For the 28th consecutive summer the first three weeks of August were spent observing North Cascade glaciers. The 2011 season exhibited unusual snowpack levels second only to 1999 in the last 28 years. In 1999 the world record annual snowfall record was set at Mount Baker, one of our key field research areas. The difference this year was that it was not the winter snowfall that was extraordinary it was the lack of melt through the spring and early summer. A comparison of snowpack at two USDA Snotel long term sites in the North Cascades illustrates that the bright green 2011 on April 1 was ordinary, and that the dark blue 1999 snowpack level was not approached until early June.
Below is a visual look at the field season in a video followed by detailed description of field results, obtained by Ian Delaney, Mariève Desjardins, Tom Hammond, Ben Pelto, Jill Pelto and Mauri Pelto.
The field season began at Columbia Glacier. This is the lowest elevation large glacier in the North Cascades. Enroute to the glacier we probed our way across the still largely frozen Blanca Lake. In the afternoon slush we forded the outlet stream instead. The glacier was 100% snowcovered average snowdepth was just over 5 meters from extensive probing on the glacier. Snow depth in 2009 and 2010 had been nearly identical in early August, this year the depths were consistently 3.8 meters deeper. 
The hike in to Lower Curtis Glacier was on snow as was our camp. A climax avalanche descended from the north side of the valley in two locations enroute to the glacier. The steep terminus of this glacier was exposed. The terminus was easier to explore with snowpack below it, a retreat of 8 meters had occurred since the previous August, all of it late last summer. 
The glacier had an average snowpack of just over 5 m, 3.6 meters more than last summer. The next field area was Easton Glacier and Squak Glacier. We measured the snowpack on both. We found 3.5 meters of snowpack at 6000 feet, where normally it is blue ice and at 6600 feet the average snow depth was 4.75 meters. The measurements were almost all made using crevasse stratigraphy as probing more than 4 meters is difficult. Both termini were buried. On 
Deming Glacier a new hole had emerged at the base of the icefall on the east side, matching the hole that developed and expanded on the right side (note arrow in top image). We also collected ice worms for an anti-freeze protein project at Queens University, Kingston Ontario (Peter Davies and Mariève Desjardins).
These anti-freeze proteins help keep organisms from freezing solid, by coalescing around ice crystals and limiting their expansion in part due to lowering the freezing point without altering the melting point. For us they could be a critical resource in surgical transplant procedures where keeping organs cold is important. We could have used some kind of protein to keep us warm on the four chilly-cloudy but dry days on the Easton Glacier. We visited Lyman Glacier ascending the former Spider Glacier valley, which was this summer of course still snow filled. Lyman Glacier has lost some of its splendor in the last three years. It had a high ice cliff in 2008 and 2009, measured at 18 meters that has now diminished to 8 meters The glacier has gone from an average surface slope of 12 degrees in 1986 to 18 degrees in 2008 to 21 degrees in 2011, as it continues a rapid ice loss. The steepening results from more rapid thinning at the terminus and overall glacier shortening as the 10 meter per year retreat continues. On Mount Daniels snowpack was not as extraordinary as at other locations. Snowpack on Ice Worm Glacier averaged 4.6 meters, and on Lynch and Daniels Glacier 4.3 and 4.6 meters respectively, this was 2.5 meters more than average. This area had significantly less above average snowfall than the other field areas. Pea Soup Lake at the base of Lynch was still ice covered. We ascended the Lynch over the bergshrund pictured in last image below with a snow depth from the winter of 6.7 meters.
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The mass balance of North Cascade glaciers will be strongly positive in 2011. We normally take 1100-1300 snow depth measurements. This year the deeper snowpack limited out measurements to 1/3 this total. Each glacier will be checked again in one month, to assess the final mass balance.
