Introduction

The reconstruction of former valley glaciers has become a common method for estimating paleo-snow-line elevations or equilibrium-line altitudes (ELAs), and thus for inferring Quaternary paleoclimate for mountainous regions throughout the world (Reference PorterPorter, 1975; Reference Porter1977; Reference PiercePierce, 1979; Reference MeierdingMeierding, 1982; Reference LeonardLeonard, 1984; Reference HawkinsHawkins, 1985; Reference Murray and LockeMurray and Locke, 1989; Reference Torsnes, Rye and NesjeTorsnes and others, 1993). In brief, an estimate of the ELA is obtained by determining that altitude which yields some specified ratio of the reconstructed glacier’s accumulation area to its total area. This ratio is referred to as the accumulation-area ratio (AAR). By analogy with modern glaciers in equilibrium with existing climates, the AAR is assumed to be between 0.50 and 0.80 depending on the glacier’s area–altitude distribution (Reference Meier and PostMeier and Post, 1962; Reference PiercePierce, 1979; Reference Porter, Wigley, Ingram and FarmerPorter, 1981; Reference LeonardLeonard, 1984). In recent comparisons of methodologies, Reference MeierdingMeierding (1982), Reference HawkinsHawkins (l985) and Reference Torsnes, Rye and NesjeTorsnes and others (1993) have concluded that the AAR method, because it has a more sound physical basis, results in the most accurate determination of paleo-ELAs. The paleoclimatic significance of variations in ELAs has generally been interpreted in terms of temperature change by applying a lapse rate to calculated ELA depressions, largely ignoring the effects of changes in snow accumulation and radiation balances (Reference SeltzerSeltzer, 1994).

Reconstructions of the mass balances and dynamics of paleoglaciers are alternatives to the “static” determination of ELAs using the AAR method. Paleo-mass balances can be approximated given some knowledge of mass-flux variations over the length of the glacier and the assumption of steady-state mass continuity. The paleo-mass-balance curve thus determined also defines the ELA. Such glaciological reconstructions have the potential to yield more useful climatic information because mass-balance gradients can be related to specific climatic regimes (Reference KuhnKuhn, 1981, 1984). This approach is problematic, however, inasmuch as mass-flux calculations are strongly dependent upon basal sliding velocities. Thus, various ad hoc assumptions must be made regarding the magnitude of sliding at the base of the paleoglacier (e.g. Reference Murray and LockeMurray and Locke, 1989).

A different approach to glaciological reconstructions is to use mass-balance curves of modern glaciers that are analogous in size and climatic setting to the paleoglaciers. Using the chosen mass-balance curve with the area–altitude distribution of a paleoglacier, the ELA can be determined by varying the altitude of the equilibrium line until net accumulation above equals net ablation below. This technique has been used to directly reconstruct the ELA (Reference Porter, Pierce, Hamilton and WrightPorter and others, 1983) and as a means to independently evaluate ELAs determined by other methods (Reference PiercePierce, 1979). For the former, the assumption of equivalence of climatic setting of the paleoglacier and modern analog presents a potential difficulty: the ELA of the paleoglacier is of interest precisely for its paleoclimatic implications, but its determination is based on some presumption of climatic conditions. Thus it is imperative to consider additional sources of information that might be used to verify the reliability of the reconstruction. This paper demonstrates how the information provided by detailed till-provenance studies can be used to discriminate between equally viable glaciological reconstructions of paleoglaciers.

Till Provenance and Glacier Dynamics

The drainage of Wildhorse Canyon, Idaho. U.S.A., has been modified by at least two and possibly three episodes of glaciation. The youngest, a late-Pleistocene event informally known as the “Wildhorse Canyon advance”, is represented by a series of terminal moraine complexes that document four distinct phases of glacier activity. The glacial history of the Wildhorse Canyon area has been discussed in detail elsewhere (Reference Brugger, Stewart, Evenson, Evenson, Schlüchter and RabassaBrugger and others, 1983), so in the interest of brevity it is summarized in Figure 1.

