Pine Island Glacier
British Antarctic Survey field camp on PIG
Map showing the location of Pine Island Glacier
Map showing the location of Pine Island Glacier
TypeIce stream
LocationWest Antarctic Ice Sheet, Antarctica
Coordinates75°10′S 100°0′W / 75.167°S 100.000°W / -75.167; -100.000[1]
Area175,000 km2 (68,000 sq mi) (whole catchment)[2]
LengthApprox. 250 km (160 mi)[2]
ThicknessApprox. 2 km (1.2 mi)
TerminusFloating Ice shelf
StatusAccelerating

Pine Island Glacier (PIG) is a large ice stream, and the fastest melting glacier in Antarctica, responsible for about 25% of Antarctica's ice loss.[3] The glacier ice streams flow west-northwest along the south side of the Hudson Mountains into Pine Island Bay, Amundsen Sea, Antarctica. It was mapped by the United States Geological Survey (USGS) from surveys and United States Navy (USN) air photos, 1960–66, and named by the Advisory Committee on Antarctic Names (US-ACAN) in association with Pine Island Bay.[1][4]

The area drained by Pine Island Glacier comprises about 10% of the West Antarctic Ice Sheet.[5] Satellite measurements have shown that the Pine Island Glacier Basin has a greater net contribution of ice to the sea than any other ice drainage basin in the world and this has increased due to recent acceleration of the ice stream.[6][7]

An iceberg about twice the size of Washington, DC broke off from the glacier in February 2020. Pine Island Glacier's ice velocity has accelerated to over 33 feet per day.[8]

The ice stream is extremely remote, with the nearest continually occupied research station at Rothera, nearly 1,300 km (810 mi) away.[9] The area is not claimed by any nations and the Antarctic Treaty prohibits any new claims while it is in force.[10]

Major rift in the Pine Island Glacier.
Pine Island Glacier, at left, and Thwaites Glacier have recently averaged ice elevation losses of 6 meters per year in places.
This "airborne" tour was created from only a small portion of the images collected during a flight over the Pine Island Glacier crack on October 26, 2011.

Ice sheet drainage

Floating ice shelf at the downstream end of Pine Island Glacier. The crack shows the start of a large iceberg calving

The Antarctic ice sheet is the largest mass of ice on earth, containing a volume of water equivalent to 57 m (187 ft) of global sea level.[11] The ice sheet forms from snow which falls onto the continent and compacts under its own weight. The ice then moves under its own weight toward the edges of the continent. Most of this transport to the sea is by ice streams (faster moving channels of ice surrounded by slower moving ice walls) and outlet glaciers.[11] The Antarctic ice sheet consists of the large, relatively stable, East Antarctic Ice Sheet and a smaller, less stable, West Antarctic Ice Sheet. The West Antarctic Ice Sheet is drained into the sea by several large ice streams, most of which flow into either Ross Ice Shelf, or Filchner-Ronne Ice Shelf. Pine Island and Thwaites Glaciers are two major West Antarctic ice streams which do not flow into a large ice shelf. They are part of an area called the Amundsen Sea Embayment. A total area of 175,000 km2 (68,000 sq mi), 10 percent of the West Antarctic Ice Sheet, drains out to the sea via Pine Island Glacier, this area is known as the Pine Island Glacier drainage basin.[2][5]

Weak underbelly of the West Antarctic Ice Sheet

The Pine Island and Thwaites glaciers are two of Antarctica's five largest ice streams. Scientists have found that the flow of these ice streams has accelerated in recent years, and suggested that if they were to melt, global sea levels would rise by 1 to 2 m (3 ft 3 in to 6 ft 7 in), destabilising the entire West Antarctic Ice Sheet and perhaps sections of the East Antarctic Ice Sheet.[12]

In 1981 Terry Hughes proposed that the region around Pine Island Bay may be a "weak underbelly" of the West Antarctic Ice Sheet.[13] This is based on the fact that, unlike the majority of the large West Antarctic ice streams, those flowing into the Amundsen Sea are not protected from the ocean by large floating ice shelves. Also, although the surface of the glacier is above sea level, the base lies below sea level and slopes downward inland, this suggests that there is no geological barrier to stop a retreat of the ice once it has started.[13]

