themselves in large-scale land forms, such as palsas and pingos[36] and smaller-scale phenomena, such as patterned ground found in arctic, periglacial and alpine areas.[37]

A group of palsas, as seen from above, formed by the growth of ice lenses.

Pingos near Tuktoyaktuk, Northwest Territories, Canada

Ground polygons

Stone rings on Spitsbergen

Ice wedges seen from top

Solifluction
Solifluction
on Svalbard

Contraction crack (ice wedge) polygons on Arctic sediment.

Cracks forming at the edges of the Storflaket
Storflaket
permafrost bog in Sweden.

Carbon
Carbon
cycle in permafrost[edit] The permafrost carbon cycle (Arctic Carbon
Carbon
Cycle) deals with the transfer of carbon from permafrost soils to terrestrial vegetation and microbes, to the atmosphere, back to vegetation, and finally back to permafrost soils through burial and sedimentation due to cryogenic processes. Some of this carbon is transferred to the ocean and other portions of the globe through the global carbon cycle. The cycle includes the exchange of carbon dioxide and methane between terrestrial components and the atmosphere, as well as the transfer of carbon between land and water as methane, dissolved organic carbon, dissolved inorganic carbon, particulate inorganic carbon and particulate organic carbon.[38] Climate
Climate
change effects[edit] Arctic permafrost has been diminishing for many centuries. The consequence is thawing soil, which may be weaker, and release of methane, which contributes to an increased rate of global warming as part of a feedback loop. Historical changes[edit]

Recently thawed Arctic permafrost and coastal erosion on the Beaufort Sea, Arctic Ocean, near Point Lonely, Alaska. Photo Taken in August, 2013

At the Last Glacial Maximum, continuous permafrost covered a much greater area than it does today, covering all of ice-free Europe
Europe
south to about Szeged
Szeged
(southeastern Hungary) and the Sea of Azov
Sea of Azov
(then dry land)[39] and East Asia
East Asia
south to present-day Changchun
Changchun
and Abashiri.[40] In North America, only an extremely narrow belt of permafrost existed south of the ice sheet at about the latitude of New Jersey through southern Iowa
Iowa
and northern Missouri, but permafrost was more extensive in the drier western regions where it extended to the southern border of Idaho
Idaho
and Oregon.[41] In the southern hemisphere, there is some evidence for former permafrost from this period in central Otago
Otago
and Argentine Patagonia, but was probably discontinuous, and is related to the tundra. Alpine permafrost also occurred in the Drakensberg
Drakensberg
during glacial maxima above about 3,000 metres (9,840 ft).[42][43] Thaw[edit] See also: Thermokarst

Permafrost
Permafrost
thaw ponds on peatland in Hudson Bay, Canada in 2008.[44]

