Anderson Glacier is the headwaters of the Quinault River in the Olympic Mountains of Washington. A century ago the glacier was 2 km long, and a half kilometer wide. Retreat of this glacier in the first half of the 20th century exposed a new alpine lake, as the glacier retreated 1 kilometer. From 1950-1980 the glacier diminished slowly. From 1959 to 1990 the glacier thinned and retreated from the lake trapped behind the Little Ice Age moraine. The picture below was given to me by Austin Post. 
Since 1990 the glacier has begun to shrink rapidly. The USGS aerial photograph of the glacier is from 1990, Anderson Glacier is on the right, West Glacier is to the left. 
Investigating this glacier in 1992 we measured its area at 0.38 square kilometers, down from 1.15 square kilometers a century before. Ten years later the glacier had diminished to 0.30 square kilometers, but had thinned even more, leaving it poised for a spectacular change, over the next five years. Large outcrops of rock have appeared beginning in 2003 and further exposed in 2005 and 2009 in the middle of the glacier. Note the outcrops in this 2007 image from Kathy Chrestensen 
The end of the glacier is an avalanche runout area and is thinning slower than most of the lower reach of the glacier. This glacier has become a series of small disconnected relict glacier ice patches. There are some large ice caves that have developed under the glacier. This is an indication of limited flow, and stagnant melting ice. 
Anderson Glacier is not the only glacier feeding the Quinault River, all the others are retreating as well. The result of glacier retreat is reduced late summer and early fall streamflow, impacting salmon runs at that time of the year. This is primarily the fall Coho, Chum and Chinook salmon and Steelhead summer run. During the spring and early summer runoff increases as snowmelt still occurs, but is not retained in the glacier system.
Category: Glacier Observations
Post detailing changes in a glacier
Zemestan Glacier, Afghanistan Retreats
The Wakhan Corridor in Afghanistan is not easy to get to, as a result field study of its glaciers are quite limited. This is where the Global land ice Monitoring System (GLIMS) comes in. GLIMS acquires satellite imagery of glaciated areas, making these images available to researchers and processing them to an extent for inventory purposes. GLIMS is led by Jeff Kargel at the University of Arizona. In the Wakhan Corridor a group of glaciers was examined by Umesh Haritashya and others (2009). This recent GLIMS project examined ASTER and Landsat MSS data 1976–2003, in the Wakhan Corridor of Afghanistan. Of the 30 alpine glaciers of varying type, size and orientation examined 28 glacier-terminus positions have retreated, two have been stationary. 
The largest average retreat rate was 36 m per year, and the average retreat was 11 m per year. The retreat is evident in a comparison of 1998 Landsat and 2010 Landsat images, note the orange arrow in both. The width and length of the terminus tongue has changed. One of the glacier examined was the Zemestan Glacier. This glacier is 5.3 kilometers long, has an area of 5.2 square kilometers, begins at 5640 meters and terminates at 4800 meters. It is one of many glacier in the Central area of the Wakhan Corridor. Zemestan Glacier has retreated at a rate of 17 meters per year over the study period, a total retreat of 460 meters, 9% of its total length. A comparison of 1998 and 2010 Landsat imagery indicates the retreat of the terminus tongue in width and length at the orange arrows. 
The glacier has remained snowcovered at its higher elevations at the end of the summer in recent satellite images. 
This indicates that with current climate the glacier does have a significant accumulation zone and can survive current climate. Continued warming will increase the retreat rate and could threaten its survival. The glacier feeds the Pamir River which in turn drains into the Panj River, to the Amu Darya River and then the Aral Sea. The terminus is on a shallow slope lacks a steep slope and is not extensively crevassed. All of these factors indicate retreat will continue. The glacier has little debris cover unlike many glaciers in the Karakoram-Himalaya-Pamir Ranges such as the Khumbu Glacier or the Zemu Glacier 
Helm Glacier Melting Away-2014 Video Update
It is clear that the business model for glaciers in our current climate is not working. The Helm Glacier in the Coast Mountains of southwest British Columbia is an example of this. Helm Glacier has been the focus of annual mass balance surveys since 1967. During the 1984-2013 period its mass balance losses have been the greatest of any of the 16 glaciers monitored in North America. The mass balance loss has been about 32 m of water equivalent, about 35 m of ice thickness lost. This is less than losses on other nearby glaciers like Spearhead Glacier but more than others such as Warren Glacier. The regional volume loss has impacted even the large glaciers Bridge Glacier and small glaciers. The loss is more than 30% of the Helm lost in just 25 years, and the trend mirrors that of all glaciers in the Pacific Northwest. Helm Glacier also fits into the pattern of glacier retreat across Canada, Canadian Glacier Retreat index. 
