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Ice shelf

Large platform of glacial ice
(Redirected from Ice-shelf)
Not to be confused with Shelf ice or Sea ice.

An ice shelf is a large platform of glacial ice floating on the ocean, fed by one or multiple tributary glaciers. Ice shelves form along coastlines where the ice thickness is insufficient to displace the more dense surrounding ocean water. The boundary between the ice shelf (floating) and grounded ice (resting on bedrock or sediment) is referred to as the grounding line; the boundary between the ice shelf and the open ocean (often covered by sea ice) is the ice front or calving front.

View of the Larsen Ice Shelf grounding line along the Foyn Coast of the Antarctic Peninsula. The floating ice shelf is in the left foreground, and the grounding line is visible as an abrupt change in surface slope due to flexure caused by the buoyancy force where the ice reaches flotation.

Ice shelves are found in Antarctica and the Arctic (Greenland, Northern Canada, and the Russian Arctic), and can range in thickness from about 100–1,000 m (330–3,280 ft). The world's largest ice shelves are the Ross Ice Shelf and the Filchner-Ronne Ice Shelf in Antarctica.

The movement of ice shelves is principally driven by gravity-induced pressure from the grounded ice.[1] That flow continually moves ice from the grounding line to the seaward front of the shelf. Typically, a shelf front will extend forward for years or decades between major calving events (calving is the sudden release and breaking away of a mass of ice from a glacier, iceberg, ice front, ice shelf, or crevasse).[2][3] Snow accumulation on the upper surface and melting from the lower surface are also important to the mass balance of an ice shelf. Ice may also accrete onto the underside of the shelf.

The effects of climate change are visible in the changes to the cryosphere, such as reduction in sea ice and ice sheets, and disruption of ice shelves. In the last several decades, glaciologists have observed consistent decreases in ice shelf extent through melt, calving, and complete disintegration of some shelves. Well studied examples include disruptions of the Thwaites Ice Shelf, Larsen Ice Shelf, Filchner–Ronne Ice Shelf (all three in the Antarctic) and the disruption of the Ellesmere Ice Shelf in the Arctic.

Definition

 
Some named Antarctic iceshelves.
 
Ice shelf extending approximately 6 miles into the Antarctic Sound from Joinville Island

An ice shelf is "a floating slab of ice originating from land of considerable thickness extending from the coast (usually of great horizontal extent with a very gently sloping surface), resulting from the flow of ice sheets, initially formed by the accumulation of snow, and often filling embayments in the coastline of an ice sheet."[4]: 2234 

In contrast, sea ice is formed on water, is much thinner (typically less than 3 m (9.8 ft)), and forms throughout the Arctic Ocean. It is also found in the Southern Ocean around the continent of Antarctica.

The term captured ice shelf has been used for the ice over a subglacial lake, such as Lake Vostok.

Properties

 
Panorama of Ross Ice Shelf

Ice shelves are thick plates of ice, formed continuously by glaciers, that float atop an ocean. The shelves act as "brakes" for the glaciers. These shelves serve another important purpose—"they moderate the amount of melting that occurs on the glaciers' surfaces. Once their ice shelves are removed, the glaciers increase in speed due to meltwater percolation and/or a reduction of braking forces, and they may begin to dump more ice into the ocean than they gather as snow in their catchments. Glacier ice speed increases are already observed in Peninsula areas where ice shelves disintegrated in prior years."[5]

Height

The density contrast between glacial ice and liquid water means that at least ⁠1/9⁠ of the floating ice is above the ocean surface, depending on how much pressurized air is contained in the bubbles within the glacial ice, stemming from compressed snow. The formula for the denominators above is  , density of cold seawater is about 1028 kg/m3 and that of glacial ice from about 850 kg/m3[6][7] to well below 920 kg/m3, the limit for very cold ice without bubbles.[8][9] The height of the shelf above the sea can be even larger, if there is much less dense firn and snow above the glacier ice.

