Data sources and image processing

The data used in this study consist of a Landsat 7 Enhanced Thematic Mapper Plus (ETM+) image, British Columbia Government aerial photography and a DMTI Spatial Inc. 30 m resolution digital elevation model (DEM). The ETM+ scene was acquired on 14 September 2001 (path 44, row 25) and was obtained from the Geogratis website of Natural Resources Canada (http://geogratis.cgdi.gc.ca/) as Landsat 7 Orthorectified Imagery over Canada. This imagery is derived from Landsat 7 raw image level L1G (i.e. radiometrically and systematically corrected) processed data and is reported to have a horizontal positional accuracy of ±30 m or less with a 90% level of confidence. The aerial photography was acquired on 17 September 1951 along British Columbia flight-lines 1393 and 1394, which were flown at an altitude of ∼5300 m. The focal length of the camera was 81.38 mm, resulting in an average photographic scale of ∼1 : 50 000. The original aerial photography prints are archived at Canada’s National Hydrology Research Institute (NHRI) at the University of Saskatchewan as part of the National Glacier Inventory and were digitally scanned at a resolution of 300 dpi using a flatbed scanner. This resulted in a ground resolution of the digital aerial photograph images of ∼4 m. As small features such as trees and small boulders could be clearly distinguished in the digital imagery, the true image resolution is likely finer than this value. The DMTI Spatial Inc. DEM was derived from interpolation of the Canadian National Topographic Database (NTDB) digital mapping, which in turn corresponds to the National Topographic System (NTS) 1 : 50 000 scale map sheets (82L09 and 82 L1 6 for the study region). Topographic contours for this region correspond to the first-edition NTS sheets, which were based on aerial photography flown in 1947 and 1951. However, vertical accuracy is not reported, so the error is estimated to be approximately ±20 m, or half of the NTDB contour interval. The DEM was obtained through the data and Geographic Information System (GIS) services of the University of Alberta Library.

The ETM+ Orthorectified Imagery was obtained with spatial reference to the Lambert Conformal Conic map projection with standard parallels of 49° and 77° N on the North American Datum 1983 (NAD83) datum and Geodetic Reference System 1980 (GRS80) ellipsoid, and subsequently projected in Universal Transverse Mercator (UTM) coordinates. Data fusion was performed to enhance the apparent resolution of the imagery using PCI Geomatica^TM. In this process, an input pseudo-color image is fused with a grayscale intensity image to produce an output RGB (red, green, blue) pseudo-color image with the same resolution as the original grayscale image. ETM+ bands 2, 3 and 4 (λ = 0.53−0.61, 0.63−0.69 and 0.78–0.90 μm; 30 m resolution) were combined with panchromatic band 8 (λ = 0.52–0.90 μm; 15 m resolution).

The digital aerial photographs were spatially referenced to the fused ETM+ Orthorectified Imagery using the thin-plate spline mathematical model in PCI Orthoengine^TM. This model fits the ground control points (GCPs) exactly, and warping is distributed throughout the image, with minimum curvature becoming linear away from the GCPs. Photographs essentially centered on individual glaciers, or groups of glaciers, were georeferenced by selecting 10–20 GCPs that were clearly identifiable in both images, with points chosen on stable terrain directly adjacent to, and surrounding, the glacier margins. This approach is well suited to the purposes of this study, as it allows a high level of accuracy over the small areas occupied by the glaciers of interest, with relatively few points collected in a dense network immediately surrounding the glaciers.

A further source of high-resolution imagery was used as visual reference to help positively identify glaciers and distinguish snowpatches near the time of the ETM+ image acquisition. This imagery is made available for public viewing through the Google^TM Earth web application, which displays British Columbia Government Terrain Resources Information Management (TRIM) orthophoto mosaic imagery over the study region (0.5 m resolution). For this region, the imagery was derived from aerial photography acquired in the late summer of 2001 and 2004. Digital scanned photographs were orthorectified using available camera calibration reports, interior orientation data (i.e. fiducial marks), and absolute orientation data consisting of a minimum of six GCPs, together with parameters for Earth curvature, terrain distortions and refraction resulting from aerial triangulation, in the adjustment package (as documented within the British Columbia Crown Registry and Geographic Base web page, http://ilmbwww.gov.bc.ca/bmgs/). The documented horizontal error of the product is stated to be a maximum of 0.5 mm for the final map scale (i.e. 10 m for 1 : 20 000 scale TRIM mapping). Google^TM Earth also allows three-dimensional (3-D) perspective viewing of the imagery by draping it over a DEM (assumed in this case to be a subset of the regional TRIM DEM).

