Introduction

This article presents the results of surface strain-rate and velocity measurements made on the Taku Glacier, a part of the Juneau Icefield in south-eastern Alaska. The icefield covers about 1,500 square miles (4,000 km.²) of area with its upper névé at an elevation between 4,000 and 7,000 ft. (1,200 and 2,100 m.). The Taku Glacier is one of the major valley glaciers of the icefield (Fig. 1).

Fig. 1.

Part of the Juneau Icefield, Alaska

The objective of this study is to obtain information on the stress conditions in the glacier. Measurements were made at four points designated as a, b, c, d along the profile aa (Figs. 1 and 2). This is one of the several sites on the icefield where continuous records have been maintained on the surface velocity and accumulation. The bore-hole deformation measurements of 1950–53 were also made at this locality (Reference MillerMiller, 1958).

Fig. 2a.

Location of velocity and strain-rate measurements

Fig. 2b.

Bedrock profile along aa (after Reference PoulterPoulter and others, 1949; Reference MillerMiller, 1952)

Strain-Rate Measurements

The measurement of strain-rate followed the procedure outlined by Reference NyeNye (1959). Squares with sides equal to 100 ft. (30.5 m.) were set on the glacier surface. The reference points were marked by wooden stakes driven into the firn. At each location, two squares were laid out in tandem as shown in Figure 3. The stakes had to be redriven after a 10-day interval because of the large ablation. The distances between the reference points were taped before and after redriving. For each square, the measurements give the normal strain in four directions at angles of 0, 45°, 90°, and 135° with the Y-axis (Figure 3). The X-axis is the direction of glacier flow, which is approximately S. 42° E. at this location.

Fig. 3.

Squares for strain-rate measurements

The measured strain-rates are summarized in Table 1. The two strain-rates in each direction are averaged to obtain the strain-rate in that direction for the area covered by the square. The results are checked against the theoretical relationship

which holds if the variation in strain-rate is linear within the area of the square. However, the values in Table 1 indicate that this may not be the actual case. At a1 and a2, the strain rates for the two halves of a square are very different and the quantity

is quite large. This suggests the possibility that the measurements are not reliable. However, if we compare the individual strain-rates at any location for the intervals 21 August to 1 September and 1 September to 11 September, we find a high degree of consistency. By means of repeated measurements it was concluded that the errors in taping do not exceed in. (3 mm.) which corresponds to a strain-rate of 0.07 × 10⁻⁵ hr.⁻¹. It is to be noted that with few exceptions the measured individual strain-rates during the two periods do not differ by more than 0.15 × 10⁻⁵ hr.⁻¹ at a1 and a2. It is therefore our conclusion that the measured values are reliable.

Table 1

Measured Strain-Rates (× 10⁻⁵ hr.⁻¹)

At points b1 and b2, the errors as measured by

are about the same order of magnitude as those at a1 and a2 but the strain-rates are much larger. However, considerable differences are observed between the individual strain-rates (a ₁, a ₂, b ₁, b ₂, …) measured during the two time intervals. These differences may be the reflection of the irregular crevasse movements.

The results from points d1 and d2 are difficult to analyze. The strain-rates changed considerably during the time intervals, especially at d2. Hence it is not possible to use the argument advanced for the measurements at a1 and a2 and we must admit that the measurements may not be dependable. The measured strain-rate at c1 is equal to zero. At c2 the distance changes measured during the two time intervals are about

in. (6 mm.). A substantial part of this is likely to be due to taping errors. Hence it is concluded that little or no strain exists at c.

Stresses and Crevasse Patterns

The measured strain-rates

are used to calculate the strain-rates in the directions parallel (X) and perpendicular (Y) to that of glacier flow (Figure 2). The best fit values of , by the principle of least squares have been shown to be (Reference NyeNye, 1959, Reference Nye1957 [b], p. 158–63)

Table II

Measured Principal. Strain-Rates (× 10⁻⁵ hr.⁻¹)

The major and minor principal strains

and their directions are calculated graphically by means of Mohr’s circle of strain. The angle between the X-axis and the vector is denoted by θ (see Figure 3 for sign). Assuming no volume change, the intermediate principle strain is determined by means of the relationship

The results of the calculations are given in Table II.

In order to obtain some indication of the general stress conditions in the glacier, the measured values are averaged to give an average strain-rate at each site. This is not done at d because of the erratic variations in the measured strain-rate. The stresses are calculated from the average strain-rates by the use of the relationship between stress and strain-rate obtained by Reference GlenGlen (1955) from laboratory creep tests on ice.

Reference NyeNye (1953) defined

and τ as follows

and

in which

and σ’ _ij are the components of the strain-rate and stress deviator tensors. The constants B and n are equal to 0.148 yr.⁻¹ bar⁻ⁿ and 4.2, respectively. The stress deviator is then obtained from the relationship

The principal stresses are

When the principal stresses are not in the X–Y directions, the stresses σ _x , σ _y and τ _xy are calculated by Mohr’s circle. The results of stress calculations are given in Table III.