Fig. 1.

Schematic illustration of the glacial history of Wildhorse Canyon for the four phases of the late-Pleistocene “Wildhorse Canyon Glaciation”.

Because the two major catchment areas of Wildhorse Canyon are underlain by distinctly different bedrock types (Reference DoverDover, 1981), pebble and heavy mineral compositions of the tills clearly indicate the source areas from which they were derived (Reference Brugger, Stewart, Evenson, Evenson, Schlüchter and RabassaBrugger and others, 1983). Tills composed of metamorphic clasts and heavy-mineral assemblages enriched in clinopyroxenes (mostly diop-side) are derived from Precambrian gneisses, schists and quartzites―rock types exposed only in the headwaters of Wildhorse Creek proper. In contrast, tills originating from the Fall Creek drainage are characterized by relatively high percentages of granitic clasts and the absence of metamorphic lithologies.

By using the statistical techniques of factor and cluster analysis (Reference DavisDavis, 1986), several till-compositional groups were identified on the basis of their unique pebble lithologies and heavy-mineral assemblages. The statistically defined groups were thus interpreted (Reference Brugger, Stewart, Evenson, Evenson, Schlüchter and RabassaBrugger and others, 1983) as being either (a) source suites, composed predominantly of indicator lithologies and minerals; (b) dilute source suites, composed predominantly of pebble lithologies and mineral assemblages not indicative of a particular catchment area, but having a small percentage of an indicator lithology present; or (c) mixed suites, having indicators of both catchment areas in varying amounts. Average compositions of these different suites are shown in Table 1. Table 1 also reveals that the dilutants in the dilute source suites are sedimentary clasts in the pebble fraction, and calcite in the heavy mineral fraction. These components were incorporated into the source tills as the glaciers eroded Paleozoic clastic and carbonate sequences that occur in the lower reaches of the trunk valley.

Table 1.

Average compositions (%) of the statistically defined till-provenance groups

Terminus geometries of the glaciers in Wildhorse Canyon were reconstructed by Reference Brugger, Stewart, Evenson, Evenson, Schlüchter and RabassaBrugger and others (1983) for all phases of glaciation using the provenance data. A condensed interpretation for the Wildhorse Canyon I and II phases is presented in Figure 2. The significance of these reconstructions is that the distribution of indicator pebbles and minerals in moraine complexes reflects the relative magnitudes of the individual glaciers constituting the compound glacier. This is seen in Figure 2a where the sharp break in till compositions of the Wildhorse Canyon II moraine complex is interpreted to define the position of the medial moraine separating Wildhorse and Fall Creek Glaciers. Because the compositional break occurs along the east-lateral extension of the moraine complex, Fall Creek Glacier is assumed to have been restricted to a similarly lateral position within the compound glacier. On modern, non-surging, compound glaciers it can be observed that the widths of individual ice streams (as delineated by medial moraines) are roughly proportional to the size of the catchment areas from which they flow. This is a logical consequence of differences in the ice flux contributed by each catchment area. Therefore it is concluded that the Wildhorse catchment area contributed a much greater volume of ice to the compound glacier than did the Fall Creek catchment area.

Fig. 2.

Terminus geometries for the (a) Wildhorse Canyon II, and (b) Wildhorse Canyon I phases of glaciation, reconstructed on the basis of till provenance.

The position of the medial moraine during the Wildhorse Canyon I phase is more difficult to ascertain because of the non-continuous nature of the associated moraine complex. The position shown in Figure 2b is based on the following reasoning. First, the till composition of the small moraine segment northeast of the terminus indicates either a Wildhorse provenance or a mixed provenance. Although few in number, the presence of metamorphic lithologies in all till samples requires that the till was, at least in part, deposited by Wildliorse Glacier. The mixed-source samples are therefore interpreted as representing the composition of the medial moraine. Secondly, shorelines of Glacial Lake East Fork (Fig. 1a) are delineated by concentrations of ice-rafted boulders of Wildhorse provenance (Reference Brugger, Stewart, Evenson, Evenson, Schlüchter and RabassaBrugger and others, 1983). Thus a source for these boulders must be present at the calving margin of the compound glacier. The inferred position of the medial moraine again has the implication that the Wildhorse catchment area provided a substantially larger volume of ice to the compound glacier than did the Fall Greek catchment area.