Acceleration and thinning

The Pine Island glacier began to retreat in the 1940s.[14] Prior to this retreat, the grounding line of Pine Island Glacier was located on a prominent seabed ridge. This ridge now acts as a barrier, restricting the amount of relatively warm circumpolar deep water that can reach the thickest ice.[15]

The speed of Pine Island Glacier increased by 77 percent from 1974 to the end of 2013, with half of this increase occurring between 2003 and 2009.[16] This speed up has meant that by the end of 2007 the Pine Island Glacier system had a negative mass balance of 46 gigatonnes per year,[7] which is equivalent to 0.13 mm (0.0051 in) per year global sea level rise.[17] In other words, much more water was being put into the sea by PIG than was being replaced by snowfall. Measurements along the centre of the ice stream by GPS demonstrated that this acceleration is still high nearly 200 km (120 mi) inland, at around 4 percent over 2007.[18] It has been suggested that this recent acceleration could have been triggered by warm ocean waters at the end of PIG, where it has a floating section (ice shelf) approximately 50 km (31 mi) long.[4][5][19] It has also been shown that PIG underwent rapid thinning during the Holocene, and that this process may continue for centuries after it is initiated.[20]

As the ice stream accelerates it is also getting steeper.[18] The rate of thinning within the central trunk has quadrupled from 1995 to 2006.[18][21] If the current rate of acceleration were to continue the main trunk of the glacier could be afloat within 100 years.[21]

The ice front stayed in a more or less stable position from 1973 to 2014, with a 10 km retreat in 2015.[22]

Subglacial volcano

In January 2008, British Antarctic Survey (BAS) scientists reported that 2,200 years ago a volcano erupted under the Antarctic ice sheet. This was the biggest Antarctic eruption in the last 10,000 years. The volcano is situated in the Hudson Mountains, close to Pine Island Glacier.[23][24] The eruption spread a layer of volcanic ash and tephra over the surface of the ice sheet. This ash was then buried under the snow and ice. The date of the eruption was estimated from the depth of burial of the ash. This method uses dates calculated from nearby ice cores.[24] The presence of the volcano raises the possibility that volcanic activity could have contributed, or may contribute in the future, to increases in the flow of the glacier.[25] In 2018 it was found that there is a substantial volcanic heat source beneath Pine Island Glacier approximately half as large as the active Grimsvötn volcano on Iceland.[26] The same year a study was published concluding that the bedrock below WAIS was uplifted at a higher rate than previously thought, the authors suggested this could eventually help to stabilize the ice sheet.[27]

Climate engineering

Pine Island Glacier, as well as the better known Thwaites Glacier, can both substantially exacerbate future sea level rise. Consequently, some scientists, most notably Michael J. Wolovick and John C. Moore, have suggested stabilizing them via climate engineering aiming to block warm water flows from the ocean. Their first proposal focused on Thwaites, and estimated that even reinforcing it physically at weakest points, without building larger structures to block water flows, would be among "the largest civil engineering projects that humanity has ever attempted", yet only 30% likely to work.[28]

This section is an excerpt from Thwaites Glacier § Engineering options for stabilization.[edit]
A proposed "underwater sill" blocking 50% of warm water flows heading for the glacier could have the potential to delay its collapse and the resultant sea level rise by many centuries.[29]

In 2023, a modified proposal was tabled: it was proposed that an installation of underwater "curtains", made out of a flexible material and anchored to Amundsen Sea floor would be able to interrupt warm water flow while reducing costs and increasing their longevity (conservatively estimated at 25 years for curtain elements and up to 100 years for the foundations) relative to more rigid structures. With them in place, Thwaites Ice Shelf and Pine Island Ice Shelf would presumably be able to regrow to a state they last had a century ago, thus stabilizing these glaciers.[30][31][32] To achieve this, the curtains would have to be placed at a depth of around 600 metres (0.37 miles) (to avoid damage from icebergs which would be regularly drifting above) and be 80 km (50 mi) long. The authors acknowledged that while work on this scale would be unprecedented and face many challenges in the Antarctic (including polar night and the currently insufficient numbers of specialized polar ships and underwater vessels), it would also not require any new technology and there is already experience of laying down pipelines at such depths.[30][31]