Table III

Stresses Calculated from Measured Strain-Rates

Reference NyeNye (1952, Reference Nye1959) and Reference WardWard (1955, p. 594) have shown that crevasses in glaciers are the result of tensile stresses and that they run in a direction perpendicular to that of the maximum tensile stress. To compare the stress conditions with the crevasse patterns, the directions of the measured major principal strain-rates at a, b, and d are plotted as vectors in Figure 2, together with the directions of the crevasses. The general agreement is considered satisfactory. On the other hand, Reference MeierMeier (1958) observed at Blue Ice Valley, Greenland, that crevasses in firn form at an angle to the trajectories of maximum principal strain-rate. This does not appear to be the case on the Taku Glacier. It should be added that site is located in an area of numerous crevasses, many of them are 3 or 4 ft. (0.9–1.2 m.) wide and over 50 ft. (15 m.) deep. At sites a and d only a few crevasses are observed. These are only fine cracks in the snow that are noticeable only at very short distances.

Surface Velocity

The surface velocity was measured during the summer of 1962 along the same profile by triangulation with a theodolite (Reference MillerMiller, 1954). Figure 4 shows the velocity obtained at five points on two lines 500 ft. (152 m.) apart. The location of points 1 through 5 are shown in Figure 2. The velocity measured along the two lines are almost identical with the exception of point 4. The value obtained for point 4 on the center line (Figure 4) appears to be too small and is discarded in subsequent calculations. The average direction of the velocity vectors is S. 42° E. The velocity measurements also show very little movement near point c. Hence we come to the conclusion that the ice immediately adjacent to the valley walls is not moving at any observable rate.

Fig. 4.

Measured velocity along aa

To calculate the velocity in a glacier subjected to longitudinal tension, use is made of the plasticity solution by Reference NyeNye (1957[a]). For the stress-strain relationship given in Equation (3), the dimensionless velocity U is

in which T is the dimensionless shear-stress related to the dimensionless distance Y as follows

The dimensionless variables are

in which

The term n ₀ denotes the surface longitudinal strain-rate and β is the rate of change of τ _xy with y. In Nye’s case of vertical velocity distribution in an infinitely wide glacier, β is equal to pgx, the component of the gravity force along the bed, and y denotes the depth below the glacier surface. In the present case, equation (8) and (9) are used to calculate the horizontal velocity distribution. Then y denotes the horizontal distance in the direction perpendicular to that of glacier flow. The x direction is that of glacier flow.

To calculate the surface velocity distribution across the glacier we make use of the measured shear stress τ xy. It is 0.68 bar at B. If the shear stress varies linearly with y, τ _xy should be between 1.0 and 1.5 bars at the edge of the moving ice. The shear-stress distributions for these two cases are shown as solid lines in Figure 5b. With a longitudinal strain-rate of 0.550 × 10⁻⁵ hr.⁻¹, the calculated velocity profiles for X = 0, and τ _xy =1.0 and 1.2 bars at the edge are shown in Figure 5a as dashed curves. Since the velocity is very sensitive to the value of τ _xy , the agreement is considered satisfactory. Because of the great sensitivity of the velocity to τ _xy it is more instructive to compare the velocity distribution across the glacier rather than the absolute quantities. The velocity distributions for τ _xy equal to 1.0 and 1.5 bars assuming that the velocity at the center is equal to the measured value of 820 ft./yr. (250 m./yr.) are shown as solid curves in Figure 5a. The agreement with the observed velocity distribution is very close.

Fig. 5a.

Calculated and measured velocities

Fig. 5b

Measured and assumed shear stresses

The plasticity solution used in the longitudinal velocity calculation also gives a transverse velocity. (In Nye’s paper, this is the vertical velocity.) This transverse velocity is of the order of 200 ft./yr. (61 m./yr.) which is appreciable. Whether this velocity can be attained at this site is indeterminate at present because of the irregularities in the valley and the many small tributaries that join the Taku glacier.

Finally it must be noted that the values of B and n used in all stress and velocity calculations are those obtained by Glen in laboratory tests. Their general agreement with field values have been demonstrated by Reference NyeNye (1953). Nevertheless, considerable variations from these values are certainly possible as indicated by the bore-hole measurements of Reference MillerMiller (1958). Therefore, the calculated stress and velocity should be considered as reasonable approximations only.

Summary

The strain-rate measurements show that the glacier is subjected to a tensile stress in the longitudinal direction estimated to be about 1 bar. The shear stress between the glacier and the valley wall is of the order of 1.2 bars.

The measured strain-rates are in general agreement with the crevasse patterns and the measured surface velocity.

Several questions remain unresolved. First among them is the very erratic variations of the surface strain-rate. A problem yet to be investigated is the extent to which strain-rates measured on the firn reflect the actual stress and strain-rate in the glacier ice. Also, the effect of large crevasses on the surface strain-rate is not determined. As some of the crevasses are 50 ft. (15 m.) or more deep, nonhomogeniety is certainly introduced by their presence.

Acknowledgement

The measurements were made as a part of the Juneau Icefield Research Program during the summer of 1963. Funds for the activities were provided by the Foundation for Glacier Research and the National Science Foundation. The writers are grateful to the members of the 1963 expedition, particularly its director, Dr. M. M. Miller, for their co-operation that made this study possible.