The glacier had an area of 4.3 square kilometers in 1928. Today the area has declined by 78% to 0.92 square kilometers. In 1928 the glacier is not too distant from its Little Ice Age moraines. The trimlines of recently deglaciated terrain are clear. The glacier has two termini, one draining north and the other west. Today in the picture from Johannes Koch, there is a vast expanse of newly deglaciated terrain that as yet lacks significant vegetation. The western terminus is gone.
Remainder of post and updates moved to
Helm Glacier
Zongo Glacier retreat
Zongo Glacier, Bolivia extends 2.9 km down the south side of Huayna Potosi from 6000 m to 4900 m. Zongo Glacier is a small valley glacier located north-east of La Paz, and its runoff is directed to an important hydraulic power station which supplies La Paz. Note Laguna Zongo in foreground of the first image. The dam is visible as is the power station to the right and below the lake. The glacier has considerable snowcover on its upper section and crevassing. This indicates a persistent accumulation zone. 
In 1991 a glaciological research program (page 46) was established on Zongo Glacier to monitor mass balance, understand its hydrology and energy balance. The long term director of this research Bernard Francou has been called the glacier guardian. The typical Alpine glaciers undergoes a long accumulation period in winter and a short ablation season in summer. The glaciers of the tropical Andes experience snow accumulation during the wet season, austral summer on their upper regions and maximum ablation during the same season low on the glacier. In the dry season winter there is a period of low ablation over the whole glacier. Mean annual air temperature at the long term snowline at 5250 m is -1.5 °C. Mean precipitation is about 0.9 m/year.
Since 1991 the glacier has lost more than 5 m of thickness and has retreated significantly. The mass balance loss has been most pronounced during El Nino periods, thus 2009 should not be a good year for Zongo Glacier. La Nina’s are associated with positive or only slightly negative mass balance. The ongoing mass balance loss has led to retreat of 184 meters of this glacier from 1996-2005. A comparison of satellite images from 2004-2008 indicate a retreat of 70-75 meters, this is consistent with the reported retreat rate of 18 meters per year. The glacier has withdrawn from the new glacier lake formed from the ongoing glacier retreat in the 1990’s. The images below are focussed on the terminus in 2004 and in 2008, note the retreat from the lake shore. 
Zongo Glacier continues to have an accumulation zone, a necessary essential for glacier survival, and unlike the nearby Chacaltaya Glacier which has disappeared in 2009, it will exist for sometime. The Chacaltaya Glacier is a small glacier, like 80% of the glaciers in this region of the Cordillera Real, and its disappearance puts more pressure on the water resources provided by the larger remaining glaciers such as Zongo Glacier.
Khumbu Glacier Decay
The Khumbu Glacier is a large debris-covered glacier in the Khumbu region. It is one of the more famous and often visited Himalayan glaciers as it is the key route for climbing Mount Everest. About 12 km long, it drains mainly from the West Cwm between Mt. Everest and Lhotse and ranges in altitude from over 8000 meters to 4900 m. The equilibrium line separating the region where snow typically persists through the year is 5600 m. Melting is very limited above 5800 m. The famed Khumbu Icefall transitions the glacier from the accumulation zone to the ablation zone. The ablation zone is where melting dominates. Base camp for climbing expeditions is on a debris covered portion of the glacier below the Khumbu Icefall, Pumori Lake is about one mile away. The debris cover is brought down by avalanches and exposed at the surface via melting. In the lower picture it is evident that the lower 10 km of the glacier is dominantly debris covered. 