That the relative contribution of Wildhorse Glacier to the compound glacier was significantly greater than that of Fall Greek Glacier is consistent with the glacial history of the area. Of particular note is the waning contribution of Fall Creek (Fig. 1c) ice during the course of the Wildhorse Canyon advance as described by Reference Brugger, Stewart, Evenson, Evenson, Schlüchter and RabassaBrugger and others (1983). Consequently, any reconstructions of these paleoglaciers should also be in accord with the till-provenance studies.

Reconstruction of the Paleoglaciers

Ice surface contours of the paleoglaciers were reconstructed for the Wildhorse Canyon I phase of glaciation following the procedure given by Reference PiercePierce (1979) and Reference Porter, Wigley, Ingram and FarmerPorter (1981). The areal extent of the compound glacier and its tributaries was determined using the geometry of moraine segments, the upper limits of erratic boulders and the upper limits of glacial erosion. The elevations at glacier margins were used to establish initial surface contours by assuming convergent and divergent flow in accumulation and ablation areas, respectively, and with due consideration of the constraints of bedrock topography on local ice flow. Longitudinal profiles obtained from the reconstructed ice surfaces provided estimates of ice thicknesses and surface slopes, which were then used to calculate basal shear stresses along both the compound glacier and its constituent ice streams. The shear stress τ is given by

where f is a “shape factor” to account for drag from the valley sides, ρ is the density of ice, g is the acceleration due to gravity, h is the ice thickness, and α is the surface slope. Surface slopes were averaged over a distance one order of magnitude larger than the local ice thickness to account for longitudinal stress gradients (Reference PatersonPaterson, 1981, p. 101). Ice surface contours were then adjusted so that the shear stresses computed at over 30 locations fell within, or were close to, the commonly accepted range of 50–l50 kPa (Reference PatersonPaterson, 1981, p. 86). The reconstructed compound glacier and profiles of Wildhorse and Fall Creek Glaciers are shown in Figures 3 and 4.

Fig. 3.

Reconstruction of the compound glacier of Wildhorse Canyon for the Wildhorse Canyon I phase of glaciation. Longitudinal profiles A–A′ and B–B′ are shown in Figure 4.

Fig. 4.

Longitudinal profiles of the Wildhorse (Profile A–A′) and Fall Creek (B–B′) glaciers. Ice thickness h and calculated basal shear stress τ values are shown for various locations.

Three simple, specific net balance curves for the compound glacier were constructed using the mass-balance characteristics of modern glaciers found in continental-type climatic regimes (Reference Grosval’d and KotlyakovGrosval’d and Kotlyakov, 1969; Reference Meier, Tangborn, Mayo and PostMeier and others, 1971; Reference Wendler, Fahl and CorbinWendler and others, 1975; Reference Young and StanleyYoung and Stanley, 1976a,Reference Young and Stanleyb; Reference KuhnKuhn, 1984). For such glaciers, maximum accumulations are typically 1–2 m w.e., while ablation gradients range from about 0.005 to 0.01 m w.e.m⁻¹. Therefore, an “average” curve (Fig. 5; Table 2A) was created using the intermediate values of 1.5 m w.e. for maximum accumulation and 0.0075 m w.e. m₋ for the ablation gradient. It is also commonly observed that higher accumulations and ablation gradients tend to occur under more moderate continental climates. Conversely, lower accumulations and ablation gradients tend to occur together on glaciers of colder continental climates. These conditions are represented by curves (Fig. 5; Table 2B and C) having maximum accumulations and ablation rates of 2.0 m w.e. and 0.01 m w.e.m₋₁, and 1.0 m w.e. and 0.005 m w.e. m⁻¹, respectively. The latter is considered to be more representative of prevailing conditions in the Wildhorse Canyon area during the late Pleistocene based on recent studies that suggest colder and drier climates than presently exist in the Rocky Mountains (Reference Porter, Pierce, Hamilton and WrightPorter and others, 1983; Reference LeonardLeonard, 1989; Reference LockeLocke, 1990). For the idealized curves it was assumed that both net ablation and net accumulation varied linearly with elevation. Finally, no attempt was made to account for calving along the eastern margin of the terminus (Fig. 3), as the mass loss here is thought to have been insignificant.

