Glacier mass balance

July 16, 2012, 9:54 pm
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Glacier Mass Balance

Crucial to the survival of a glacier is its mass balance, the difference between accumulation and ablation (melting and sublimation). The two zones are separated by the snowline, which at the end of the summer is the annual equilibrium line. Climate change may cause variations in both temperature and snowfall, causing changes in mass balance. Changes in mass balance control a glacier's long term behavior and are the most sensitive climate indicator on a glacier.

A glacier with a sustained negative balance is out of equilibrium and will retreat, while one with a sustained positive balance is out of equilibrium and will advance. Glacier retreat results in the loss of the low elevation region of the glacier. Since higher elevations are cooler than lower ones, the disappearance of the lowest portion of the glacier reduces overall ablation, thereby increasing mass balance and potentially reestablishing equilibrium. However, if the mass balance of a significant portion of the accumulation zone of the glacier is negative, it is in disequilibrium with the local climate. Such a glacier will melt away with a continuation of this local climate. [1]

 

caption Lemon Creek Glacier

 

The key symptom of a glacier in disequilibrium is thinning along the entire length of the glacier.[2][3].  For example, Lemon Creek Glacier will likely shrink to half its size, but at a slowing rate of reduction, and stabilize at that size, despite the warmer temperature, over a few decades. However, the Grinnell Glacier will shrink at an increasing rate until it disappears. The difference is that the upper section of Lemon Creek Glacier remains healthy and snow-covered, while even the upper section of the Grinnell Glacier is bare, melting and has thinned. Small glaciers with shallow slopes such as Grinnell are most likely to fall into disequilibrium if there is a change in the local climate.

 

caption Grinnell Glacier

 

In the case of positive mass balance, the glacier will continue to advance expanding its low elevation area, resulting in more melting. If this still does not create an equilibrium balance the glacier will continue to advance. If a glacier is near a large body of water, especially an ocean, the glacier may advance until iceberg calving losses bring about equilibrium.

Measurement methods

Mass balance

 

caption glacier cravasse

 

Mass balance is measured by determining the amount of snow accumulated during winter, and later measuring the amount of snow and ice removed by melting in the summer. The difference between these two parameters is the mass balance. If the amount of snow accumulated during the winter is larger than the amount of melted snow and ice during the summer, the mass balance is positive and the glacier has increased in volume. On the other hand, if the melting of snow and ice during the summer is larger than the supply of snow in the winter, the mass balance is negative and the glacier volume decreases. Mass balance is reported in meters of water equivalent. This represents the average thickness gained (positive balance) or lost (negative balance) from the glacier during that particular year.

 

caption snowpit

 

To determine mass balance in the accumulation zone, snowpack depth is measured using probing, snowpits or [[crevasse stratigraphy]]. Crevasse stratigraphy makes use of annual layers revealed on the wall of a crevasse[4]. Akin to tree rings, these layers are due to summer dust deposition and other seasonal effects. The advantage of crevasse stratigraphy is that is provides a two-dimensional measurement of the snowpack layer, not a point measurement. It is also usable in depths where probing or snowpits are not feasible. In temperate glaciers, the insertion resistance of a probe increases abruptly when its tip reaches ice that was formed the previous year. The probe depth is a measure of the net accumulation above that layer. Snowpits dug through the past winter's residual snowpack are used to determine the snowpack depth and density. The snowpack's mass balance is the product of density and depth. Regardless of depth measurement technique, the observed depth is multiplied by the snowpack density to determine the accumulation in water equivalent. It is necessary to measure the density in the spring as snowpack density varies. Measurements of snowpack density completed at the end of the ablation season yield consistent values for a particular area on temperate alpine glaciers and need not be measured every year. In the ablation zone, ablation measurements are made using stakes inserted vertically into the glacier either at the end of the previous melt season or the beginning of the current one. The length of stake exposed by melting ice is measured at the end of the melt (ablation) season. Most stakes must be replaced each year or even mid-way through the summer.