The Kathmandu-based mountain research institute, ICIMOD, reports that the Khumbu Glacier is retreating at an average of 20m per year. The length of the glacier has shrunk from 12,040m in the 1960s to 11,100m in 2001. This 1 kilometer retreat has been consistently between 15 and 20 m per year during this interval. This retreat is less than nearby Ngozumpa Glacier and Imja Glacier. Everest Base Camp has actually dropped from 5,320m to 5,280m since Hillary and Tenzing first set up camp there more than fifty years ago. This 40 m of thinning at the base camp has occurred over this 55 year period. Base camp is on the right side of the glacier in this view notice the small colored blotches. 
Measurements of velocity on the glacier by Nakawao and others (1999) noted that the Khumbu Glacier near the climbing base camp slowed by 10% between 1958 measurements and 1995 measurements. Kadota and others (2000) surveyed the Khumbu glacier in 1995 and compared the results with those of the 1978 survey. They found that the surface of the glacier lowered about 12-15 meters over most of the length but by only 6-8 meters near the terminus. A recent paper by Bolch et al (2008) compared a Corona DTM 1962 image and the ASTER DTM 2002 of Khumbu, Glacier. During this interval the Khumbu Glacier thinned in the ablation zone by an average of 17 m, This is a rate of 0.4 m/year.
Bolch et al. (2008).
Thinning at base camp of 40 meters is greater than at the terminus. The result is a reduced glacier slope. Reduced slope and thickness both lead to deceleration. The reduced thickness loss at the terminus is due to the debris cover thickness increasing towards the terminus. The same story is playing out on the Satopanth Glacier(Image from Jeff Engels) 
Takeuchi and others (2000) noted that for Khumbu Glacier debris cover less than 5 cm increases ablation, debris greater than 5 cm in thickness reduces ablation. On Khumbu Glacier their ablation measurements indicate that ablation is reduced 40% from that of clean ice when the debris cover is 10 cm thick. Thicker debris cover reduced ablation even more, but only slightly. This is the primary reason why thinning has been less near the terminus.
Naito et al. (2000) developed a model coupling mass balance and flow dynamics of debris covered glaciers and applied it to the Khumbu Glacier. The model predicts formation and enlargement of a depression in the lower ablation area about 5 km upstream of the terminus. This depression could transform into a glacier lake in future. Given the more rapid melting upglacier of the terminus and the low surface slope of this glacier, this is a reasonable result. The movement of the glacier can be tracked by examining the movement of supraglacial lakes downglacier. Below is 4 lakes denoted in a 2003 and 2009 image, the mean movement has been 120 m, 20 meters/year. 
Given the slow rate of retreat and the 3000 m of altitude range above the current snowline the Khumbu Glacier is not in danger of disappearing with current climate. The entire Western Cwm the flat cirque seen beneath Nuptse, Lhotse and Everest here is in the permanent snow zone above 6000 m. The icefall then descends to 5400 m. The terminus is at 4900 m. It is not difficult to imagine this lower section of the glacier below the icefall wasting away. It is likely that a substantial proglacial will develop as is occurring at Ngozumpa Glacier and has occurred at Imja Glacier. 
Kadota, T., K. Seko, T. Aoki, S. Iwata, and S. Yamaguchi. 2000.
Shrinkage of the Khumbu Glacier, east Nepal from 1978 to
1995. IAHS Publ. 264 (Symposium at Seattle 2000 – Debris-
Covered Glaciers), 235–243.
Naito, N., M. Nakawo, T. Kadota and C.F. Raymond. 2000.
Numerical simulation of recent shrinkage of Khumbu Glacier,
Nepal Himalayas. IAHS Publ. 264 (Symposium at Seattle 2000 –
Debris-Covered Glaciers), 245–254.
Nakawo, M., H. Yabuki and A. Sakai. 1999. Characteristics of
Khumbu Glacier, Nepal Himalaya: recent changes in the debriscovered
area. Ann. Glaciol., 28, 118–122.
Tasman Glacier Retreat
Update for 2/22/2011-the Tasman Glacier’s thin and weak terminus area, see in the GE image below, in Tasman Lake shed some large icebergs due to the earthquake generating some substantial waves in the lake. The post earthquake image with numerous fresh icebergs is the second below and is from the EPA. 