The ground can consist of many substrate materials, including bedrock, sediment, organic matter, water or ice. Frozen ground is that which is below the freezing point of water, whether or not water is present in the substrate. Ground ice is not always present, as may be the case with nonporous bedrock, but it frequently occurs and may be present in amounts exceeding the potential hydraulic saturation of the thawed substrate. By definition, permafrost is ground that remains frozen for two or more years. Since frozen soil, including permafrost, comprises a large percentage of substrate materials other than ice, it thaws rather than melts even as any ice content melts.[45] An analogy is when a freezer door is left open, although the ice in the freezer may change phase to a liquid, the food solids will not experience a phase change. In aggregate, the food thaws but does not melt. Melting implies the phase change of all solids to liquid. One visible sign of permafrost degradation is the random displacement of trees from their vertical orientation in permafrost areas.[46][47] As a consequence, precipitation has increased which in turn results in the weakening and eventual collapse of buildings in areas such as Norilsk in northern Russia, which lies upon the permafrost.[48] Effect on slope stability[edit] Over the past century, an increasing number of alpine rock slope failure events in mountain ranges around the world have been recorded. It is expected that the high number of structural failures is due to permafrost thawing, which is thought to be linked to climate change. Permafrost
Permafrost
thawing is thought to have contributed to the 1987 Val Pola landslide that killed 22 people in the Italian Alps.[49] In mountain ranges, much of the structural stability can be attributed to glaciers and permafrost. As climate warms, permafrost thaws, which results in a less stable mountain structure, and ultimately more slope failures.[50] McSaveney [51] reported massive rock and ice falls (up to 11.8 million m3), earthquakes (up to 3.9 Richter), floods (up to 7.8 million m3 water), and rapid rock-ice flow to long distances (up to 7.5 km at 60 m/s) caused by “instability of slopes” in high mountain permafrost. Instability of slopes in permafrost at elevated temperatures near freezing point in warming permafrost is related to effective stress and buildup of pore-water pressure in these soils.[52] Kia and his co-inventors [53] invented a new filter-less rigid piezometer (FRP) for measuring pore-water pressure in partially frozen soils such as warming permafrost soils. They extended the use of effective stress concept to partially frozen soils for use in slope stability analysis of warming permafrost slopes. The use of effective stress concept has many advantages such as ability to extend the concepts of "Critical State Soil
Soil
Mechanics" into frozen ground engineering. Ecological consequences[edit] Worldwide, permafrost contains 1700 billion tons of organic material equaling almost half of all organic material in all soils.[9] This pool was built up over thousands of years and is only slowly degraded under the cold conditions in the Arctic. The amount of carbon sequestered in permafrost is four times the carbon that has been released to the atmosphere due to human activities in modern time.[54] One manifestation of this is yedoma, which is an organic-rich (about 2% carbon by mass) Pleistocene-age loess permafrost with ice content of 50–90% by volume.[55] Formation of permafrost has significant consequences for ecological systems, primarily due to constraints imposed upon rooting zones, but also due to limitations on den and burrow geometries for fauna requiring subsurface homes. Secondary effects impact species dependent on plants and animals whose habitat is constrained by the permafrost. One of the most widespread examples is the dominance of Black Spruce in extensive permafrost areas, since this species can tolerate rooting pattern constrained to the near surface.[56] One gram of soil from the active layer may include more than one billion bacteria cells. If placed along each other, bacteria from one kilogram of active layer soil will form a 1000 km long chain. The number of bacteria in permafrost soil varies widely, typically from 1 to 1000 million per gram of soil.[57] Most of these bacteria and fungi in permafrost soil can not be cultured in the laboratory, but the identity of the microorganisms can be revealed by DNA-based techniques. The Arctic region is one of the many natural sources of the greenhouse gas methane.[58] Global warming accelerates its release, due to both release of methane from existing stores, and from methanogenesis in rotting biomass.[59] Large quantities of methane are stored in the Arctic in natural gas deposits, permafrost, and as submarine clathrates. Permafrost
Permafrost
and clathrates degrade on warming, thus large releases of methane from these sources may arise as a result of global warming.[60][61] Other sources of methane include submarine taliks, river transport, ice complex retreat, submarine permafrost and decaying gas hydrate deposits.[62] Preliminary computer analyses suggest that permafrost could produce carbon equal to 15 percent or so of today’s emissions from human activities.[63] A hypothesis forwarded by Sergey Zimov
Sergey Zimov
is that the reduction of herds of large herbivores has increased the ratio of energy emission and energy absorption tundra (energy balance) in a manner that increases the tendency for net thawing of permafrost.[64] He is testing this hypothesis in an experiment at Pleistocene
Pleistocene
Park, a nature reserve in northeastern Siberia.[65]