Diagram of a proposed "curtain".[30]
The authors estimated that this project would take a decade to construct, at $40–80 billion initial cost, while the ongoing maintenance would cost $1–2 billion a year.[30][31] Yet, a single seawall capable of protecting the entire New York City may cost twice as much on its own,[32] and the global costs of adaptation to sea level rise caused by the glaciers' collapse are estimated to reach $40 billion annually:[30][31] The authors also suggested that their proposal would be competitive with the other "climate engineering" proposals like stratospheric aerosol injection (SAI) or carbon dioxide removal (CDR), as while those would stop a much larger spectrum of climate change impacts, their estimated annual costs range from $7–70 billion for SAI to $160–4500 billion for CDR powerful enough to help meet the 1.5 °C (2.7 °F) Paris Agreement target.[30][31]

History of fieldwork

On the ice

Seismic surveying on Pine Island Glacier
Birth of an iceberg.

Due to the remoteness of Pine Island Glacier, most of the information available on the ice stream comes from airborne[2] or satellite-based measurements.[5][7]

The first expedition to visit the ice stream was a United States over-snow traverse, which spent around a week in the area of PIG during January 1961. They dug snow pits to measure snow accumulation and carried out seismic surveys to measure ice thickness. One of the scientists on this traverse was Charles R. Bentley,[33] who said "we didn't know we were crossing a glacier at the time." PIG is around 50 km (31 mi) wide at the point visited and at ground level cannot be visually distinguished from the surrounding ice. This expedition was called the "Ellsworth Highland Traverse".[34][35]

In the 2004–2005 field season a team of nine, using a British Antarctic Survey (BAS) Twin Otter aircraft equipped with ice-penetrating radar, completed an aerial survey of PIG and its adjacent ice sheet. The team of seven British and two Americans flew 30 km grid patterns over the PIG until January 5, mapping the sub-glacial terrain of an area roughly the size of Nevada.

Due to the remoteness of PIG and the logistical difficulties of caching enough fuel for the 2004–05 expedition and future project(s), BAS used the resources of the United States Antarctic Program (USAP) and their ski-equipped LC130 aircraft. After many weeks of weather delays the first four men arrived from McMurdo Station on 9 November 2004, and began to establish camp and build a skiway for the C130s. The remaining members of the team arrived from Rothera Research Station 10 days later in a Twin Otter.

Because of unusually good weather in the area that season the survey completed flying their grids by mid-January, and began flying 15 km grids of Thwaites Glacier for a USAP expedition who had been experiencing unusually poor weather in their area that year. Flying over Antarctica's Pine Island Glacier on October 14, 2011, in a DC-8 research plane, scientists participating in NASA's IceBridge mission discovered a massive crack running about 29 kilometers (18 mi) across the glacier's floating tongue. The rift is 80 metres (260 feet) wide on average and 50 to 60 meters (160 to 200 ft) deep.

Another team from the British Antarctic Survey arrived at the ice stream on 8 December 2006 for the first of two field seasons. In the second field season, they spent three months there from November 2007 to February 2008. Work on the glacier included radar measurements and seismic surveys.[9]

In January 2008 Bob Bindschadler of NASA landed on the floating ice shelf of PIG, the first ever landing on this ice shelf, for a reconnaissance mission to investigate the feasibility of drilling through around 500 m (1,600 ft) of ice, to lower instruments into the ocean cavity below. It was decided that the small crevasse free area was too hard for further landings and so further fieldwork had to be postponed. Therefore, two Global Positioning System (GPS) units and a weather station were positioned as near as possible to PIG.[36]

In the 2011–2012 field season, after five weeks of delays, the camp staff was finally able to establish the Main Camp just before New Year.[37] The following week, Bindschadler and his team were able to arrive. Due to additional weather delays, the helicopters were not able to arrive by the NSF 'drop dead' date and the field season was cancelled.[38] Limited science was still accomplished by the team thanks to a series of flights by KBA back onto the glacier; conditions had changed drastically since the last Twin Otter flights.[39]

The British Antarctic Survey deployed a small team of four during the 2011–12 summer field season to carry out a series of seismic and radar surveys on PIG. They also installed a series of overwintering GPS stations. During the season, a separate BAS team travelled to the field party's location and installed an overwintering autonomous VLF station. This was followed by a radar traverse upstream using snowmobiles. This survey linked previous radar lines.