No word on the Hooker Glacier in the next valley west, which also calves into an expanding lake or Murchison Glacier in the next valley east. There is a Tasman Glacier update in 2013.
. The New Zealand National Institute of Water and Atmospheric Research has been examining the changes in volume and snowline on New Zealand Glaciers since 1977. This survey has concluded for 2009 they same observation as for 2007 and 2008, the glaciers are shrinking. An examination of the recent volume changes on the glacier indicate that the volume has been particularly negative since 1998.
. This followed a period of relatively positive mass balance from 1990-1997, which made the New Zealand glaciers the least rapidly retreating glaciers in the world. For Tasman Glacier the retreat has been ongoing, the NWIA has noted a retreat of 180 m per year on average since the 1990’s. The proglacial lake at the terminus continues to expand as the glacier retreats upvalley. The lake is deep with most of the lake exceeding 100 metes in depth, and the valley has little gradient, thus the retreat will continue. It has been noted by researchers at Massey University that it is just to warm for the terminus area at 730 m to endure. Imagery of Tasman Glacier indicates the future it faces. There was no lake in 1973 and now it is more than 7 km long. The glacier appears quite rotten along the ice margin and poised for further retreat. The glacier drains a valley just east of the highest mountains in the range Mount Cook and Mount Tasman. 
. The image above has a blue line up the center of the glacier from the former terminus at the end of the lake too the head of the glacier. The upper image is from 2007 and the lower image from 2009. In the latter image the lake has expanded considerably. The disconnected lakes and debris covered ice on the left side-west side of the glacier has been replaced by all lake. Icebergs are afloat in this lake, they do not survive very long. The debris cover itself insulates the glacier ice from melting, slowing the process. However, the process due to the warmth and increased melting of the last decade has been increasing.
In the image below is a closeup of the section of ice that has now disintegrated, before it did. You can see the crevasses in some of the icebergs too. This is a rapidly changing environment due to the ongoing climate warming.
Pine Island Glacier Grounding Line Updated 2012
The Pine Island Glacier is a principal outlet glacier of the West Antarctic Ice Sheet draining into the Amundsen Sea. The ice stream is 40 km wide as it reaches the sea. Recent retreat, thinning and acceleration have focussed attention on this glacier. This is a brief note in support of a RealClimate article. The grounding line is of principal concern here. This is where the glacier goes afloat. The grounding line is where the bottom of the glacier comes in contact with the ground, in this case the sea bottom. The grounding line is an anchoring point for the outlet glaciers. The length of the glacier that is grounded is being both slowed and stabilized by the basal friction. Beyond the grounding line toward the margin the floating ice shelf is susceptible to a rapid calving retreat and as the grounding line retreats, so would the calving front. Note in the image below that the current grounding line is on relatively high terrain, but is close to a deep basin. The annotated image below is from a British Antarctic Survey image, taken from their autosub program exploring beneath the ice shelf of the Pine Island Glacier combined with data from radar altimeter data flown by NASA. The second image below is a profile of depth under Pine Island Glacier from (Shepard et al, 2001)that indicates that beyond the grounding line the depth remains more than 1000 meters below sea level for approximately 200 km. 
Grounding line retreat could lead to the glacier retreating into this basin, not a stable situation. Basal melting is of particular concern, has been calculated to exceed 15 m/year. In addition the formation of basal crevasses which are much wider than surface crevasses may be critical in the rifting process. The British Antarctic Survey, NASA and several universities in particular have been focusing on this glacier. The second image shows the grounding line in the surface. This is an annotated satellite image from NASA. Just above the grounding line you can note that the surface of the glacier has some large scale roughness which indicates the impact of the sub-glacier topography. 
This topography acts to slow and buttress the glacier. This area is above the topographic rise from the deep basin to the higher terrain of the current grounding line. The ongoing focus on the Pine Island Glacier will be fascinating to watch. In particular the emphasis on the oceanographic aspects beneath the ice shelf. The melt rates beneath the ice shelf are significant, on the order of 15 m/year. This is an aspect that has received less attention and will certainly yield interesting results, considerable technologic frustrations and innovations. The nearby Smith Glacier has experienced a similar inland spread of rifting and retreat. In 2011 an additional rift has formed that is 20-25 km inland of the calving front, first noted by NASA’a Operation Icebridge. November 3, 2011 MODIS imagery is seen below. The rifts in both 2001 and 2011 have begun on the east edge of the ice stream an propogated westward. The propagation is more likely as an exploitation of basal crevasses then surface crevasses. The rift from 2011 led to iceberg formation in the fall of 2013 as seen in MODIS images. 