Table 2.

Results of model I reconstructions (all mass-balance and flux quantities are water-equivalent values)

Fig. 5.

(a) Area–altitude attribution for the compound glacier of Wildhorse Canyon; and the specific net balance used in the model I (b) and model II (c) reconstructions.

The specific net balance curves were used in conjunction with the glacier’s area altitude distribution (Fig. 5) to estimate the ELA associated with each mass-balance curve. These ELA reconstructions are henceforth referred to collectively as model I and individually as models IA–C, corresponding to the mass balances given in Table 2. The elevations of the equilibrium lines were located by imposing a condition of steady state, that is

where is the mean specific net balance over the area. S_i for the ith elevation interval of the glacier, and k is the number of elevation intervals. The ELAs determined for models IA–C (Table 2) are remarkably similar, all being about 8960ftFootnote * (2730m). It must be noted here that because of the considerable latitude inherent in generating mass-balance curves for the paleoglacier, there can be no “unique” ELA determined. The fortuitous agreement of these results is an artifact of the specific combinations of accumulation and ablation gradients used in the models. Other models using different combinations result in notably different ELAs (Brugger, unpublished data). Thus, as alluded to earlier, it was necessary to independently access the viability of the reconstructions.

Two methods were used to assess the glaciological reconstructions. The first involved the calculation of the AAR, which was then compared with those associated with the ELAs estimated above. For valley glaciers, an AAR of 0.65 ± 0.5 is usually taken as being indicative of steady state (Reference Andrews and MillerAndrews and Miller, 1972; Reference Porter, Wigley, Ingram and FarmerPorter, 1981; Reference MeierdingMeierding, 1982; Reference LeonardLeonard, 1984). Outside this range, larger values are representative of glaciers fed by upland ice fields, whereas smaller values are more typical of piedmont-type glaciers (Reference LeonardLeonard, 1984). For the glacier system of Wildhorse Canyon an AAR of 0.65 corresponds to an ELA of 9100ft (2774m), slightly greater than that of 8960 ft (2730 m) obtained by the mass-balance method. The latter elevation yields an AAR of 0.68, well within the acceptable range.

A second method to determine the ELA is to calculate the toe-to-headwall altitude ratio (THAR), Based on empirical studies of modern glaciers, different THAR values ranging from 0.35 to 0.50 (the median glacier elevation) have been used by different investigators (Reference Porter, Wigley, Ingram and FarmerPorter, 1981; Reference MeierdingMeierding, 1982; Reference HawkinsHawkins, 1985; Reference Murray and LockeMurray and Locke, 1989; Reference Torsnes, Rye and NesjeTorsnes and others, 1993). This wide range of values reflects differences in the interpretation of the term “headwair”, the inability to accurately define its elevation, and variations in glacier morphology (Reference HawkinsHawkins, 1985). These difficulties notwithstanding, a THAR value of 0.50 has been suggested for glaciers having a normal area altitude distribution (Reference Porter, Wigley, Ingram and FarmerPorter, 1981; Reference LeonardLeonard, 1984). For the reconstructed compound glacier, a THAR value of 0.50 renders an ELA of 9000 ft (2743 m) which is in excellent agreement with those determined by the AAR and mass-balance methods.

