Introduction

Urumqi Glacier No. 1 is an extra-continental type glacier, sometimes classified as a sub-polar glacier. It is located in the hinterland of Eurasia at 43°06′N, 87°15′E. Its equilibrium line is at about 4050 m a.s.l., where the annual precipitation is about 550 mm water equivalent and the mean annual temperature is −10°C. It is a small cirque-valley glacier, 2.2 km long, and is both retreating and thinning.

Glacier-flow measurements, which began in 1959, have shown that the velocity is decreasing, e.g. the velocity averaged for May 1980 to May 1981 had decreased by 31–73% compared with that for 1959–62 (Reference Zuozhe, Yaowu, Genxiang and JiankangSun and others, 1985).

Some observations on glacier dynamics have been made since 1980 with the aim of investigating the flow mechanisms of continental-type glaciers. Reference Echelmeyer and ZhongxiangEchelmeyer and Wang (1987), Huang and Wang (1987), and Reference EchelmeyerEchelmeyer (1987) have described their observations which were made in a tunnel excavated close to the glacier bed at an elevation of 3820 m. We should now like to present some new results for this glacier.

Surface Areal Strain-Rate

Fifty-four points, where surface velocity was measured, were distributed over the glacier, which has an area of 1.84 km². By using the processing method of Reference Meier, Kamb, Allen, Sharp and WashingtonMeier and others (1974), we can draw a map showing the distribution of surface strain-rate and the isopleths of surface areal strain-rate for the glacier. Figure 1 is one of these maps based on the survey data for the period 19 May 1980–18 May 1981. Data for the horizontal flow velocity were used and the vertical components were eliminated. The error in the strain-rate is generally estimated to be ±0.25 × 10⁻² a⁻¹ but it is ±0.5 − 10⁻²a⁻¹ at the margins. As shown in Figure 1, zero isopleths for surface areal strain-rate occur in both the eastern and western branches of the glacier; up-stream of these isopleths, the areal strain-rate is positive and down-stream it is negative, i.e. up-stream there is extending flow and down-stream there is a compressive-flow area.

Fig. 1.

A map showing the distribution of surface strain-rate and isopleths of surface areal strain-rate on Urumqi Glacier No. 1. An ice tunnel and three sites of temperature measurement are also shown.

However, these isopleths do not coincide with the equilibrium lines. They are roughly parallel to, but below, the equilibrium line. In the compressive-flow area, there are some local zones of extending flow, e.g. there is a positive areal strain-rate zone in the middle part of the western branch, at the top of a steep section of the glacier. The maximum areal strain-rate does not occur at the terminus but at the bottom of the steep section of the glacier. The maximum shear strain-rate occurs at the outside of a bend, particularly the bend in the western branch, where many crevasses have formed.

Ice Temperature

Ice temperatures in Urumqi Glacier No. 1 have been measured in detail; Huang and others (1982) have summarized measurements up to 1978. Since then, Ren and others (1985) have made more detailed measurements. In the ablation area, the ice temperature is quite low in the active layer but it increases rapidly downwards. Huang and others (1982) have pointed out that, in many small-scale glaciers, such as Urumqi Glacier No. 1, the temperature at the base of the active layer is generally higher than the mean annual air temperature at the same elevation, whereas the ice at the base of the glacier is usually at the melting point. By extrapolating from data obtained from depths of not more than 35 m, Ren and others (1985) have concluded that the temperature at the base of the glacier is at the melting point at some places but not at others. Huang and Wang (1987) published the ice-temperature data measured in the tunnel (Fig. 1); these show that the ice temperature below the floor of the tunnel is close to but not at the melting point. In addition, in September 1983, they observed water springing up from a hole in the tunnel floor. In the period September-November 1984, Reference EchelmeyerEchelmeyer (1987) measured the ice temperature in a lateral shaft connected to the main ice tunnel. A basal temperature gradient of 0.3 K. m⁻¹, more than an order of magnitude greater than the geothermal gradient, was recorded in the shaft, where the ice thickness is about 22 m. Echelmeyer believed that ground water flowing beneath the glacier is responsible for this large basal temperature gradient, and he calculated that there is a subglacial upward heat flow of 0.6 W m⁻², which requires a water flux of about 0.1 m³s⁻¹ over the 400 m width of the glacier.

In July 1986, three holes were drilled with a hot-water drill in the lower and middle parts of the ablation area and near the equilibrium line in the eastern branch of the glacier, respectively, for the measurement of ice temperature (Cai and others, 1987). The sensors had an accuracy of ±0.05 K. The elevations at the tops of the holes were 3854 m for T₁ 3928 m for T₂ and 4033 m for T₃ (Fig. 1). The depths of the bore holes were 86, 102, and 106 m, respectively. According to radar sounding, the maximum ice thickness is 140 m in the eastern branch of the glacier, and at T₁, T₂, and T₃ the thicknesses are 96, 138, and 106 m, respectively (Zhang and others, 1985). Therefore, bore hole T₃ reached the base of the ice and T₁ was close to it. For T₁, T₂, and T₃, the net mass balances are −1, −0.5, and 0 m a⁻¹, respectively. The temperature profiles measured on 8 August 1986 are shown in Figure 2.