On October 5, 2011 MODIS imagery indicates no rift. By Sept. 17, 2012 a second rift parallel to the first had developed. 
Gilkey Glacier Retreat, Juneau Icefield
Above is a paired Landsat image from 1984 left and 2013 right indicaing the 3200 m retreat during this period of Gilkey Glacier.The Juneau Icefield Research Program has long monitored the mass balance of the Lemon Creek and Taku Glacier on the Juneau Icefield. This program begun by Maynard Miller in 1946 and continuing through today has also monitored the terminus behavior of the icefields outlet glaciers. Of the 17 significant outlet glaciers 5 have retreated more than 500 m since 1948, 11 more than 1000 m, and one glacier the Taku has advanced. I have a chance to visit the glaciers during a number of summers over the last 25 years as part of this ongoing annual program. The Gilkey Glacier is a 32 km long 245 km2 outlet glacier flowing west from the Juneau Icefield. In 1948 it terminate at the head of a braided outwash plain. At that time it was joined 5 km above the terminus by the Battle and Thiel Glaciers from the south. 
All three of these glaciers drain from the Juneau Iceifeld accumulation zone between 1500 and 2000 m, which maintain consistent snow cover. From 1948 to 1967 the Gilkey Glacier retreated 600 m and in 1961 a proglacial lake began to form. By 2005 Gilkey Glacier had retreated another 3200 m , generating a proglacial lake that is now 3.9 kilometers long, which is approximately the amount of retreat in the last 60 years as well. 
The lake is partly filled with large icebergs from disintegration of the, note below in an image from Scott McGee of JIRP,Gilkey terminus. The lake is currently terminating in this still growing lake. Approximately half of this retreat occurred after a 1991 satellite image indicated the lake was close to half its current size. The retreat has been resulted from calving icebergs into the new lake as well as thinning from melting in the lower reach of the glacier. The extensive debris cover and lack of crevassing in the lower 1500 meters of the glacier indicates that this section is stagnant and will break up soon. 
Gilkey Glacier was in 1955 joined by the tributary glaciers Battle and Thiel Glacier. A visit to the Battle Glacier in 1982 indicated that it had separated from the Gilkey Glacier and the Thiel Glacier, but the Thiel Glacier was still connected. By 1991 the Thiel Glacier had separated. Today these glaciers terminate 3200 m and 1700 m up their respective valleys from Gilkey Glacier. Thiel has retreated 1700 m from the Gilkey Glacier. A retreat of 3200 m has created a glacier 70 % its former length. The vast bare valley beyond the terminus is in stark contrast to the map above. Thiel Glacier has extensive lateral moraines extending above the glacier terminus indicating the ongoing retreat. The lower 3 kilometers of this glacier are flat and are downwasting, indicating a substantial retreat is still underway. A view up the valley from the Gilkey toward the terminus of Battle Glacier indicates that most of the area deglaciated was a flat low elevation valley. Now that the glacier is retreating up a steeper slope, the retreat rate of Battle Glacier should slow.
Mass Balance of the Easton Glacier 2009
Immediately below is Easton Glacier on Mt. Baker in the North Cascades in late May 2009. The glacier is still completely snow covered. The bench where the small gray cloud shadows are at 6000 feet averages 20 feet of snow remaining.
Easton Glacier extends from the terminus at 5600 feet to the slopes near Sherman Crater at 9000 feet. Each summer since 1990 NCGCP has measured the mass balance of this glacier. View Youtube for a pictorial review of the full 2009 field season . The glacier has retreated 300 m since 1990. During this same period the glacier has lost a cumulative mean of 13 m of thickness. Given a thickness in 1990 between 60 and 75 m, this is about 20 % of the total glacier volume. The image below shows the terminus in 2009(green=2009, 2006=brown, red=2003, purple=1993 and yellow=1984). 