The AAR and THAR methods would thus appear to confirm the validity of the glaciological reconstructions of the paleoglaciers of Wildhorse Canyon. However, given the till-provenance data and their implications, a more rigorous test of viability is to compute the magnitude of the ice flux contributed by each glacier to the compound glacier. Steady-state mass continuity requires that the ice flux Q through any cross-section j must equal the mass balance integrated over that part of the glacier above it. Q_i , is thus the cumulative mass balance at j,

. Equation (3) was used to calculate the mass flux at successive cross-sections along the lengths of the tributary and compound glaciers for each reconstruction (Table 2). Since the cross-sections at the 8500 ft contour lie immediately above the confluence, the mass fluxes here provide estimates of the relative contribution of Wildhorse and Fall Creek Glaciers to the compound glacier. Table 2 reveals that for models IA–C the ice flux entering the trunk valley from Fall Creek is about equal to that from the Wildhorse catchment area. These results are inconsistent with the conclusions drawn from the till-provenance studies, and therefore problematic.

By using one specific net balance curve for the entire glacier system, model I reconstructions implicitly suppose that the altitudinal dependencies of factors affecting mass balance such as temperature and precipitation) were the same for the Wildhorse and Fall Creek valleys. Considering the ruggedness of the topography, local variability of these factors would be expected due to orographic effects on precipitation, differences in local energy balances, and so forth. This variability would be indicated if gradients in late-Pleistocene snow lines existed in the study area.

An analysis of cirque-floor elevations was performed to examine this possibility. The trend in the elevations of the lowest cirque floors is thought to approximate the paleo-snow line or ELA (Reference PorterPorter, 1964; Reference Andrews and MillerAndrews and Miller, 1972; Reference LockeLocke, 1990). In Wildhorse Canyon this trend suggests a steep, eastward rise of the paleo-snow line of roughly 30 m per km. Such steep gradients are not unprecedented in areas of high relief. Reference PorterPorter (1975, Reference Porter1977) reported gradients in late-Pleistocene snow lines up to 23 m per km in the Southern Alps of New Zealand, and 25 m per km in the Cascade Range of North America. Reference LeonardLeonard (1984) reported gradients of 20–24 m per km for parts of the San Juan Mountains in southwestern Colorado. Given that these are regional gradients, it would not be surprising for local gradients to be steeper within an individual drainage basin.

The significance of snow lines approximated by cirque-floor elevations with respect to time are equivocal, the cirques being erosional forms modified by successive glacial events (Reference Porter, Pierce, Hamilton and WrightPorter and others, 1983; Reference HawkinsHawkins, 1985; Reference LockeLocke, 1990). However, a close parallelism of snow-line and ELA gradients of different ages has been documented by several workers (Reference Andrews and MillerAndrews and Miller, 1972; Reference PorterPorter, 1975, Reference Porter1977; Reference ZwickZwick, 1980; Reference LeonardLeonard, 1984; Reference LockeLocke, 1990), indicating that the climatic factors responsible for regional gradients were relatively constant through time. There being no evidence to the contrary, this was assumed to be the case for the Wildhorse Canyon area.

Thus, a second glaciological reconstruction of the paleoglaciers of Wildhorse Canyon incorporated an ELA gradient equal to that exhibited by the lowest cirque-floor elevations. The specific mass-balance curve for this reconstruction is shown in Figure 5. For reasons discussed previously, the maximum accumulation in the Wildhorse catchment area was chosen as 1.0 m w.e., and the ablation gradient below the confluence of the two ice streams (for simplicity taken as 8500 ft) was specified to be 0.005 m w.e. m⁻¹. It was assumed that accompanying the rise in ELA was a concomitant decrease in accumulation, as observed in modern glaciated regions (Reference Meier, Tangborn, Mayo and PostMeier and others, 1971; Reference PorterPorter. 1977). Accumulation values for the Fall Creek system were therefore somewhat arbitrarily determined using an accumulation gradient equivalent to that in the Wildhorse catchment. The ablation gradient for Fall Creek Glacier above the confluence was simply defined as that of the line connecting its ELA with the value of ablation at the confluence elevation (Fig. 6).