By country or region

Antarctica

See also: List of Antarctic ice shelves
 
An image of Antarctica differentiating its landmass (dark grey), ice shelves (light grey), and sea ice (white)[10]

A large portion of the Antarctic coastline has ice shelves attached.[11] Their aggregate area is over 1,550,000 square kilometers (600,000 square miles).[12]

It has been found that of all the ice shelves on Earth, nearly all of them are in Antarctica.[13]: 2234 

In steady state, about half of Antarctica's ice shelf mass is lost to basal melt and half is lost to calving, but the relative importance of each process varies significantly between ice shelves.[14][15] In recent decades, Antarctica's ice shelves have been out of balance, as they have lost more mass to basal melt and calving than has been replenished by the influx of new ice and snow.[16]

Ross Ice Shelf

 
Ross Ice Shelf: "The mystic Barrier" at Bay of Whales. Note humans for size comparison (dark spots next to the large chunk of sea ice at left image border).
This section is an excerpt from Ross Ice Shelf.[edit]

The Ross Ice Shelf is the largest ice shelf of Antarctica (as of 2013, an area of roughly 500,809 square kilometres (193,363 sq mi)[17] and about 800 kilometres (500 mi) across: about the size of France).[18] It is several hundred metres thick. The nearly vertical ice front to the open sea is more than 600 kilometres (370 mi) long, and between 15 and 50 metres (50 and 160 ft) high above the water surface.[19] Ninety percent of the floating ice, however, is below the water surface.

Most of the Ross Ice Shelf is in the Ross Dependency claimed by New Zealand. It floats in, and covers, a large southern portion of the Ross Sea and the entire Roosevelt Island located in the east of the Ross Sea.

Filchner–Ronne Ice Shelf

Page 'Filchner–Ronne Ice Shelf#Description' not found

Arctic

Canada

All Canadian ice shelves are attached to Ellesmere Island and lie north of 82°N. Ice shelves that are still in existence are the Alfred Ernest Ice Shelf, Ward Hunt Ice Shelf, Milne Ice Shelf and Smith Ice Shelf. The M'Clintock Ice Shelf broke up from 1963 to 1966; the Ayles Ice Shelf broke up in 2005; and the Markham Ice Shelf broke up in 2008. The remaining ice shelves have also lost a significant amount of their area over time, with the Milne Ice Shelf being the last to be affected, with it breaking off in August 2020.

Russia

The Matusevich Ice Shelf was a 222 square kilometers (86 square miles) ice shelf located in Severnaya Zemlya being fed by some of the largest ice caps on October Revolution Island, the Karpinsky Ice Cap to the south and the Rusanov Ice Cap to the north.[20] In 2012 it ceased to exist.[21]

Disruption due to climate change

See also: Effects of climate change § Ice sheets decline
 
Processes around an Antarctic ice shelf
 
Glacier-ice shelf interactions

In the last several decades, glaciologists have observed consistent decreases in ice shelf extent through melt, calving, and complete disintegration of some shelves. Well studied examples include disruptions of the Thwaites Ice Shelf, Larsen Ice Shelf, Filchner–Ronne Ice Shelf (all three in the Antarctic) and the disruption of the Ellesmere Ice Shelf in the Arctic.

The effects of climate change are visible in the changes to the cryosphere, such as reduction in sea ice and ice sheets, and disruption of ice shelves.

Disruption of Thwaites Ice Shelf

 
Thwaites Ice Shelf (Antarctica)
This section is an excerpt from Thwaites Ice Shelf.[edit]

Thwaites Ice Shelf (), is an Antarctic ice shelf in the Amundsen Sea. It was named by ACAN[22] after Fredrik T. Thwaites, a glacial geologist and geomorphologist. The Thwaites Ice Shelf is one of the biggest ice shelves in West Antarctica, though it is highly unstable and disintegrating rapidly.[23][24] Since the 1980s, the Thwaites Glacier, nicknamed the "Doomsday glacier",[25] has had a net loss of over 600 billion tons of ice, though pinning of the Thwaites Ice Shelf has served to slow the process.[26] The Thwaites Ice Shelf has acted like a dam for the eastern portion of glacier, bracing it and allowing for a slow melt rate, in contrast to the undefended western portion.[25][27]

According to the American Geophysical Union in a 2021 study, the Thwaites Eastern Ice Shelf (TEIS) buttresses one-third of Thwaites glacier. Removal of the shelf has the potential to increase the contribution of Thwaites glacier to sea level rise by up to 25%.[28] As of 2021, the ice shelf appears to be losing its grip on a submarine shoal that acts as a pinning point and the shear margin that separates the Thwaites Eastern Ice Shelf from the Thwaites glacier Tongue has extended, further weakening the ice shelf connection to the pinning point.[28]