Measuring mass balance requires assessing snowpack depth and areal extent at the end of the summer melt season and the amount of melting in areas where blue ice or firn (snow more than a year old) is exposed. Below is measuring crevasse stratigraphy and below that emplacing a stake to measure ablation with weather instruments on it. 
Mass Balance = residual snow accumulation – ice-firn melting.
The melt season began a bit late just when the May picture was taken Winter snowpack was between 75and 90% of normal in the area as of April 1. The melt season had been late to begin and snowpack by late May was near normal. Record heat was experienced at the end of May and the start of June, quickly causing snowpack to fall below normal.Each year we measure the snow depth via probing and crevasse stratigraphy at more than 200 locations. These depth measurements allow the completion of a map of snow distribution. This map is completed in early August and updated, based on a smaller number of observation in late September. The amount of melting is assessed from stakes emplaced in the glacier and the recession of the snowline in areas where snow pack depth has been assessed. below are images from early and then mid-August indicating the rise of the snowline. 
A warm June and July caused exceptional snow pack melt and by early August when we began assessing snow pack depth retained, the snowcover had receded to the 6400 foot level, 300-400 feet higher than normal. Snowpack remained below normal all the way to the 8600 foot level. the snowpack since early July had been rising nearly 100 feet per week. By mid-August at right the snow line on the glacier averaged 6800 feet. By mid and Late September the snowline had risen to 7400 feet a rate of rise of 150 feet per week since mid-August. Below is an image from mid-September 2009. 
The amount of melting on the glacier in July was the highest we have measured totaling, 2.1 m. This led to the exposure of a couple of new bedrock knobs evident in the picture at right near the 2100 meters, black arrows. Overall the mass balance of the glacier in 2009 was a negative 2.06 m. This glacier averages 55-70 m in thickness and this mass balance loss represents a 3% volume loss in a single year for the glacier.
Sperry Glacier Recession
In 1900 Sperry Glacier had an area of 3.39 km2. By 1938 it had diminished to 1.58 km2 and by 1946 it was only 1.34 km2 in area. The estimated loss in volume between 1938 and 1946 was a 23 meter reduction in the level of the surface of the lower half of the glacier during that period. Recession proceeded at an annual rate of 15.3 m. be¬tween 1938 and 1945; 11.9 m. from 1945 to 1947; 10.5 m. from 1947 to 1948; and 12.9 m. from 1948 to 1949 (Dyson, 1950).
Recession of Sperry Glacier continued from about 1950-1970 and has been accompanied by loss of volume of the lower part of the glacier. Sperry Glacier has been examined in reconnaissance (Johnson, 1958, 1960, 1964). Comparison of longitudinal and transverse profiles shows that since 1947 the upper part of the glacier has increased in vol¬ume during some years and remained constant during others, whereas the lower part has decreased in volume. Throughout this time span slow terminal recession has been continuous. Surface ice velocities on Sperry Glacier average about 3 m./year.
Sperry Glacier retreated at a slower rate of 5 m/a, from 1950-1979 (Cararra and McGrimsey, 1981). The retreat has ranged from 3-5 m/a from the 1979-1993 period (Key, Fagre and Menicke, 2002).
In 1993 0.87 square kilometers remained. This glacier still has crevasses and is not merely stagnant and melting away. A comparison of imagery from 1991 top (orange line for terminus), 2003 middle (green line) and 2005 bottom (blue line) indicate the marginal changes during this 14 year interval. These images are all from Google Earth using the historic imagery function. 
Marginal recession averages 95 meters in this period ranging from 20-200 meters. The glacier was 1200 meters long in 1990 so this is close to a 10% loss in length. The current rate of retreat is slightly higher than the 3-5 m/a average fro the 1979-1993 period. The image in 1991 is from Aug. 25th, the glacier still has 70% of its area covered with snow from the previous winter. This is called the accumulation area ratio and in general must be above 60 at the end of the summer for the glacier to not lose mass. In 2003 the accumulation area ratio is about 30 and this is on Sept. 25th at the end of the melt season. In 2005 the accumulation area ratio is 30 at the most. Both years this limited a snowcover would lead to a significant negative mass balance, volume loss. The thinning in the upper portion of the glacier appears limited. There is not an evident change in the upper margin of the glacier. The crevassing which is indicative of movement has also not decreased much suggesting limited changes in the dynamics of the upper glacier. The comparatively slow changes in the accumulation zone, suggests a glacier that still has a consistent accumulation zone and is not likely to melt away rapidly, within the next 30 years, given the current climate. The glacier is showing no signs that it is approaching equilibrium, and that it can survive the current climate. This is in contrast to nearby Harrison Glacier which is receding quite slowly. There are new outcrops appearing at points A and B in the 2005 image indicating thinning and retreat is continuing. Annual layers are evident at point c in the 2005 image. Crevassing in the same area at point D is evident in each image. 
