Paris Gletscher is a medium-sized outflow glacier from the Greenland ice sheet (lat. 66° 45′ N., long. 36° 45′ W.) in the Angmagssalik district of East Greenland. The glacier flows through the mountains near Mont Ford down to the ice basin of Femstjernen (Fig. 1). The glacier was inferred to be polar in character with only a small seasonal layer near the surface reaching freezing-point temperatures, as it was observed that there was no evidence of any subglacial drainage and that many crevasses were filled with water which did not drain away. The polar nature of the glacier was also indicated by the low value of ice resistivity found (Reference Meyer and RöthlisbergerMeyer and Röthlisberger, 1962).

Fig. 1. Map of Paris Gletscher, East Greenland. The stakes used for the surface flow studies were surveyed from the base camp and the station to the north. The resistivity profile was measured just east of the outermost stake line.

Observations on the glacier were concentrated in an area on the east side of the valley north-west of Quervain Bjwrg (Fig. 1). In this area the surface was level transverse to the flow and it had a slope of about 3° up-glacier. The surface was relatively crevasse-free with only small narrow crevasses less than 15 cm wide and 100 m apart being present. Measurements were made of the glacier flow and electrical resistivity (D.C.) during August 1966 when the surface of the glacier consisted of a layer of loosely packed crystalline snow about 30 cm thick over waterlogged packed firn. Observations of ablation during the summer of 1966 and of net ablation over the year 1966–67 showed that the observation area was just below the firn line at the end of the ablation season in 1966.

Surface-flow measurements were made by observing the displacement of a grid of stakes drilled into the glacier. The stakes were surveyed from two stations established on rock on the east side of the glacier (Fig. 1). Measurements were made over a 10-day period in August 1966 and the stakes were re-surveyed in August 1967. The average velocities of the stakes during the summer of 1966 and the year 1966–67 are given in Table I. The measurements indicate that apart from minor variations the flow down the glacier was uniform over the area of measurement, except for the eastern line 4, 8, 12, which shows retardation due to the rock walls. The mean flow velocities for the year 1966–67 show that there were no seasonal variations in the velocity, probably due to the fact that observations were made near the firn line on a polar glacier.

Table 1. Surface-flow Velocities Down-stream (m/d)

Ice resistivities were measured along a profile parallel to the prominent medial moraine about 200 m to the west. As the general techniques of ice-resistivity sounding have recently been discussed (Reference RöthlisbergerRöthlisberger, 1967), the basic details will not be given here. Current from a 720 V dry battery was passed through electrodes of 2 cm diameter dural tube hammered 30 cm into the underlying firn. The current was measured by a 50 μA Avometer and voltage on a battery-operated high-impedance valve voltmeter (Airmec type 314). An insulation check of the wiring showed that leakage currents were less than 0.1 μA.

Ground potentials up to a maximum of 300 mV were found. These were not steady but varied by as much as 20 mV during an observation. In most cases the ground potential could be allowed for by making a measurement of its value before and after switching on and off the current. However, at large electrode separations the signal voltage was of the same size as the ground-voltage fluctuation. A series of readings was therefore taken with the current electrode region saturated with brine in order to increase the input current.

Measurements were made with the Wenner electrode system. The apparent resistivity/electrode separation curve is shown in Figure 2. It can be seen that at large electrode separations there is a divergence between the results obtained with plain and electrolyte-immersed electrodes. The results with the large current obtained with brine-saturated electrodes are believed to give the correct curve as errors due to the fluctuations in ground potential were significant in the low-current case at this separation. The divergence at small separation was shown to be due to the surface conditions. In Table II measurements made with a wet snow surface during the day are compared with values from a frozen surface during the night. It can be seen that the resistivity of the frozen surface was significantly greater than that of the wet one.

Fig. 2. The measured resistivity profile is shown both for the unsalted (low current) and salted (high current) electrodes. The deviation at large electrode separations is due lo errors introduced by fluctuating ground potentials in the low-current case. Comparison is made with the computed curve for the four-layer system shown.

Table II. Apparent Resistivity (kΩm)

From Figure 2 it can be seen that the curve has three points of inflexion, indicating a four-layer structure of the ice. The measured profile was compared with the set of master curves of the Compagnie Générale de Géophysique (1955). The transformation of the curves to the Wenner configuration was made using the factor 1.4.Footnote * The best-fit four-layer curve is shown in Figure 2. The first layer, 12 m thick, is thought to be due to the waterlogged firn. The next layer, only 2 m thick but of high resistivity, is assumed to be ice at or just below freezing point; the high resistivity found is comparable with values obtained in measurements on temperate glaciers (Reference Röthlisberger and VögtliRöthlisberger and Vögtli, 1967). The bulk of the ice has the typical low resistivity found in polar glaciers (Reference Meyer and RöthlisbergerMeyer and Röthlisberger, 1962; Reference VögtliVögtli, 1967). There is some evidence that the resistivity decreased slightly with depth but not to the extent found on ice sheets (Reference HochsteinHochstein, 1967). At the base of the glacier, instead of the low resistivity expected of the rock bed (≈10⁴Ω m), a layer of high resistivity (>1 M Ω m) was found at a depth of about 420 m. The origin of this layer was not understood but it is presumably the same feature as that found by Reference Meyer and RöthlisbergerMeyer and Räthlisberger (1962) in north-west Greenland.Footnote †

The surface-flow results show that in the observation area the surface strain-rate was zero. In this case, Reference NyeNye (1952) has shown that, provided the depth is much less than the glacier width, the surface velocity (Vs) in the centre of the glacier due to shear slip is given by

where α is the surface slope of the glacier, h the depth, V _b the bed-slip velocity, and k and n are the constant and exponent in Glen’s law for ice shear (Reference GlenGlen, 1955).

Unfortunately, as the bed-slip velocity V _b is not known, this relation cannot be used to give an accurate value of h. However, as V _s is a rapidly varying function of h, the value of the depth calculated from the above expression should be accurate to about 10% provided the proportion of bed slip contributing to the flow is less than 40%.

Using the values of k and n found by Reference Butkovich and LandauerButkovich and Landauer (1958) for ice at −5° C, the depth of the glacier is found to be about 450 m. There is a fairly large error in this result, however, as the slope of the glacier surface is only approximately known. Nonetheless, it does indicate that the identification of the high-resistivity layer at 400 m with the base of the glacier is justified, although the actual magnitude of the resistivity is considerably in excess of that anticipated for the rock bed.

The resistivity technique shows that Paris Gletscher is basically a four-layered structure. The first two layers to a depth of 14 m correspond to the seasonal variation in temperature near the surface. The bulk of the glacier is below freezing and has a conductivity much higher than that of the ice near the freezing point. At the base of the glacier a layer of high resistance is found, which is not thought to be due to the underlying bedrock.