 

Net balance

Net balance is the mass balance determined between successive mass balance minimums. This is the stratigraphic method focusing on the minima representing a stratigraphic horizon. In the northern mid-latitudes, a glacier's year follows the hydrologic year, starting and ending near the beginning of October. The mass balance minimum is the end of the melt season. The net balance is then the sum of the observed winter balance (bw) normally measured in April or May and summer balance (bs) measured in September or early October.

Annual balance

Annual balance is the mass balance measured between specific dates. The mass balance is measured on the fixed date each year, again sometime near the start of October in the mid northern latitudes.[5]

Geodetic methods

Geodetic methods are an indirect method for the determination of mass balance of glacier. Maps of a glacier made at two different points in time can be compared and the difference in glacier thickness observed used to determine the mass balance over a span of years. This is best accomplished today using [[Differential Global Positioning System]]. Sometimes the earliest data for the glacier surface profiles is from images that are used to make topographical maps and digital elevation models. Aerial mapping or [[photogrammetry]] is now used to cover larger glaciers and icecaps such as those occuring in [[Antarctica]] and [[Greenland]], however, because of the problems of establishing accurate ground control points in mountainous terrain, and correlating features in snow and where shading is common, elevation errors are typically not less than 10 m (32 ft) [6] Laser altimetry provides a measurement of the elevation of a glacier along a specific path, e.g., the glacier centerline. The difference of two such measurements is the change in thickness, which provides mass balance over the time interval between the measurements. Again this is a good method over a span of time but not for annual change detection. The value of geodetic programs is providing an independent check of traditional mass balance work, by comparing the cumulative changes over ten or more years [7].

Mass balance research worldwide

Mass balance studies have been carried out in various countries worldwide, but have been conducted mostly in the [[Northern Hemisphere]] due to there being more mid-latitude glaciers in that hemisphere. The World Glacier Montioring Service annually compiles the mass balance measurements from around the world. From 2002-2006, continuous data are available for only 7 glaciers in the Southern Hemisphere and 76 glaciers in the Northern Hemisphere.The mean balance of these glaciers was its most negative in any year for 2005/06. [8] The similarity of response of glaciers in western North America indicates the large scale nature of the driving climate change.[9]

Alaska

The [[Taku Glacier]] near [[Juneau, Alaska]] has been studied by the Juneau Icefield Research Program since 1946, and is the longest continuous mass balance study of any glacier in North America. Taku is the world's thickest known temperate alpine glacier, and experienced positive mass balance between the years 1946 and 1988, resulting in a huge advance. The glacier has since been in a negative mass balance state, which may result in a retreat if the current trends continue[10]

Austrian Glacier Mass Balance

The mass balance of Hintereisferner and Kesselwandferner glaciers in [[Austria]] have been continuously monitored since 1952 and 1965 respectively. Having been continuously measured for 55 years, Hintereisferner has one of the longest periods of continuous study of any glacier in the world, based on measured data and a consistent method of evaluation. Currently this measurement network comprises about 10 snow pits and about 50 ablation stakes distributed across the glacier. In terms of the cumulative specific balances, Hintereisferner experienced a net loss of mass between 1952 and 1964, followed by a period of recovery till 1968. Hintereisferner reached an intermittent minimum in 1976, briefly recovered in 1977 and 1978 and has continuously lost mass in the 30 years since then.[11]

 

 

New Zealand

Glacier mass balance studies have been ongoing in [[New Zealand]] glaciers since 1957. [[Tasman Glacier]] has been studied since then by the New Zealand Geological Survey and later by the Ministry of Works, measuring the ice stratigraphy and overall movement. However, even earlier fluctuation patterns were documented on Franz Josef and [[Fox Glacier]]s in 1950. Other glaciers on the South Island studied include Ivory Glacier; since 1968, while on the North Island, glacier retreat and mass balance research has been conducted on the glaciers on Mount Ruapehu since 1955. On Mount Ruapehu, permanent photographic stations allow repeat photography to be used to provide photographic evidence of changes to the glaciers on the mountain over time. [12]

 

North Cascade glacier mass balance program

The North Cascade Glacier Climate Project measures the annual balance of 9 glaciers, more than any other program in North America. These records extend from 1984–2005 and represent the only set of records documenting the mass balance changes of an entire glacier-clad range to monitor an entire glaciated mountain range in North America, which was listed as a high priority of the National Academy of Sciences in 1983. North Cascade glaciers annual balance has averaged ?0.52 m/a from 1984–2005, a cumulative loss of over 12.5 m or 20–40% of their total volume since 1984 due to negative mass balances. The trend in mass balance is becoming more negative, which is fueling more glacier retreat and thinning.[13]