Author: mspelto
Professor of Environmental Science at Nichols College in Massachusetts since 1989. Glaciologist directing the North Cascade Glacier Climate Project since 1984. This project monitors the mass balance and behavior of more glaciers than any other in North America
Nordenskjöld Coast Glacier Retreat, Antarctic Peninsula
A recent paper by Shuman et al (2011) in the Journal of Glaciology examined the thinning and retreat of glaciers feeding the area that used to contain Larsen Ice Shelf B and the southern end of Larsen Ice Shelf A. They found that the thinning of over 80 meters occurred over large areas of Hektoria, Jorum, Evans, Crane and Green Glaciers. Terminus retreat of five kilometers of the primary glaciers from late 2002-2009 occurred for Larsen B. The rapid loss of thickness and retreat has accompanied the expected and observed acceleration of the glaciers after ice shelf loss. The removal of an ice shelf is a substantial reduction in the backforce on a feeder glacier, or like taking off the brakes. Pine Island Glacier is another example where this is of concern. The Shuman et al (2011) paper particularly the figures are compelling and prompted me to take a look at one embayment in the Larsen A region that is experiencing ongoing glacier retreat. The area has been mapped by USGS and is referred to as the Nordenskjöld Coast. 
We will look at the unnamed embayment marked B, between Drygalski and Dinsmoor Glacier. This embayment which has formed in the last decade is 25 square kilometers in area.The above map indicates the extensive retreat due to the Larsen A ice Shelf loss that took place in the mid-1990’s and the development of the embayment by 2009. The five glaciers that feed it flow from the center of the Antarctic Peninsula, upper left in the image below. 
. The embayment itself has numerous icebergs suggesting the rapid ice discharge from the glaciers feeding this bay. 
This bay has been ice covered for a long time, transitioning from a grounded ice sheet to an ice shelf environment 10,700 years ago, and which has persisted since (Brachfield et al, 2003). The embayment did not expanded notably from the Landsat imagery from 2001 to 2009, as seen in the 2001 Landsat
. In 2011 the retreat was significant as seen in MODIS imagery from Jan.27 the embayment has developed two lobes (note black arrows in image below.. The southern lobe has expanded by 1.5 km. The northern lobe by a smaller amount, but the area between glacier 4 and 5 is now a headland, indicating at least 500 meters of retreat.
. The glaciers in this bay do not appear to have large floating sections generating tabular icebergs at this point, such as are evident on Fleming Glacier.
Grande Motte, Pramort Glacier Retreat and the Tignes Ski area, France
The Tignes ski area in France is famous for its great summer glacier skiing. The portion of the area that is generally open from early June to early September is on the Grand Motte Glacier
. A webcam view for the glacier indicates that on Aug. 20th there is limited snowcover on the glacier, note the 3100 meter camera view, and the ski season will likely be cut short a bit. The bottom of the lift is at 3000 meters and the top of the lift is at 3450 meters. This webcam even has the ability to look back at archive coverage. To protect the ski season on the Grand Motte Glacier the resort has adopted the use of snow guns at the bottom of the Grande Motte Glacier lift. This is similar to the strategy on Pitzal Glacier. A look at the Grande Motte Glacier (Point A) and two neighboring glaciers indicates the issue. 
The terminus of Grande Motte Glacier at 2700 meters, top image, is thin and uncrevassed, indicating retreat will continue. In 2011 as in most years the majority of the glacier has lost its snowcover. This indicates a negative mass balance and continued glacier loss. The neighboring unnamed glacier, labelled B, is completely bare of snow in the Google Earth imagery, is quite thin and uncrevassed. This glacier has separated into three parts, the largest is labelled and is still 500 meters wide and 400 meters long, it will still melt away in the coming decade. The Parmort Glacier, Point C, used to be connected to the Grande Motte Glacier and the Premou Glacier. It is now a 1 km long debris covered stagnant terminus tongue ranging from 2700 meters to 2400 meters. This glacier has no snowcover at the end of most summer and is melting away. There are several areas of concentric crevasses that indicate basins beneath the glacier that periodicially fill with water lifting the glacier a bit, then drain, leading to the crevasses. 
The glaciated landscape in this area is changing dramatically(Gardent and Deline, 2011) noted a 30% loss in glacier area since the 1960’s. This trend is following the behavior of Glacier D’Argentiere and Mer De Glace. Those larger glaciers are not currently threatened, as these are with melting away.
28th Field Season of the North Cascade Glacier Climate Project 8-1 to 8-20
During the interval of 8-1 to 8-20 there will be no blog updates, we will be in the field for the entire period. This is the 28th consecutive year we will monitoring the terminus behavior and mass balance of these glaciers identifying how they respond to climate change. In these 28 years all the glaciers have retreated significantly they have lost 20% of their volume and two of the glaciers we monitored every year have disappeared.
If you are in need of glacier observations, please take a look back at the index of 100+ posts to date
Or look at the video footage below from the 2010 field season and the 2009 field season
North Cascades Glacier Documentary Promo 2010 from Cory Kelley on Vimeo.