The results of the second reconstruction are shown in Table 3. The ELAs associated with this model are at 8845 ft (2696 m) for Wildhorse Glacier and at 9295 ft (2833 m) for Fall Creek Glacier. These elevations correspond to an AAR of 0.67 for the compound glacier, essentially no different than that determined for models IA–C. The notable difference between the two models lies, however, in their estimation of the relative contribution of the two catchment areas. Above their confluence, model II yields an ice flux of 18.0 × 10⁶m³ w.e. a⁻¹ from Wildhorse Glacier and 8.86 × 10⁶ m³ w.e. a⁻¹ from Fall Creek Glacier. Thus model II represents a significant improvement over the model I reconstructions in being not only glaciologically sound but also supported by the till-provenance data.

Table 3.

Results of model II reconstruction (all mass-balance and flux quantities are water-equivalent values)

It is worth examining one additional aspect of model II. Steady-state mass continuity requires that

where Q is the ice flux given by Equation (3) at some cross-section having an area S and mean ice velocity ū. The mean ice velocity is the sum of the mean ice velocity due to internal deformation ū_d and the mean sliding velocity ū _b.ū _d is given by

where A and n are the flow-law parameters for ice, and f* is a flux-shape factor (Reference NyeNye, 1965). Parameter n is taken as 3 so that parameter A for 0°C is 5.3×10⁻¹⁵s⁻¹ kPa⁻³ (Reference PatersonPaterson, 1981, p. 39). From Equation (5) the mean deformational velocities for Wildhorse and Fall Creek Glaciers are on the order of 7 and 4m a⁻¹, respectively. Using the cross-sectional areas (4,7 × 10⁵ and 2.1 × 10⁵ m²) and the ice fluxes at the 8500 ft elevation contour, Equation (4) renders mean velocities of 38 m a⁻¹ for Wildhorse Glacier and 42 m a⁻¹ for Fall Creek Glacier. This means that basal sliding accounts for 80–90% of ice motion at these cross-sections.

The high rates of basal sliding given by model II are rather insensitive to potential errors in the estimates of ice thicknesses, which a affects both velocities due to ice deformation and cross-sectional areas (Reference BruggerBrugger, 1985). Sliding rates are more dependent on the total velocity u, and thus by Equation (4) the ice flux Q. Because of the non-uniqueness inherent in the reconstruction, it is possible to reduce sliding rates by reducing the accumulation values used for the particular specific net balance curve. However there is no paleoclimatic data to support such a reduction. Furthermore the sliding velocities, while high, are not unreasonable (Reference PatersonPaterson, 1981, p. 71). Therefore the model II reconstruction represents a good “first-order” approximation of the glaciers and glacial systems as they are though to have existed in Wildhorse Canyon during the late Pleistocene.

Conclusions

Till-provenance studies in Wildhorse Canyon provide additional constraints on the glaciological reconstructions of the late-Pleistocene paleoglaciers. When evaluated by established methods, reconstructions using one specific net balance curve for the entire glacier system appear quite reasonable in terms of the resulting ELAs. However, these reconstructions suggest that the ice fluxes contributed to the compound glacier from its two main tributaries were comparable in magnitude, contradicting the inferences drawn from the till-provenancc data. A different approach to reconstruction accounted for possible variations in the specific net balance of the compound glacier suggested by the trend of cirque-floor elevations. This approach yields a glaciologically sound reconstruction of the glacial systems in Wildhorse Canyon that is consistent with the provenance data. Moreover, this more accurate reconstruction would not have been developed in the absence of the provenance data.