 Norway mass balance program

Norway maintains the most extensive mass balance program in the world and is largely funded by the hydropower industry. Mass balance measurements are currently performed on twelve glaciers in Norway. In southern Norway six of the glaciers have been measured for 42 consecutive years or more, and they constitute a west-east profile reaching from the very maritime Ålfotbreen Glacier, close to the western coast, to the very continental Gråsubreen Glacier, in the eastern part of Jotunheimen. Storbreen Glacier in Jotunheimen has been measured for a longer period of time than any other glacier in Norway, a total of over 55 years, while Engabreen Glacier has the longest series (35 years) in northern Norway. The Norwegian program is where the traditional methods of mass balance measurement were largely derived.[14]

Sweden Storglaciären

The Tarfala Research Station in the Kebnekaise region of northern Sweden is operated by  Stockholm University. It was here that the first mass balance program was initiated immediately after World War II, and continues to the present day. This survey was the initiation of the mass balance record of Storglaciären Glacier, and constitutes the longest continuous study of this type in the world.[15]

 Iceland Glacier mass balance

Glacier mass balance is measured once or twice annually on numerous stakes on the several ice caps in Iceland by the National Energy Authority. Regular pit and stake mass-balance measurements have been carried out on the northern side of Hofsjökull since 1988 and likewise on the Þrándarjökull since 1991. Profiles of mass balance (pit and stake) have been established on the eastern and south-western side of Hofsjökull since 1989. Similar profiles have been assessed on the Tungnaárjökull, Dyngjujökull, Köldukvíslarjökull and Brúarjökull outlet glaciers of Vatnajökull since 1992 and the Eyjabakkajökull outlet glacier since 1991. [16]

Swiss mass balance program

Temporal changes in the spatial distribution of the mass balance result primarily from changes in accumulation and melt along the surface. As a consequence, variations in the mass of glaciers reflect changes in climate and the energy fluxes at the earth's surface. The Swiss glaciers Gries in the central Alps and Silvretta in the eastern Alps, have been measured for many years. The distribution of seasonal accumulation and ablation rates are measured in-situ. Traditional field methods are combined with remote sensing techniques to track changes in mass, geometry and the flow behaviour of the two glaciers. These investigations contribute to the Swiss Glacier Monitoring Network and the International network of the World Glacier Monitoring Service (WGMS) [17]

United States Geological Survey (USGS)

The USGS operates a long-term "benchmark" glacier monitoring program which is used to examine climate change, glacier mass balance, glacier motion, and stream runoff. This program has been ongoing since 1965 and has been examining three glaciers in particular. Gulkana Glacier and Wolverine Glacier in the Coast Ranges of Alaska have both been monitored since 1965, while the South Cascade Glacier in Washington State has been continuously monitored since the International Geophysical Year of 1957. This program monitors one glacier in each of these mountain ranges, collecting detailed data to understand glacier hydrology and glacier climate interactions.[18]

Canada Geological Survey-Glaciology Division (CGS)

CGS is in charge of monitoring the western Canada mass balance network Helm, Place and Peyto Glacier. The Arctic glaciers Baby, Devon and White Glacier. CGS relies on standard stake methods for monitoring the glaciers. Helm Glacier (-33 m) and Place Glacier (-27m) have lost more than 20% of their entire volume, since 1980, Peyto Glacier (-20 m) is close to this amount. The Canadian Arctic White Glacier has not been as negative at (-6 m)since 1980. [19]

 Bolivia mass balance network

The glacier monitoring network in Bolivia, a branch of the glacio-hydrological system of observation installed throughout the tropical Andes mountains by IRD and partners since 1991, has monitored mass balance on Zongo (6000 m asl), Chacaltaya (5400 m asl) and Charquini glaciers (5380 m asl). A system of stakes has been used, with frequent field observations, as often as monthly. These measurements have been made in concert with energy balance to identify the cause of the rapid retreat and mass balance loss of these tropical glaciers. .[20]