2009 field season video
We begin the field season on Columbia Glacier near Monte Cristo, WA. 
We will then head north to the Lower Curtis Glacier on Mount Shuksan. 
A traverse west will takes us to Sholes and Rainbow Glacier on the ne side of Mount Baker.
We will then drive around Mount Baker and examine the Easton, Deming, Squak, Talum and Boulder Glaciers on the south and east side of Mount Baker.
We then head to Cache Col Glacier near Cascade Pass and finally south to Mount Daniels for Ice Worm, Daniels and Lynch Glacierto finish the field season. It was a historically cool and wet spring and the glaciers still have a thick blanket of snowcover. How thick is what we will be measuring one glacier at a time. 
Umiamako Glacier Acceleration and Retreat
Draining the West side of the Greenland Ice Sheet just north of Disko Island, Umiamako Glacier unlike most of the others in the region reaches close to the end of its fjord. The glacier flows 50 km down this fjord, though in the last 10 years this distance has decline sharply. 
A recent paper by McFadden et al (2011) explores the dynamic changes of this glacier. The glacier was first chosen for examination in the late 1930’s by the British West Greenland Expedition. The first good data on velocity come from the survey of Carbonell and Bauer in 1964, who reported a velocity of 1200-1900 meters per year. The terminus and the velocity of the glacier both were pretty stable for the next 40 years, much as was the case on the Jakobshavn to the south. In the McFadden et al (2011) paper the velocity is still in the same range of 1500 meters per year until 2005, top box in image below. From 2005 to 2009 the velocity increased to 5000 meters per year. The associated retreat is in the middle box of this image. The extent of the acceleration inland is not identified here directly, but in the surface profiles the bottom of the three boxes in the McFadden image, the inland thinning in 2008 is significant to 20 km inland, suggesting an acceleration to here. The fjord reach of the glacier still extends another 25-30 km, so the acceleration has not reached to the inland ice. In the Joughin et al (2010), second figure below,the extent of high velocity is quite limited for Umiamako compared to Rinks just to the south inn 2005/06. Is this still true? 
After the retreat of 2003-2005 the acceleration began. This is typical for the marine terminating outlet glaciers as thinning usually leads to retreat and the thinning leads to decoupling of the glacier to extent from the fjord walls and its bed. This typifies the third type of Greenland glaciers reviewed by Bailey and Pelto (2011). The reduced frictional forces lead to acceleration and further retreat. In this case the fjord is longer than many in the sector of West Greenland, leading to a smaller area of contribution from the inland ice and less capability to drawdown this ice. The terminus change can be seen in the map from McFadden , but also in the three images below, first from Google Earth in 2004( top image), than from MODIS in 2010 (middle image)and 2011(bottom image). C marks the terminus position, B the juncture with the first southerly tributary glacier and A the juncture with the second tributary glacier. The two tributary glaciers that clearly feed the glacier in 2004, B now enters the fjord below the glacier and A is right at the terminus. In the McFadden image the 2009 terminus is still downstream of tributary A. Total retreat in the last decade is at least 7.5 km. Extreme Ice Survey set up a camera at the terminus and has a time sequence from 2008, this same camera location in 2011 would show a much different scene as the glacier has retreated 2 kilometers. 
Sommelier Glacier, France Disappearing
Index list of over 100 glaciers examined to date
The Sommelier Glacier is close up against the France-Italy border. The glacier is on the north side of Punta Sommelier centered on 3000 meters. The glacier has retreated 1800 meters from its Little Ice Age Maximum and is currently 600 meters long. 
The most notable aspect of the glacier today is its thin nature and the fact that there are three separated and stagnant ice masses (B, C), the main glacier section is outlined in blue. The large deglaciated fluted moraine is noted by point A. 
Within the area of the main glacier there are several rock outcrops protruding indicating the thin and decaying nature of the glacier, note blue placemarks. Also note that the glacier has limited snowcover. Both of these indicate a glacier is not forecast to survive. 
This is not surprising for the Sommelier Glacier given the fate of the nearby Galambra Glacier noted by the Italian Glacier Commission, inn this photo pair from 1954 and 2009. This glacier no longer graces the slopes of Punta Galambra. Punta Sommelier likewise will lose its glacier cover. This is the trend of alpine glaciers in Italy, other examples include Dosde Glacier, Italy and Presena Glacier.