A sequence of Sentinel-1 radar imagery shows that parallel wing and comb cracks have recently formed rifts at high angles to the main shear margin and are propagating into the central part of the ice shelf at rates as high as 2 km per year. Satellite data, ground-penetrating radar, and GPS measurements taken in 2021 indicate that collapse of the ice shelf may be initiated by intersection of rifts with hidden basal crevasse zones as soon as 2026.[28]

Complete melting of Thwaites glacier is predicted to increase global sea levels by 65 cm (2.13 ft) according to the European Geosciences Union,[29] and the Cooperative Institute for Research in Environmental Sciences states that the collapse of Thwaites glacier could ultimately lead to sea-level rise of up to 3 meters[30] if it draws the Pine Island and surrounding glaciers with it, due to marine ice sheet instability. However, both of these processes would take time: a Science Magazine interview with the International Thwaites Glacier Collaboration researchers who had discovered the impending collapse of the ice shelf noted that the glacier itself would still take approximately several centuries to collapse even without the ice shelf,[31] and a 2022 assessment of tipping points in the climate system stated that while the West Antarctic Ice Sheet may be committed to disintegration at between 1°C and 3°C, the timescale for its collapse after that ranges between 500 and 13,000 years, with the most likely estimate of 2000 years.[32][33]

Disruption of Larsen Ice Shelf

Two sections of Antarctica's Larsen Ice Shelf broke apart into hundreds of unusually small fragments (hundreds of meters wide or less) in 1995 and 2002, Larsen C calved a huge ice island in 2017.[34]

Page 'Larsen Ice Shelf#Breakup' not found

Disruption of Larsen B Ice Shelf

Page 'Larsen Ice Shelf#Larsen B' not found

Disruption of Filchner–Ronne Ice Shelf

Page 'Filchner–Ronne Ice Shelf#Disintegration (calving)' not found

Other ice shelves in Antarctica

  • Wordie Ice Shelf has gone from an area of 1,500 km2 (580 sq mi) in 1950 to 1,400 km2 (540 sq mi) in 2000.[35]
  • Prince Gustav Ice Shelf has gone from an area of 1,600 km2 (620 sq mi) to 1,100 km2 (420 sq mi) in 2008.[35] After their loss the reduced buttressing of feeder glaciers has allowed the expected speed-up of inland ice masses after shelf ice break-up.[36]
  • The Ross Ice Shelf is the largest ice shelf of Antarctica (an area of roughly 487,000 square kilometres (188,000 sq mi) and about 800 kilometres (500 mi) across: about the size of France).[37]
  • Wilkins Ice Shelf is another ice shelf that has suffered substantial retreat. The ice shelf had an area of 16,000 km2 (6,200 sq mi) in 1998 when 1,000 km2 (390 sq mi) was lost that year.[38] In 2007 and 2008 significant rifting developed and led to the loss of another 1,400 km2 (540 sq mi) of area and some of the calving occurred in the Austral winter. The calving seemed to have resulted from preconditioning such as thinning, possibly due to basal melt, as surface melt was not as evident, leading to a reduction in the strength of the pinning point connections. The thinner ice then experienced spreading rifts and breakup.[39] This period culminated in the collapse of an ice bridge connecting the main ice shelf to Charcot Island leading to the loss of an additional 700 km2 (270 sq mi) between February and June 2009.[40]

Disruption of Ellesmere Ice Shelf (Arctic)

The Ellesmere ice shelf was reduced by 90% in the twentieth century, leaving the separate Alfred Ernest, Ayles, Milne, Ward Hunt, and Markham ice shelves. A 1986 survey of Canadian ice shelves found that 48 km2 (3.3 cubic kilometres) of ice calved from the Milne and Ayles ice shelves between 1959 and 1974.[41] The Ayles Ice Shelf calved entirely on August 13, 2005. The Ward Hunt Ice Shelf, the largest remaining section of thick (>10 meters (33 feet)) landfast sea ice along the northern coastline of Ellesmere Island, lost 600 square kilometers (230 square miles) of ice in a massive calving in 1961–1962.[42] It further decreased by 27% in thickness (13 meters (43 feet)) between 1967 and 1999.[43] In the summer of 2002, the Ward Ice Shelf experienced another major breakup,[44] and other instances of note happened in 2008 and 2010 as well.[45] The last remnant to remain mostly intact, the Milne Ice Shelf, also ultimately experienced a major breakup at the end of July 2020, losing over 40% of its area.[46]

Page 'Ellesmere Ice Shelf' not found

See also

References

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External links

 
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