Glacier delineation and change detection

Ice margins were delineated from the 2001 ETM+ imagery and the georeferenced 1951 aerial photography using onscreen digitizing techniques in ESRI® ArcMap^TM 9.1 GIS. Glaciers were defined by manually digitizing a series of points along the ice margins to construct a shapefile of individual glacier polygons. Thorough inspection was undertaken to identify all glaciers positively and delineate their margins accurately. This included reviewing all sources of imagery in detail and distinguishing small glaciers from snowpatches by confirming the presence of visible crevasses and/or exposed ice. There were relatively few debris-covered glaciers, but, where these were encountered, accurate delineation was still possible with the use of the aerial photography. Based on the digital aerial photography, it was possible to define glaciers as small as 10²–10³ m² and to digitize their margins to within up to ±5 m (for further discussion on the potential error associated with co-registration between the data sources, see Reference DeBeer and SharpDeBeer and Sharp, 2007). In instances where ice flow diverges into separate drainages, the glacier polygons were clipped manually along the flow divides identified from the DEM (valid for the initial time frame). For all glaciers, we determined how the glacier area changed between the 1951 and 2001 imagery. In order to achieve maximum confidence in our results for this task, it was necessary to refer visually to the British Columbia TRIM imagery shown in Google^TM Earth, as very small features could be detected in this imagery and compared with the 1951 imagery. This allowed us to overcome the potential limitations of the coarser-resolution fused ETM+ imagery where snow, shadows or debris cover obscured the glacier margins.

Topographic analysis

A number of topographic indices were derived for each glacier using the shapefile polygons together with the DEM in ArcMap^TM GIS. Parameters such as glacier area (A; m²) and perimeter (P; m) were derived directly from the polygons representing the 1951 glacier extents. Only glaciers with an initial surface area <0.4 × 10⁶ m² (i.e. 0.4 km²) were included in the analysis. The area-weighted mean elevation of each glacier (Z; m) was determined for the 1951 spatial extent of the glacier polygons from the DEM and, in a similar manner, the average slope (α; degrees) and aspect (ω; degrees clockwise from north) of each glacier were determined using raster files derived from the DEM representing terrain slope (i.e. gradient) and aspect. Since aspect values are given in degrees clockwise from north, special care had to be taken in assigning mean values to glacier polygons that included both high and low values of aspect. In these cases, the appropriate value was interpreted manually using the aspect raster file and contour lines derived from the DEM. Potential error associated with the values of all of these parameters should be very small (i.e. within a few percent of their total ranges), because of the detailed methods used to delineate the glaciers and because the error associated with the DEM is not likely to be random. If the error in the DEM is directionally biased, individual gridcells would be offset from their true ground value, but the derived parameters involving slope or aspect would not be affected significantly. The estimated error of the DEM (±20 m) is minimal in comparison to the range of elevations of these glaciers (∼700 m). The elevation and aspect of a glacier influence its mass balance primarily through their effects on energy receipt (i.e. air temperature, solar radiation receipt) and also through their influence on snow accumulation (i.e. increasing snowfall with elevation, and windward and leeward slope effects on snowfall and snow redistribution). The slope influences ice velocity and mass flux, and may also influence snow accumulation rates through its effect on avalanche transport of snow over the glacier surface.