The temperatures at a depth of 20 m and at the bottom of bore holes at the three sites are listed in Table 1. The temperature gradients from a depth of 20 m to the bottom of each bore hole and the gradients in the lowest 20 m of each bore hole are also shown.

Fig. 2.

Temperature profiles measured on 8 August 1986. The dotted line is and extrapolation.

Table 1

Temperatures (t) and temperature gradients (dt/dz) for the three sites

From Figure 2 and Table I, we can see that the temperature gradients in the upper layer are greater than those in the lower layer. Apart from the ice flowing upward towards the surface, carrying warm basal ice with it, Cai and others (1987) have suggested that the up-stream temperature significantly affects the down-stream temperature by means of horizontal conduction and advection. Generally speaking, the mean temperature gradient from a depth of 20 m to the bore-hole bottom is two to three times greater than the geothermal gradient. But the mean temperature gradients of the lowest 20 m of the bore holes are less than this and agree with what Echelmeyer (1987, table 2) had calculated. For the prescribed temperature conditions at the surface Τ = −10°C, the net mass balance b = −1 to −2 m a⁻¹, and glacier thickness H = 100 m, he had calculated that (dT/dz)/(dT/dz)_e = 1.1–2.2, where (dT/dz)_e is the geothermal gradient (= 0.023 Κ m⁻¹). On the basis of the temperatures at the bottom of the bore holes and the temperature gradients in the lowest 20 m (Table I), we believe that in the middle and lower parts of the ablation area the temperature at the base of the glacier will be close to (e.g. at T₁) or at (e.g. at T₂) the melting point. But the temperature at the base of T₃ is −1.8°C, which implies that above and around the equilibrium line the glacier is frozen to its bed.

Deformation of Ice

In the tunnel, there is clear bulk ice above the layer of ice-laden subglacial till and its deformation was observed regularly in both 1983 and 1984.

Inhomogcncity

Inhomogeneous deformation of the ice was observed from 18 January to 13 November 1984. Two circular peg arrays, A_r and A_l, for observing deformation were fixed on the southern and northern walls at section A in the tunnel, and five circular peg arrays, D-1, D-2, …, D-5, were fixed on the southern wall at section D of a lateral shaft connected with the tunnel. The locations of the arrays are listed in Table II. Each array comprised 17 pegs frozen into the ice. Among them, one is the origin (0), eight (I₁,I₂,…, I₈) form a circle 400 mm in diameter centred on the origin, and the other eight (J₁, J₂, …, J₃) form another circle 600 mm in diameter for section A, and 700 mm for section D, centred on the same origin. The angle between adjacent pegs in each circle is 45 (Fig. 3).

We can subdivide each array into several elements and determine the deformation ellipse for each element, on the two assumptions that the deformation in a particular element occurs in the principal plane and is homogeneous.

Three series of elements can be distinguished: one is composed of eight triangles (0 I_i I_i+1 (i = 1–7) and 0 I₈I₁), another one of eight triangles (0 J_i- J_i+1 (i = 1–7) and 0 J₈ J₁), and a third one of eight quadrilaterals (I_i J_jJ_i+1 I_i+1 (i= 1–7) and I₈ J₈ J₁ I₁). The deformation ellipses for these elements also form three series denoted (Ε_1i, Ε_2i, and E_si (i = 1–8)). A deformation ellipse can be characterized by its major axis, minor axis, and principal direction. For any series of ellipses, there are both the average values and the standard deviations of the major axis, minor axis, and principal direction (Table III). The standard deviations are used to assess the inhomogeneity of deformation. From Table III, we can see that for section D, where the strain-rate is smaller, the standard deviations (representing the inhomogeneous component of deformation) are not significant and hence the deformation is homogeneous. But this is not the case for section A at the margin of the glacier, where the shear strain-rate is greater.

Table 2

Locations of observed arrays, 1984

Fig. 3.

Circular peg array for observing inhomogeneous deformation, together with three series of elements for calculating deformation ellipses.

Table 3

Average values and standard deviations of major axes (a), minor axes (b), and principal directions (α°), for deformation ellipses, 1984

Table 4

Average values of major axis (a), minor axis (b), principal directions (α, °) and rotation of principal axis (ω, °/year) for deformation ellipses, 1983

Summary

Urumqi Glacier No. 1 is a small extra-continental type glacier. The zero isopleth of surface areal strain-rate is roughly parallel to, but below, the equilibrium line. In the ablation area, the ice temperature is quite low in the active layer but it increases rapidly with depth. In the middle and lower parts of the ablation area, the basal temperature is close to or at the melting point, whereas above and around the equilibrium line the glacier is frozen to its bed. Above the ice-laden subglacial till there is clear bulk ice, which is deforming continuously and inhomogeneously, but in the inner parts of the glacier, where the strain-rate is smaller, the inhomogeneous component of deformation is not significant, so that homogeneous deformation can only be assumed conditionally. However, this is no longer valid at the margins of the glacier, where the shear strain-rate is greater. In the ablation area, pure shear is predominant near the base of the glacier and simple shear becomes progressively more important as the ice moves out towards its margins.

Acknowledgements

The authors wish to thank Dr W.S.B. Paterson for his comments and for a critical review of this paper.