From the sea

The first ship to reach Pine Island Glacier's ice shelf, in Pine Island Bay, was the USS/USCGC Glacier in 1985. This ship was an icebreaker operated by the U.S. Coast Guard. The mission, known as Deep Freeze, had scientists on board who took sediment samples from the ocean floor.[40]

During the summer field season, over two months from January to February 2009, researchers aboard the U.S. Antarctic Program research vessel Nathaniel B. Palmer reached the ice shelf. This was the second time that the Palmer had successfully made it up to the glacier, the first time being in 1994. In collaboration with the British, the scientists used a robotic submarine to explore the glacier-carved channels on the continental shelf as well as the cavity below the ice shelf and glacier.[41] The submarine, known as Autosub 3, was developed and built at the National Oceanography Centre in the UK. It completed six successful missions, travelling a total of 500 km (310 mi) under the ice shelf.[42] Autosub is able to map the base of the ice shelf as well as the ocean floor and take various measurements and samples of the water on the way. The success of Autosub 3 was particularly notable because its predecessor Autosub 2 was lost beneath the Fimbul Ice Shelf on only its second such mission.[43]

See also

References

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  2. 1 2 3 4 Vaughan, D. G.; Corr, H. F. J.; Ferraccioli, F.; Frearson, N.; O'Hare, A.; Mach, D.; Holt, J. W.; Blankenship, D. D.; Morse, D. L.; Young, D.A. (2006). "New boundary conditions for the West Antarctic ice sheet: Subglacial topography beneath Pine Island Glacier" (PDF). Geophysical Research Letters. 33 (9): L09501. Bibcode:2006GeoRL..3309501V. doi:10.1029/2005GL025588. S2CID 128406976.
  3. ↑ "History Repeating Itself at Antarctica's Fastest-Melting Glacier". LiveScience. 2014.
  4. 1 2 Payne, A. J.; Vieli, A.; Shepherd, A. P.; Wingham, D. J.; Rignot, E. (2004). "Recent dramatic thinning of largest West Antarctic ice stream triggered by oceans". Geophysical Research Letters. 31 (23): L23401. Bibcode:2004GeoRL..3123401P. CiteSeerX 10.1.1.1001.6901. doi:10.1029/2004GL021284. S2CID 4891690.
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  15. ↑ Dutrieux, P.; De Rydt, J.; Holland, P. R.; Ha, H. K.; Lee, S. H.; Steig, E. J.; Ding, Q.; Abrahamsen, E. P.; Schoder, M. (2014). "Strong Sensitivity of Pine Island Ice-Shelf Melting to Climatic Variability". Science. 343 (6167): 174–178. Bibcode:2014Sci...343..174D. doi:10.1126/science.1244341. PMID 24385606. S2CID 8014155.
  16. ↑ Mouginot, J.; Rignot, E.; Scheuchl, B. (2014). "Sustained increase in ice discharge from the Amundsen Sea Embayment, West Antarctica, from 1973 to 2013". Geophysical Research Letters. 41 (5): 1576–1584. Bibcode:2014GeoRL..41.1576M. doi:10.1002/2013GL059069.
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  19. ↑ Thoma, M.; Jenkins, A.; Holland, D.; Jacobs, S. (2008). "Modelling Circumpolar Deep Water intrusions on the Amundsen Sea continental shelf, Antarctica" (PDF). Geophysical Research Letters. 35 (18): L18602. Bibcode:2008GeoRL..3518602T. doi:10.1029/2008GL034939. S2CID 55937812.
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  29. ↑ Wolovick, Michael J.; Moore, John C. (20 September 2018). "Stopping the flood: could we use targeted geoengineering to mitigate sea level rise?". The Cryosphere. 12 (9): 2955–2967. Bibcode:2018TCry...12.2955W. doi:10.5194/tc-12-2955-2018. S2CID 52969664.
  30. 1 2 3 4 5 6 Wolovick, Michael; Moore, John; Keefer, Bowie (27 March 2023). "Feasibility of ice sheet conservation using seabed anchored curtains". PNAS Nexus. 2 (3): pgad053. doi:10.1093/pnasnexus/pgad053. PMC 10062297. PMID 37007716.
  31. 1 2 3 4 5 Wolovick, Michael; Moore, John; Keefer, Bowie (27 March 2023). "The potential for stabilizing Amundsen Sea glaciers via underwater curtains". PNAS Nexus. 2 (4): pgad103. doi:10.1093/pnasnexus/pgad103. PMC 10118300. PMID 37091546.
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