Other relevant indices for glacier mass balance were derived from these initial parameters and/or the topography of the local areas surrounding individual glaciers. A compactness ratio (C; dimensionless) defined by the ratio of the area/perimeter ratio of a glacier to the area/perimeter ratio of a circle with the same area was derived following Reference AllenAllen (1998). This ratio is useful in describing the morphometry of a glacier as it relates to the confinement and potential mass inputs from avalanching from surrounding slopes (e.g. less compact glaciers may exhibit indented or irregular shapes and extend up feeding avalanche gulleys, or be elongated and occupy ledges and/or the base of steep slopes or cliffs). The potential effects of avalanching were further represented using indices of the upslope area and its average slope. A separate shapefile was created to represent upslope contributing areas above each of the glaciers. In this case, polygons were formed from the upslope edge of the glacier, the ridgeline above the glacier, and two paths, orthogonal to the contour lines, leading from the lateral extremes of the glacier to the ridgeline. The area occupied by the glacier within this zone was excluded, but in cases where other distinct glaciers were situated either partially or entirely within the upslope zone their area within this zone was included. Relative upslope area (U_A ; dimensionless) was then defined as the ratio of the upslope area to glacier surface area. Mean slope within the upslope contributing zone (U_α ; degrees) was determined in the same manner as mean slope for the glacier polygons. These parameters provide an index of the potential contribution to the local mass balance from avalanching from slopes above the glacier, with larger and steeper upslope zones potentially providing greater mass inputs.

Finally, a parameter (R _s; dimensionless) was derived to represent the potential intensity of clear-sky direct-beam solar radiation inputs to the glacier surface during the ablation period. This involved taking the cosine of the incidence angle between the local glacier surface and the sun (following Reference Garnier and OhmuraGarnier and Ohmura, 1970) at solar noon on 1 August. For each glacier, this angle was determined using its average slope and aspect, together with the median latitude of the study region (50.7°) and the solar declination (18.05°) for this date and time. The resulting value was then modified to include the effects of shading by adjacent terrain. A hillshade raster was generated in ArcMap^TM for the same solar geometry and was converted to a binary grid of 0 (shade) and 1 (no shade). The average value of this grid (equivalent to the fraction of non-shaded area) was then determined for each glacier and used to scale the direct-beam radiation intensity term. This term is a useful approximation and serves as an index that should correlate well with incident radiation amounts obtained by integration over the ablation season and different times of day. Previous studies on mid-latitude alpine glaciers have found that net shortwave radiation is the dominant component in the surface energy balance during the ablation season (e.g. Reference Greuell and SmeetsGreuell and Smeets, 2001; Reference Oerlemans and KlokOerlemans and Klok, 2002), so this parameter should provide an index for potential ablation rates on different glaciers during the summer.

Regional climate trends and glacier changes

Figure 2 shows climatic trends for Revelstoke, BritishColumbia (Fig. 1; 50.97° N, 118.18° W; 443 m a.s.l.) that are relevant for glacier mass balance in the region during the 20th century. At several times just prior to, and during, the study period conditions were likely to favor increasing regional glacier mass balance (i.e. more positive or less negative). These are times when total winter precipitation was unusually high and average summer temperatures were below average, such as the periods ∼1945–60 and the late 1960s and early 1970s. At other times, conditions were likely more conducive for decreasing mass balance in the region. The final two decades of the study period were characterized by considerably lower than average winter precipitation totals, beginning around the mid-1970s, and warmer than usual summer air temperatures. Mass-balance studies in the Canadian Rocky and southern Coast Mountains and the Pacific northwest of the United States record this decline in winter snowfall and show that it resulted in increasingly negative net mass balance due to the resulting more rapid rise of the transient summer snowline and earlier exposure of low-albedo glacier ice (Reference Hodge, Trabant, Krimmel, Heinrichs, March and JosbergerHodge and others, 1998; Reference Bitz and BattistiBitz and Battisti, 1999; Reference Moore and DemuthMoore and Demuth, 2001; Reference Demuth, Keller, Demuth, Munro and YoungDemuth and Keller, 2006).

Fig. 2. Time series of (a) total winter (December–March) precipitation and (b) average summer (June–August) air temperature shown together with 7 year running averages (bold lines) for Revelstoke (station ID 1176749) (source: Historical Adjusted Climate Database for Canada; http://www.cccma.ec.gc.ca/hccd/).