Mazama Glacier Retreat, North Cascades, Washington
Mazama Glacier flows down the north side of Mount Baker, a strato volcano in the North Cascades of Washington. The glacier begins at the summit plateau, 3260 meters, and terminates at the head of Wells Creek 1470 meters. This is a glacier we visit briefly each summer since 1984, but is not a focus of detailed observations. In 2010 we descended from its divide with Rainbow Glacier at 2100 meters to just above the terminus. 
In the 1970’s the USGS map (top image in sequence) indicates the terminus extended down valley to 1200 meters, this was after a period of advance for the glacier. The glacier advance 450 meters from 1950-1980 (Pelto and Hedlund, 2001). In 1987 we observed the glacier to have begun to retreat. By 1993 the glacier had retreated 200 meters. From 1993 (middle) to 2009 (bottom image) the glacier retreated an additional 750 meters. The rate of retreat has been higher for this glacier because of the loss of the low elevation debris covered terminus that had existed from the 1950’s-1990’s. 
The glacier is still heavily crevassed and active. The retreat will continue as indicated by thinning near the snowline of the glacier from 1993 to 2009. Note the expansion of the rock outcrop in glacier center (A) from the top image, 1993 to 2009 bottom image. There is also considerably less crevassing near Point A. Also note the stranded glacier ice at Point B and C in 2009. This loss has been due to 7 of the last 10 years having a snowline that rose above the elevation necessary for equilibrium. In 2009 at the end of the summer just 36% of the glacier was snowcovered, 65% needs to be snowcovered for equilibrium. 
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In two weeks we will be visiting Mazama Glacier again. Given the heavy 2011 snowpack it is unlikely we will get to see the terminus which should be under avalanche debris.
Retreat of Hansbreen, Svalbard
Hansbreen is tidewater glacier flowing into Hornsund in sw Svalbard. 
The glacier has been examined in detail over the last twenty years from the Polish Research Station. The glacier has retreated 2.7 kilometers from 1900 to 2008. The chart below from Oerlemans, Jania and Kolandara (2011) illustrates this retreat as does the comparative images from the Polish Research Station. 
The glacier mass balance has been measured since 1989 and is submitted to the World Glacier Monitoring Service. In a detailed review of this calving glacier Oerlemans, Jania and Kolandra (2011) report that The average surface mass balance has been -0.36 meters per year, but this is equaled by the calving loss, leading to a loss of 0.8 meters per year. The low slope of this glacier 1.6 degrees makes it difficult to reestablish equilibrium as it retreats. The bed of the glacier remains below sea level for at least 70% of its length, note Figure 3 in Oerlemans et al (2011). The glacier retreated 400 meters from 2000-2005, and has continued this rate of recession. In the two side by side Landsat images below from 2001 (right) and 2010 (left) changes are evident at the front of the neighboring Paierbreen-circle, Hansbreen (H) and Nannbreen (A)
Focusing just on the Hansbreen a red line from the summit of two adjacent mountains is added to the 2001 and 2010 image to illustrate the terminus change. The 2001 images is on top, 2010 image below. 
Retreat of Nannbreen, Svalbard
Nannbreen is a 5 km long land terminating glacier in southwest Svalbard. The glacier is just north of Hornsund. 
During the course of the 20th century Nannbreen retreated from its Little Ice Age moraine complex forming a new proglacial lake. The glacier ends at an elevation of 150 meters descending from 600 meters, the snowline in several Landsat images from the last decade has been 400-450 meters. 
By 2000 (first image below)the glacier had retreated 750 meters from the moraine complex and the glacier ended in a lake, that was over 500 meters long. In 2010 (second image below) the glacier had retreated out of the lake, 250 meters of retreat in 10 years, 1000 meters of retreat in the last century. Certainly the 21st century retreat rate is far above the average 20th century retreat rate. 
Most of the large glaciers in Svalbard are tidewater calving glaciers, such as the nearby Hansbreen, which retreated 400 meters from 2000-2005. Svalbard glaciers have been losing considerable volume, indicative of negative mass balance and glacier retreat. Nuth et al (2010) concluded that over the past 40 years for Svalbard ice loss is 9.71 ± 0.55 cubic kilometers/year. This is an average thinning of 0.36 meters/year for an annual contribution to global sea level rise of 0.026 mm yr.
