Introduction
Glacier recession has been an accepted condition for high mountain areas of western Canada for the major part of the twentieth century (Reference HeusserHeusser, 1956; Reference Porter and DentonPorter and Denton, 1967; Reference HenochHenoch, 1971; Reference Gardner, Slaymaker and McPhersonGardner, [c1972]). Yet in recent years, there have been some indications that an increasing number of mountain glaciers may now be re-advancing.
Several large glacier termini in western Canada re-advanced in the mid to late 1960s (Athabasca Glacier, 1965-67; Saskatchewan Glacier, 1967-69; Bugaboo Glacier, 1964-75; Sphinx Glacier, 1966-68) according to photogrammetric surveys reported in Reference OmmanneyOmmanney (unpublished). Of these glaciers, only Bugaboo Glacier appears to have sustained re-advance into the current decade.
More recent re-advance has been described in a number of Coast Mountain glaciers (Reference RickerRicker, 1979, Reference Ricker1980, Reference Ricker1981; Reference Tupper and RickerTupper and Ricker, 1982). In the Clendenning and Elaho Ranges, Reference RickerRicker (1980) estimates that 67% of the glaciers are in a state of re-advance; Havoc Glacier having advanced an average of 38.5 m a−1 between 1970 and 1979 (Reference RickerRicker, 1981). Not only are these re-advances dramatic in amount, but they appear to be symptomatic of considerable instability in the general condition of Coast Mountain glaciers. A single year’s re-advance of 5 to 8 m at the central point of the terminus of Wedgemount Glacier, for instance, was accompanied by substantial thinning and recession along the margin such that the terminus as a whole lost mass (Reference Tupper and RickerTupper and Ricker, 1982).
This paper describes re-advance at the debriscovered terminus of Emerald Glacier, Yoho National Park, which has been sustained since 1978 at least. All the larger glaciers in the Rocky Mountains are known to be receding after the brief rally of Athabasca and Saskatchewan Glaciers between 1965 and 1969.
Emerald Glacier
Emerald Glacier is a small, mountain shelf glacier, whose longest dimension lies normal to the direction of ice motion. The northern section of the glacier is almost separated from the rest and embraces an area of only 0.6 km2. The terminus is approximately 2200 m above sea-level while the snow line at the end of the melt season was around 2500 m between 1978 and 1982.
Part of the terminus has a continuous cover of supraglacial debris, while part is relatively debrisfree. Along the ice margin in both cases the glacier is currently forming a push moraine (Reference Rogerson, Batterson, Davidson-Arnott, Davidson-Arnott, Nickling and FaheyRogerson and Batterson, 1982), termed moraine A along the section which is debris-covered and moraine B where the proximal ice surface is debris-free. A lake called Terminal Lake lies near the eastern limit of moraine A. The moraine is between 1.5 and 4 m in height and consists of a single ridge for most of its length with small multiple ridges, seldom more than 1 m in height and breadth, characteristic of the proximal side of moraine B, The moraine is stratigraphically complex: Moraine A is composed of coarse supraglacial tills with injected fines from the subglacial sources, while moraine B is composed of “bulldozed” subglacial melt-out tills (Reference Rogerson, Batterson, Davidson-Arnott, Davidson-Arnott, Nickling and FaheyRogerson and Batterson, 1982).
Re-Advance Observations
Where a glacier is bounded by an active terminal moraine, re-advance of the ice margin may be represented by forward displacement of markers on the moraine. This avoids the problem of locating and measuring an ice margin which in the melt-season may be in a temporary state of rapid recession due to high melt rates. In this paper, all measurements are made to moraine markers.
Between 1978 and 1980, the record of terminal fluctuations consists of measurements and photographs of a single site where a large block was observed, lodged in the distal slope of moraine A (Site 7; Fig. 1). In July 1980, the terminus was measured at 28 locations from 16 fixed markers on bedrock or securely lodged boulders (Fig. 2), using a steel tape. The tape was read to the nearest centimetre where possible. These measurements were repeated in September 1981 and September 1982: on these occasions several sites were measured to the nearest decimetre when more precise reading was not possible due to loss of exact site on the moraine.
Fig. 1. Measurements of re-advance of a block emplaced in moraine A taken at site 7, 1978-82.
Fig. 2. The approximate location of fixed markers around the terminus of Emerald Glacier.
Results
Between 1978 and 1980, substantial re-advance occurred at site 7, suggesting support for the qualitative observation of some re-advance along the whole length of moraine A and B. Although advance at site A was more marked in 1978–79 (4.57 m) than in 1979–80 (1.97 m) no data are available to indicate that this contrast applies along the full length of the glacier margin.