Although these data are for a single site at low elevation and therefore may not be entirely representative of conditions in the vicinity of the glaciers, they provide a sense of recent climatic variability within the region. Although more detailed investigation of changes in the climate near the glaciers (e.g. accumulation at the equilibrium-line altitude (ELA); Reference BraithwaiteBraithwaite, 2008) and of the relationship between climate forcing and glacier response would be desirable, it would be difficult given the lack of available data and is beyond the objectives of the current study. Nevertheless, it is clear that recent conditions within the region have favored glacier decline. For instance, over the period 1951–2001, the larger glaciers (i.e. 0.4–5.0 km²) within the region (Blanket Glacier, ∼7.7 km² in 1951, is the largest ice mass in the region, but was divided into two separate drainages for accounting in this study) exhibited terminal retreat of up to nearly 2 km and net reduction of up to 60% of their initial area. These glaciers should have a response time in the order of decades (Reference Jóhannesson, Raymond, Waddington and OerlemansJóhannesson and others, 1989; Reference Harrison, Elsberg, Echelmeyer and KrimmelHarrison and others, 2001), implying that this decline is a response to recent climatic conditions within the region. There is no discernible spatial pattern of changes in glacier area and terminus position across the region, despite there being considerable differences between individual glaciers (Fig. 1; a pattern attributed primarily to differences in the local setting and morphology of the glaciers). This suggests that the recent declining tendency in winter precipitation and increasing summer air temperatures in the region have been distributed uniformly over the study area and that local characteristics have largely influenced the response of the glaciers to these trends.

The frequency distributions of glacier areas for both time periods (Fig. 3) are highly skewed towards the smaller glaciers in terms of their total numbers. Glaciers <0.4 × 10⁶ m² in area represented 81% and 84% of the total population and 25% and 31 % of the total area in 1951 and 2001, respectively. While four very small glaciers disappeared and were not counted in 2001, many larger glaciers retreated substantially and some became separated into two or more smaller glaciers, so that the number of glaciers in most of the smaller area classes either increased or remained unchanged. These results show a shift in the distributions of the glacier population and total glacier area towards smaller glaciers over this time period.

Fig. 3. Frequency histogram of glacier sizes within the study region for the 1951 and 2001 glacier extents. Size classes represent the maximum glacier area within each class.

Topographic indices and local mass balance

Of the glaciers in the study region, 86 had an initial area of ≤0.4 × 10⁶ m² as determined from the 1951 imagery. Table 1 gives summary statistical information for the various topographic and geometric indices calculated for these glaciers, and distinguishes between glaciers that disappeared or decreased in area and glaciers that either increased or did not change in area. Several differences are noted between the two populations. Glaciers that decreased in area or disappeared have lower mean values of elevation, surface slope and upslope zone steepness and higher mean values of upslope contributing area and potential direct-beam solar radiation than glaciers that maintained a constant area. However, given the small sample size we did not attempt to establish whether any of the differences between the two populations are statistically significant.

For aspect values, which are circular in nature, it is inappropriate to use ordinary linear statistics for analysis of these data (e.g. since 0° is equivalent to 360°), so vector summation was used as an alternative. The mean aspect of each set of glaciers was determined by converting individual glacier aspects into unit vectors, summing the east and north components of these vectors and subsequently converting the direction of the resultant vector into a value of degrees clockwise from north. The strength of this vector was determined as the length of the resultant vector, expressed as a fraction of the total length of the individual component vectors (Reference EvansEvans, 1977, Reference Evans2006). Vector strength provides a measure of the dispersion of glacier aspects, ranging from 0 for no favored direction to 1 for all glaciers having the same aspect. Table 1 shows that both populations are characterized by mean aspects slightly east of north; however, the vectors are concentrated in this direction for glaciers with areas that either did not change or increased in area (vector strength = 0.55), whereas those of the glaciers that decreased in area or disappeared showed almost no favored direction (vector strength = 0.04). The distribution of glacier aspects is shown as a frequency histogram in Figure 4, which also shows observed net changes in area of the glaciers within specific aspect classes. Glaciers with a northerly aspect are clearly the most common, but many glaciers also have aspects within the range east to south. Only two glaciers had an aspect of southwest or west and, of those, one shrank and one disappeared during the study period. These results indicate that sites facing towards the sun in the mid-afternoon are not favorable for glacier preservation. This tendency is likely due in part to more effective melting in the afternoon when the combination of incident solar radiation and air temperature is at a maximum (Reference EvansEvans, 2006). Sites with a northern and eastern orientation are well suited for sheltering small glaciers, as suggested by the strong concentration of vectors in this direction for glaciers that underwent no net area change. Although these results are intuitive, there are several deviations from this generalization (e.g. the lack of a favored orientation for shrinking glaciers and the preservation of numerous glaciers with aspect values far from the mean), which are likely due to the combined effects of other factors affecting local mass balance, including those described previously in this paper.