Chüebodengletscher and Ghiacciaio del Pizzo Rotondo, Switzerland nearly gone
Chüebodenhorn is 3,070 meter high in the Lepontine Alps. The Ghiacciaio del Pizzo Rotondo lies at the foot of its north face and Chüebodengletscher is on its south side. Chüebodengletscher is confined to a small cirque, and currently ends in a lake . 
In several recent years including 2010 the glacier lost all of its snowcover. The glacier is currently 500 meters long and has an elevation range of 75 meters. The lake which fringes the glacier will turn into a circular alpine lake as the glacier melts away
. At present the crescent shaped lake is 140 meters wide. The annual layers in this glacier are evident much like tree rings, that the are all emergent at the surface indicates that all the snow and firn that is supposed to cover most of a glacier at the end of the summer, has been lost from all of the glacier. There are at least 75 annual layers evident. The youngest layer (y) is at the top of the glacier and oldest (o) at the bottom. 
Ghiacciaio del Pizzo Rotondo is a thin slope glacier. This glacier also has a short elevation span of 80 meters from the terminus to its head in a distance of 500 meters. The glacier is a slope glacier that has little apparent thickness. The glacier will be lost faster than the thicker Chüebodengletscher.
Ghiacciaio del Pizzo Rotondo also has lost all of its snowcover, and without a persistent and consistent accumulation zone it cannot survive. These two glaciers are losing mass like many neighboring such as the large Gries Glacier monitored by the In the graph below From the Swiss Glacier Monitoring Network the cumulative mass loss of Gries Glacier has been 20 meters. Swiss Glacier Monitoring Network.
This mass loss of Swiss Glaciers led to 86 of the 95 glacier observed to retreat, while six were stationary and three advanced. The lack of an accumulation zone indicates that the glaciers will follow the path of Presena Glacier and Dosde Glacier unlike Oberaar Glacier which retains an accumulation zone.
Spectacular Retreat of Melbern Glacier, British Columbia
The combined Melbern and Grand Pacific Glacier with a length of 55 km and width of 2-5 km, is a large valley glacier draining from the Saint Elias Mountains near the British Columbia-Alaska boundary. The glacier separates into two distinct glacier termini at Grand Pacific Pass. One of the tongues, Melbern Glacier, flows 20 km northwest ending in . Grand Pacific Glacier flows southeast to Tarr Inlet of Glacier Bay, just across the Alaska boundary. The Melbern Glacier turns north and ends in Lake Melbern. Lake Melbern began to form around 1979 as noted by Clague and Evans (1994). By 1986 the lake had expanded greatly as the former tributary to Melbern Glacier, Konamoxt Glacier had separated, and a 7km retreat of Melbern Glacier from the Konamoxt Glacier had ensued, first image from their paper. Clague and Evansin the second image further note that the ice dam of the Konamoxt Glacier that blocks Melbern Lake had broken by 1991 and the lake level had dropped. 
The retreat has continued unabated up through 2009. Here we use a series of Landsat images and one Google Earth Image to illustrate the retreat up to 2013. The first is a 1986 Landsat Image, K=Konamoxt and M=Melbern. In this image Konamoxt still blocks Melbern Lake and Melbern Glacier terminates adjacent to another tributary from the south, orange marks the 1986 terminus of both glaciers. The second image is a false color Landsat image from 2001. Konamoxt Glacier extends partly across the lake but not completely. The lake to the northwest of Konamoxt is filled with icebergs. Melbern Glacier has retreated 3 km since 1986. The third image is the Google Earth image also from 2001 showing the 1986 margin as well, in orange and the 2007 terminus in purple. The fourth image is from 2007, indicating a 1.5 km retreat of Melbern Glacier in the last six years. By 2013 the retreat is 2.25 km since 2001 and 5.25 km since 1986. Konamoxt Glacier no longer reaches Lake Melbern proper and is beginning a retreat up its own valley. The lake itself has changed color and lost its fleet of icebergs. The last image is from July 2013 and Lake Melbern is now 20 km long and still expanding. 