Predicted rate of change in the Arctic[edit] See also: Arctic methane release According to IPCC Fifth Assessment Report there is high confidence that permafrost temperatures have increased in most regions since the early 1980s. Observed warming was up to 3 °C in parts of Northern Alaska
Alaska
(early 1980s to mid-2000s) and up to 2 °C in parts of the Russian European North (1971–2010).[66] In Yukon, the zone of continuous permafrost might have moved 100 kilometres (62 mi) poleward since 1899, but accurate records only go back 30 years. It is thought that permafrost thawing could exacerbate global warming by releasing methane and other hydrocarbons, which are powerful greenhouse gases.[67][68][69] It also could encourage erosion because permafrost lends stability to barren Arctic slopes. Arctic temperatures are expected to increase at roughly twice the global rate.[70] The Intergovernmental Panel on Climate
Climate
Change (IPCC) will in their fifth report establish scenarios for the future, where the temperature in the Arctic will rise between 1.5 and 2.5 °C by 2040 and with 2 to 7.5 °C by 2100. Estimates vary on how many tons of greenhouse gases are emitted from thawed permafrost soils. One estimate suggests that 110–231 billion tons of CO2 equivalents (about half from carbon dioxide and the other half from methane) will be emitted by 2040, and 850–1400 billion tons by 2100.[54] This corresponds to an average annual emission rate of 4–8 billion tons of CO2 equivalents in the period 2011–2040 and annually 10–16 billion tons of CO2 equivalents in the period 2011–2100 as a result of thawing permafrost. For comparison, the anthropogenic emission of all greenhouse gases in 2010 is approximately 48 billion tons of CO2 equivalents.[71] Release of greenhouse gases from thawed permafrost to the atmosphere may increase global warming. Other issues[edit] The International Permafrost Association
International Permafrost Association
(IPA) is an integrator of issues regarding permafrost. It convenes International Permafrost Conferences, undertakes special projects such as preparing databases, maps, bibliographies, and glossaries, and coordinates international field programmes and networks. Among other issues addressed by the IPA are: Problems for construction on permafrost owing to the change of soil properties of the ground on which structures are placed and the biological processes in permafrost, e.g. the preservation of organisms frozen in situ. Construction on permafrost[edit] Building on permafrost is difficult because the heat of the building (or pipeline) can thaw the permafrost and destabilize the structure. Three common solutions include: using foundations on wood piles; building on a thick gravel pad (usually 1–2 metres/3.3–6.6 feet thick); or using anhydrous ammonia heat pipes.[72] The Trans-Alaska Pipeline System uses heat pipes built into vertical supports to prevent the pipeline from sinking and the Qingzang railway
Qingzang railway
in Tibet employs a variety of methods to keep the ground cool, both in areas with frost-susceptible soil. Permafrost
Permafrost
may necessitate special enclosures for buried utilities, called "utilidors". The Permafrost
Permafrost
Research Institute in Yakutsk, found that the sinking of large buildings into the ground can be prevented by using pile foundations extending down to 15 metres (49 ft) or more. At this depth the temperature does not change with the seasons, remaining at about −5 °C (23 °F).

Modern buildings in permafrost zones may be built on piles to avoid permafrost-thaw foundation failure from the heat of the building.

Heat pipes in vertical supports maintain a frozen bulb around portions of the Trans- Alaska
Alaska
Pipeline that are at risk of thawing.

Above-ground utility lines in a permafrost zone avoid thawing of ground.

Pile foundations in Yakutsk, a city underlain with continuous permafrost.

Revival of organisms preserved in permafrost[edit] In 2012, Russian researchers have proved that permafrost can serve as a natural depository for ancient life forms by reviving of Silene stenophylla from 30,000 year old tissue found in an Ice Age
Ice Age
squirrel burrow in the Siberian
Siberian
permafrost. This the oldest plant tissue ever revived. The plant was fertile, producing white flowers and viable seeds. The study demonstrated that tissue can survive ice preservation for tens of thousands of years.[73] A 2016 outbreak of anthrax in the Yamal Peninsula
Yamal Peninsula
is believed to be due to thawing permafrost.[74] References[edit]

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External links[edit]

Wikimedia Commons has media related to Permafrost.

Permafrostwatch University of Alaska
Alaska
Fairbanks International Permafrost Association
International Permafrost Association
(IPA) Center for Permafrost Map of permafrost in Antarctica. Permafrost
Permafrost
– what is it? – YouTube (Alfred Wegener Institute)

v t e

Periglacial
Periglacial
environment

Landforms

Blockfield Bratschen Cryoplanation terrace Paha Palsa Periglacial
Periglacial
lake Pingo Protalus rampart Rock glacier Strandflat Glaciokarst Thermokarst

Patterned ground

Frost boil Polygons Solifluction
Solifluction
lobes and sheets Sorted stripe Stone ring

Processes

Cryoplanation Cryosuction Cryoturbation Fluvio-thermal erosion Frost heave Frost weathering Gelifluction Ice segregation Methane
Methane
release Nivation Solifluction Zero-curtain effect

Soils and deposits

Active layer Gelisols Ice wedge Loess Peat Permafrost Stratified slope deposit Talik Yedoma

Biomes and ecotones

Arctic tundra Arctic tree line Antarctic oasis Antarctic tundra Montane grasslands and shrublands Alpine tundra Alpine tree line (Massenerhebung effect) Taiga
Taiga
(Drunken trees)

Climate

Alpine Polar Subpolar

Category: Periglacial
Periglacial
landforms Template:Glaciers

Authority control

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