Fig. 4. Frequency histogram of glaciers (initial area <0.4 × 10⁶ m²) within different aspect classes, indicating observed net changes of glaciers in these classes over the study period.

Figure 5 and Table 2 provide details of the interrelationships between the various topographic and geometric indices calculated for individual glaciers. Spearman’s rank correlation coefficients are used as a measure of the degree of association between these indices because they provide a simple non-parametric measure with few limiting assumptions. These are univariate associations, but are reasonable in this context because of the small sample size and the exploratory nature of this analysis. Many of the indices are significantly correlated with each other, which is to be expected given the inherent association between some of the parameters (e.g. area and perimeter for common shapes) and because some of the parameters were calculated in part using other parameters (e.g. compactness, which depends on perimeter and area). However, several of the significant correlations are not inherent and may have important implications for the local mass balance of many glaciers. The correlation between R _s and Z, for example, indicates that glaciers situated at lower elevations generally receive less clear-sky direct-beam solar radiation than glaciers at higher elevations. Atmospheric effects on incident radiation are not included in our model, but would tend to strengthen the positive association between R _s and Z if they were included. This may help to explain the observed lack of area change of many of the glaciers, as glaciers in sites that are relatively exposed to the sun tend to be situated at higher elevations where air temperatures are cooler, thereby limiting ablation rates. Net longwave radiation is likely reduced on these higher-elevation glaciers due to reduced air mass above them and less obstructed local horizons (e.g. Reference Strasser, Corripio, Pellicciotti, Burlando, Brock and FunkStrasser and others, 2004), as suggested by the strong negative association between Z and U_A . Further, these high-elevation glaciers may retain snow cover later in the summer due to higher snow accumulation and reduced melt rates, which act to maintain a relatively high albedo and limit the net shortwave radiation receipt. In contrast, glaciers situated at relatively low elevations are sheltered to a greater extent from direct solar radiation. This tends to create a local microclimate that is cooler and more favorable for the preservation of ice. It has been suggested that smaller glaciers, with an inherently greater area-to-volume ratio, should shrink faster than larger glaciers under the same ablation rate (Reference Granshaw and FountainGranshaw and Fountain, 2006). The topographic settings of many of the very small glaciers in this study indicate that ablation rates at a given elevation on these glaciers are likely much less than those at equivalent elevations on the larger and more exposed glaciers.

Fig. 5. Scatter plots showing relationships between selected topographic indices, indicating observed net changes of individual glaciers over the study period. Z is mean elevation, ω is mean aspect, U_A is relative upslope contributing area, U_α is mean slope in the upslope contributing zone and R _s is incident solar radiation index. The regional average long-term ELA is shown as the gray line in (a) and (b). The aspect classes of Figure 4 are shown in (c).