Melbern Glacier is following the same pattern as nearby Yakutat Glacier and Grand Plateau Glacier. The lower 3 km of the glacier appears stagnant. However, there is a moraine band 10m km above the terminus that has shifted down glacier 1000-1500 meters from 2001 to 2007 as seen in images from those dates below. The green line indicates the moraine position in 2007. This indicates significant flow at this point. Thus, it is evident that retreat will continue on Melbern Glacier, but should slow as either the lake basin is left behind, or the moraine band is approached 
BAMS State of Climate 2010-Glacier Chapter
STATE OF THE
CLIMATE IN
2010 Published June 2011
Below is the chapter that I author on Alpine glacier and ice sheets. The full BAMS report is an invaluable resource for understanding the climate of 2010 and how it fits into the context of climate change and recent climate. The editorial process is rigorous. The picture below is of Lemon Creek Glacier in Alaska, one of the glaciers discussed. 
g. Land surface properties
1) Alpine glaciers and ice sheets—M. S. Pelto
The World Glacier Monitoring Service (WGMS) record of mass balance and terminus behavior(WGMS 2008; WGMS 2009) provides a global index for alpine glacier behavior. Mass balance was negative in 2009 for the 19th consecutive year. Preliminary data for 2010 from Austria, Greenland, Italy, Norway,New Zealand, and the United States indicate it is highly likely that 2010 will be the 20th consecutive year of negative annual balances. Alpine glaciers have been studied as sensitive indicators of climate for more than a century, most commonly focusing on changes in terminus position and mass balance (Oerlemans 1994). The worldwide retreat of mountain glaciers is one of the clearest signalsof ongoing climate change (Haeberli et al. 2000). The retreat is a reflection of strongly negative mass balances over the last 30 years (WGMS 2008). Glacier mass balance is the difference between accumulation and ablation. A glacier with a sustained negative balance is out of equilibrium and will retreat. The recent rapid retreat has led to some glaciers disappearing (Pelto 2010).
The cumulative mass balance loss of the last 30 years is 12.3 m w.e., the equivalent of cutting a 14 m thick slice off the top of the average glacier (Fig. 2.60). The trend is remarkably consistent from region to region (WGMS 2009). WGMS mass balance results based on 30 reference glaciers with 30 years of record are not appreciably different from the results for all reporting glaciers. The decadal mean annual mass balance was -198 mm in the 1980s, -382 mm in the 1990s, and -654 mm for 2000–09. The declining mass balance trend during a period of retreat indicates alpine glaciers are not approaching equilibrium and retreat will continue to be the dominant terminus response.
In 2010 winter accumulation on Austrian and Italian glaciers was about average, and summer temperature was above the mean in 2010. The result was mass losses on glaciers in the Alps: Sonnblickkees, Austria, -790 mm; Ciardoney, Italy, -830 mm; and Fontana Bianca, Italy, -130 mm. The Swiss Glacier Monitoring Network reported that in 2010 the termini of 86 glaciers were in retreat, six were stationary, and three advanced. In Norway, terminus fluctuation data from 30 glaciers for 2010 indicate 27 retreating, one stable, and two advancing. The average terminus change was -17 m, compared to -183 m in 2009. Mass balance surveys found deficits on all Norwegian glaciers. Winter 2009/10 was cold but with little snow on the glaciers, 50%–80% of the long-term normal. Summer was warmer than normal in the south and a bit colder than normal in the north. (L. Andreasson 2011, personal communication).
In the North Cascades, Washington (M. Pelto 2011, personal communication), a transition from El Niño to La Niña conditions led to equilibrium mass balances. El Niño winter conditions led to reduced winter snowfall. La Niña conditions developed by summer causing low summer melting, which offset the low accumulation. The result was positive annual balance on four glaciers, negative balance on five glaciers, and an equilibrium balance on one glacier. All 33 glaciers observed retreated in 2010. In southeast Alaska, snowlines were 50 m above average on Lemon Creek and Taku Glacier of the Juneau Icefield indicative of moderate negative balances. In New Zealand, El Niño led to normal to below normal temperatures through summer and into fall 2010, leading to snowlines in a near steady state (J.Hendrikx 2011, personal communication). On 50 glaciers surveyed, the average snowline was at the equilibrium snowline elevation, after two strongly negative years in 2008 and 2009.
For information on 2010 ice melt on the Greenland ice sheet and in Antarctica please refer to sections 5f and 6e, respectively.
Fig. 2.60. The (top) annual mean and cumulative annual mean balance and (bottom) decadal mean cumulative
specific mass balance (mm w.e.) reported for the 30 reference glaciers to the WGMS.
From a Glaciers Perspective 