Measurable re-advance occurred at most sites during 1980–81, averaging less than one metre along moraine B but almost 2.5 m along moraine A (Table I). The greatest amount of re-advance occurred in the vicinity of Terminal Lake where the ridge at Site 6 advanced 5.31 m. A similar amount of re-advance was measured just north of the lake during 1978–79 when the ridge at site 7 moved 5.7 m. During 1981–82, re-advance along moraine B was negligible, averaging only 0.46 m, with the two southernmost sites showing no forward displacement at all. Along moraine A, displacement was less than in 1980-81 but still averaged 1.62 m with a maximum amount of 3 m measured at site 7. Average re-advance for moraine A was consistently higher than for moraine B although less than two standard deviations separate the means in both 1980–81 and 1981–82. This in part is due to a number of low values of displacement in moraine A. Most of these low values were obtained from boulders emplaced in the distal slope of the moraine. The boulders are probably partly lodged and in the case of those at sites 12 and 16, moved far less than the ridge measured above them. The differences between ridge crest and boulder displacements represent a general increase in the angle of distal slopes along moraine A and a substantial increase in the height of the moraine ridge. Since 1978 the height of the ridge has approximately doubled in the vicinity of sites 6 and 7.
Table I. Measurements of Re-Advance of Emerald Glacier at Sites shown in Figure 2
Discussion
In the case of Emerald Glacier it is clear that re-advance is accentuated by the existence of supraglacial debris cover proximal to the push moraine. This may be explained using the two models of push moraines proposed earlier (Reference Rogerson, Batterson, Davidson-Arnott, Davidson-Arnott, Nickling and FaheyRogerson and Batterson, 1982), where thick supraglacial debris cover decreases ice surface melt and allows proximal ice to remain in contact with the moraine ridge throughout the summer. In contrast, the ice margin proximal to moraine B recedes from the moraine during the summer, and during the winter must advance up to 15 m to the moraine before re-advance displaces any of the markers. Thus, a single glacier may display characteristics of synchronous advance and retreat along the same terminus where there is some alternation between bare ice and supraglacial debris. Where medial moraines meet sections of a glacier terminus, the terminus frequently displays an arcuate bulge or lobe, as noted for Berendon Glacier, British Columbia (Reference Eyles and RogersonEyles and Rogerson, 1977) and various Icelandic glaciers (Reference EylesEyles, 1979). The lobe represents a rate of recession which is lower than that for clean ice. Stagnation or disintegration topography is commonly left in zones of high supraglacial debris when the ice margin recedes so far as to abandon the area of low recession rates (Reference EylesEyles, 1979). Thus, heavily debris-covered glacier termini are often loosely referred to as “dead” or “stagnant” when they may, as in the case of Emerald Glacier, be zones of more vigorous and sustained re-advance than adjacent clean ice margins.
Measurements made on the terminus of a rock glacier 2 km to the north-west indicate no forward displacement of blocks along the terminus since 1978, despite the presence of soils which appear to have been recently disturbed by re-advance (Fig. 3).
Re-advance of any ice margin may represent recent climatic deterioration reflected in positive glacier mass balances. Mass-balance measurements at Peyto Glacier, less than 20 km to the north of Emerald Glacier indicated a slight positive mass balance for five of the year years between 1965 and 1974 (Reference Young and StanleyYoung and Stanley, [c1977]) although in recent years it has (Figure 3) been negative (personal communication from J. Power in 1982). No mass-balance measurements have been made on Emerald Glacier which has probably, like President Glacier to the north-west (Reference BrayBray, 1964) and Yoho Glacier to the north (Reference Bray and StruikBray and Stuik, 1963) retreated for most of the twentieth century from its neoglacial maximum. The current re-advance may merely represent the minor fluctuation of a glacier which has shrunk close to its equilibrium size with respect to present climate. It is however important to monitor this and other small glaciers which have a rapid throughflow of mass and which are likely to respond early to climatic change. If re-advance persists during the present decade, it is likely to be a result of climatic deterioration. whatever the control, recession should be least, and re-advance greatest, along debriscovered rather than clean ice margins, which suggests that such margins should be singled out for observations of re-advance in any glacierized area.
Fig. 3. Blocks and disturbed soils along the front of a rock-glacierized talus slope, 2 km north-west of the terminus of Emerald Glacier
Acknowledgement
This work was accomplished with the financial support of NSERC operating grants and the permission and co-operation of the Western Region, Parks Canada and the Yoho National Park personnel. Field assistance by Roger Jackson (1978), Martin Batterson and Richard Kodybka (1979), Helene Trudel (1980), and Hazen Russell (1982) is gratefully acknowledged. Drafting and photographic printing were accomplished by staff of the Department of Earth Sciences, Memorial University.