Ice may also persist at elevations far below the regional ELA, in part due to enhancement of accumulation to levels that exceed potential ablation for that altitude (Reference KuhnKuhn, 1995). Wind drifting and avalanches, for example, may considerably increase the local snow accumulation relative to winter precipitation alone, such that accumulation on small sheltered glaciers can be almost invariant in response to variations in direct snowfall (e.g. Reference Hoffman, Fountain and AchuffHoffman and others, 2007). Several of the topographic and geometric indices derived in this study are useful for examining differences in the local accumulation characteristics. Table 2 shows significant rank correlations between the indices representing elevation, compactness, upslope zone steepness and relative area, and potential direct-beam solar radiation. These interrelationships suggest that glaciers situated at relatively low elevations are generally less compact in shape, are located beneath relatively steeper slopes and tend to have more extensive contributing areas above their upper margins than glaciers at higher elevations. Such glaciers commonly have more complex and elongated shapes, occupy ledge systems and the shaded edges of cirque backwalls, and have upper margins that extend up feeding avalanche gulleys. In general, they do not extend far beyond the shelter of the cirque backwalls along their flow trajectory (see Fig. 7a below). This suggests that there may be large gradients in ablation rates with distance from the cirque backwalls that are due to increasing direct-beam solar radiation. Since these glaciers likely receive enhanced mass inputs and are relatively more sheltered from direct solar radiation, they may be insensitive to the recent decline in winter precipitation that has been observed in this region.

Figure 5 provides additional insight into how the topographic setting of individual glaciers has influenced their response to recent climatic variations. In Figure 5a, all of the glaciers that decreased in area or disappeared during the study period plot within the lower right quadrant of the graph. Most of these glaciers are situated up to several hundred meters below the regional average long-term ELA (∼2360 m) and have R _s values >∼0.6. (The regional average long-term ELA was estimated as the average elevation where contour lines change from concave to convex down-valley (e.g. Reference Leonard and FountainLeonard and Fountain, 2003), for glaciers with an initial area >∼0.8 × 10⁶ m² in the region. This provides an approximate measure of the long-term average ELA that would have persisted over several decades before the time of initial image acquisition.) This suggests that these glaciers are subjected to higher air temperatures and solar radiation receipts than the glaciers that maintained their areas. Concomitantly, these glaciers are situated below slopes that are less steep than 30° on average (Fig. 5b–d), which are unlikely to contribute significant amounts of snow to the glacier surface by avalanching and which leave the glaciers more reliant on local winter precipitation for nourishment. The two glaciers that were situated below relatively steeper slopes (i.e. ∼40°) and underwent a reduction in area were either located at extremely low elevation (Fig. 5b) or had a relatively small contributing upslope area (Fig. 5d). Thus, the glaciers that decreased in area or disappeared have likely responded more to increasing air temperatures and/or decreasing winter precipitation because they were initially situated in locations that are marginal for ice preservation.

A number of glaciers are situated within sites that are unlikely to receive enhanced inputs from avalanches (i.e. those in the lower left quadrant of Fig. 5d), and many of these maintained their area over the study period. These glaciers are typically found at higher elevations (Fig. 5b) and have aspect values in the range of northwest to southeast (i.e. <157.5° and >292.5°; Fig. 5c). Most glaciers facing in these directions occupy leeward positions that are sheltered from westerly and southwesterly winds (Fig. 1), and those at high elevations are likely sustained predominantly by wind drift in addition to direct snowfall. Previous authors have used quantitative approaches to characterize potential accumulation on small glaciers and perennial snowpatches (e.g. Reference MitchellMitchell, 1996; Reference AllenAllen, 1998; Reference Carr and ColemanCarr and Coleman, 2007), but these are not likely to be informative here since the approaches relate accumulation to upwind plateau surface area or site elevation in relation to elevation in the upwind direction. The terrain here does not include large plateaus upwind of the glaciers. The dominant control on wind-drifted snow deposition on high-elevation glaciers here is most likely airflow separation over the sharply crested terrain characteristic of the region (Reference BarryBarry, 1992), which is not dependent on relative mean elevation in a specified direction or upwind contributing source area. Further, some techniques require information on ablation at the ELA, which is difficult to obtain (e.g. ELAs are difficult or impossible to determine on these very small glaciers), and cannot distinguish between snow-blow and avalanching (Reference Carr and ColemanCarr and Coleman, 2007).