The USGS and the NPS have made Sperry Glacier a focus of field study beginning in 2005. The long term record of glacier area and glacier retreat makes it a good candidate. To date no mass balance data has been completed or reported. This data is essential to understand future terminus and volume responses. This project has been particular good at acquiring historic images to compare to current images 1913 and 2008. Bob Sihler captured the lack of snow remaining on Sperry Glacier in 2009., with a month still left in the melt season.
Devon Ice Cap
Two recent papers have examined the changes in flow, mass balance and volume of the Devon Ice Cap(Shepherd et al., 2007) (Dowdeswell, 2004). The Devon Ice Cap on Devon Island in the Canadian Arctic ice cap’s area has an area of 14,000 km2, with a volume of 3980 km3 . The ice cap area decreased by 332 km2 (2.4%) between 1960 and 2000.
The mass balance of the glacier has been assessed since 1960, the total mass loss due to surface melting and runoff between has been about 59 km3. Between 1960 and 1999 about 21 km3 of ice was lost from the ice cap by calving of icebergs, contributing 0.21 ± 0.02 mm to global sea level over this time. The long term mean net surface mass balance was 0.13 m from 1960-2000. From 1998-2007 the mean annual balance has been -0.23 m year, a substantial increase. 
The Belcher Glacier above is the principal outlet glacier calving up to 30% of the total iceberg volume from the ice cap.
Devon Ice Cap’s negative balance has been due to warming and greater ablation, as the upper part of the glacier has seen some increase in accumulation, which has been more than offset by increased melting. 
In this case the mass balance record indicates a dramatic worsening after 1995. It will be interesting to see the ablation results from the summer of 2008, when record melting was noted both in northern Greenland and northern Ellesmere Island. The glacier is not alone in its behavior, the Prince of Wales Icefield has had a negative mass balance over the last forty years of -80 km3, equivalent to a mean-specific mass balance across the ice field of -0.1 m w.e. a-1, contributes 0.20 mm to global eustatic sea level rise (Mair et at., 2008).
Photographs of the fieldwork coordinated by the University of Alberta
26th Annual North Cascade Glacier Climate Project 2009 Field Season
This video examines the 2009 North Cascade Glacier Climate Project Field Season. It is a look more at where we work, than what we find. Mass balances were substantial averaging -1.93 m. The winter season was wetter than average, with close to average snowpack in the North Cascades. Summer melt conditions were exceptionally warm, leading to enhanced melting and considerable losses in glacier volume. The mass loss of approximately 2 meters represents about 4% of total glacier volume, gone in one year. In July ablation averaged 8.5 cm per day. For glaciers that average 50-60 m in thickness that is the loss of 2.5 m in one month. Most of the melt was snowpack from the previous winter. However, by mid-August blue ice was exposed on the majority of the glacier surfaces across the North Cascades and any ablation was a loss in long term glacier volume. In the case of Columbia Glacier at the end of August a view of its surface indicates only a few white patches of snow remaining. 
Glacier retreat was slowed on Rainbow and Ice Worm glaciers where the terminus was buried under avalanche snow. Retreat of Easton Glacier was 20 m, Lower Curtis Glacier 11m, Daniels Glacier 12 m, Lynch Glacier 8 m. All 42 glacier observed retreated in 2009. Easton Glacier developed a new rock outcrop in the midst of the glacier
. More details on this project North Cascade Glacier Climate Project
[url=http://www.youtube.com/watch?v=DJGQXlvWXy8]
From a Glaciers Perspective 