 References

  1. ^Dyurgerov, M. (M. Meier and R. Armstrong, eds.). "Glacier mass balance and regime measurements and analysis, 1945–2003". Institute of Arctic and ^Alpine Research, University of Colorado. Distributed by National Snow and Ice Data Center, Boulder, CO..
  2. ^Mauri S. Pelto (Nichols College). "The Disequilibrium of North Cascade, Washington Glaciers 1984–2004". In "Hydrologic Processes". Retrieved on February 14, 2006.
  3. ^Pelto, M.S. and Hartzell, P.L. (2004). "Change in longitudinal profile on three North Cascades glaciers during the last 100 years". Hydrologic Processes 18: 1139–1146. doi:10.1002/hyp.5513. 
  4. ^Mauri S. Pelto, Director NCGCP (March 09). "Glacier Mass Balance". North Cascade Glacier Climate Project.
  5. ^Mauri S. Pelto, Director NCGCP (March 28). "Glacier Mass Balance". North Cascade Glacier Climate Project.
  6. ^David Rippin, Ian Willis, Neil Arnold, Andrew Hodson, John Moore, Jack Kohler and Helgi Bjornsson (2003). "Changes in Geometry and Subglacial Drainage of Midre Lovénbreen, Svalbard, Determined from Digital Elevation Models". Earth Surface Processes and Landforms 28: 273–298. doi:10.1002/esp.485. 
  7. ^Andreas Bauder, G. Hilmar Gudmundsson (March 28). "Mass Balance Determination using Photogrammetric Methods and Numerical Flow Modeling". Laboratory of Hydrolic, Hydrology and Glaciology.
  8. ^"Glacier Mass Balance Bulletin". WGMS. Retrieved on 2008-03-09.
  9. ^Pelto, Mauri. "Western North American Glacier Mass Balance 1984-2005, Equilibrium or Disequilibrium Response?". North Cascade Glacier Climate Project. Retrieved on 2008-03-09.
  10. ^Pelto, Mauri; Matt Beedle, Maynard M. Miller. "Mass Balance Measurements of the Taku Glacier, Juneau Icefield, Alaska 1946-2005". Juneau Icefield Research Program. Retrieved on 2007-01-09.
  11. ^"Mass balance of Hintereisferner". Institute for Meteorology and Geophysics, University of Innsbruck, Austria (January 20, 2004). Retrieved on 2007-01-09.
  12. ^"Glaciers of New Zealand". Satellite Image Atlas of Glaciers of the World. U.S. Geological Survey. Retrieved on 2007-01-16.
  13. ^Pelto, Mauri (November 9, 2006). "Glacier Mass Balance". United States Mass Balance Surveys. Retrieved on 2007-01-09.
  14. ^Norwegian Water Resources and Energy Directorate (March 28). "Mass balance measurements". Glaciological investigations in Norway.
  15. ^"Storglaciären". Stockholm University (February 9, 2003). Retrieved on 2007-01-09.
  16. ^"Iceland". Iceland National Energy Authority (2006). Retrieved on 2008-03-09.
  17. ^Bauder, Andreas; Martin Funk (March 20, 2006). "Mass Balance Studies on Griesgletscher and Silvrettagletscher". The Swiss Glaciers. Laboratory of Hydraulics, Hydrology and Glaciology, Swiss Federal Institute of Technology. Retrieved on 2007-01-09.
  18. ^"Benchmark Glaciers". Water Resources of Alaska-Glacier and Snow Program. United States Geological Survey (July 9, 2004). Retrieved on 2007-01-09.
  19. ^"Canada Glacer Mass Balance Network". National Glaciology Group. Canada Geological Survey (January 14, 2008). Retrieved on 2008-03-09.
  20. ^"Benchmark Glaciers". Institute of Hydraulics and Hydrology of Bolivia. Bernard Francou, Institut de Recherche pour le Développement (IRD (Jan., 2001). Retrieved on 2008-03-09.
 
Glossary

Citation

Pelto, M. (2012). Glacier mass balance. Retrieved from http://www.eoearth.org/view/article/152983

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