Other local site characteristics

All of the glaciers that disappeared over the study period share an attribute that was not addressed by the topographic analysis. In contrast to all other small glaciers, which were predominantly snow-covered, these glaciers had little or no snow cover in the 1951 aerial photography. Glaciers that disappeared were typically located in close proximity (i.e. horizontally and vertically) to areas in which there was extensive wastage of larger glaciers between image acquisition dates. This may indicate that these were relict glaciers, out of equilibrium with climatic conditions prior to, and during, the study period. Figure 6 provides an example where the small glacier in the top left-hand corner of the 1951 image had almost no snow cover, was relatively distorted in shape and was situated at a lower elevation than the other small glaciers in the lower right-hand corner of the images. This glacier was located adjacent to the extensive ablation area of the larger glacier and was situated in a site that appears previously to have been a contributing source area for the large glacier. Thus, this glacier seems to be a remnant of a former larger glacier system from which it had become detached before the time of initial image acquisition. At the beginning of the study period, this glacier had no discernible accumulation area and appeared to be an isolated ice mass left to melt in situ. Figure 6 (as well as Figure 7) also shows how the high-resolution TRIM imagery is essential in distinguishing glacial ice from snowpatches in order to determine reliably the changes in these glaciers.

Fig. 6. Comparison of glacier margins between 1951 and 2001 shown over (a) British Columbia Government aerial photograph and (b) Landsat 7 ETM+ image (inset in (b) is part of the TRIM orthophoto mosaic shown in Google^TM Earth). White, black (in bold) and dashed lines represent ice margins in 1951, 2001 and both time periods (i.e. unchanged margins), respectively. Contour lines (25 m interval) derived from the DMTI Spatial Inc. DEM are also shown in the figure. The location of these images within the study region is indicated in Figure 1.

Fig. 7. Example images of the TRIM orthophoto mosaic viewed in 3-D with Google^TM Earth, showing examples of several features of the small glaciers within the study region (p: protalus/pronival ramparts; d: snowdrifts and cornices; i: visible ice and crevasses; s: snowpatches). Arrows in the top right corners indicate the direction of north. The locations of these images within the study region are indicated in Figure 1.

Very few glaciers advanced or increased in area. This is likely because regional climatic conditions were conducive to declining tendencies of mass balance during most of the study period. There are also several topographic factors that may partly explain the observed lack of areal increase of most of the glaciers. In many cases, glaciers are prevented from advancing far beyond cirque backwalls and sheltered areas due to the high gradients in energy receipt (i.e. direct solar radiation, temperature) away from these locations, which act to limit the extent of the glacier. The margins of many of the glaciers analyzed in this study are topographically constrained and they terminate on very steep slopes and cliffs. In these instances, an increase in accumulation and local mass balance typically leads to an increase in ice advection and/or loss by avalanching and ice calving to locations far below where the ice/snow melts in situ or contributes to other glaciers. Thus, the margins of many of these glaciers likely do not change on a year-to-year basis. In addition, small moraines and protalus/pronival ramparts (i.e. small accumulations of fallen rock debris) at the lower margins of the glaciers may form a barrier to ice movement and act as dams for avalanches (Reference KuhnKuhn, 1995). If the glaciers gain mass such that they overtop the crests of these ridges, subsequent avalanches will continue past the glacier margin and be lost to local mass balance. Such features were indeed observed in front of some of the small glaciers in this study, indicating that significant advance beyond these limits is physically unlikely.

Figure 7 provides examples of several of the features discussed in this paper. In Figure 7a it is clear that the glaciers are sustained by avalanching from upper contributing slopes and are highly sheltered from direct solar radiation (especially the lower-elevation glacier at the right). Several protalus/pronival ramparts can be seen, which act to trap snow from avalanching. Figure 7b shows some high-elevation glaciers occupying northeast-facing positions that terminate on steep slopes or cliffs. Note the relative confinement of all glaciers and also the increasingly compact shape and evidence of wind-blown snow accumulation (i.e. cornices and drifts) on glaciers at higher elevations in general. Numerous snowpatches can also be seen in these images, but are readily distinguished from glaciers in most instances by the absence of crevasses and visible ice.