Chronology

In the course of the Filchner Ice Shelf Programme conducted by the Federal Republic of Germany — Filchner I (1983–84) and II (1985–86) operations — observations extended over two field seasons. A pattern of so-called raster points was planned at intervals of 100 km, both parallel and at right angles to the ice front. Velocity and strain data for the area between the ice front and Filchner Station were available from our measurements in the 1979–80 and 1981–82 seasons (Reference MollerMöller 1985). As far as it was possible logistically, the first set of observations was also carried out at intervals of 50 km. The planned Filchner III (1986–87) operation had to be cancelled because of unusual pack-ice conditions in the Weddell Sea. In the course of a substitute programme which had been planned for such an eventuality, Ekström Ice Shelf was surveyed. Similar measurements had been carried out near Georg von Neumayer Station since 1979–80.

Ice-flow velocities and directions

The absolute positions of the points marked with stakes were established with doppler satellite receivers, partly with reference to rock stations at Belgrano II and on Anvers Island, so that not only single-point solutions but also translocation calculations could be made for each season. In 1985–86, a Global Positioning System (GPS) receiver was used for the first time, as several GPS receivers were available for 1986–87, so that multiple-point solutions were also possible for these measurements. Evaluation of all the satellite observations was undertaken by the Institut für Erdmessung of the University of Hannover.

Strain parameters

The deformation figures (pentagon, rectangle and/or triangle) were established, using electro-optical distance measurement, direction observation and zenith-angle measurement. As a result of experience in earlier years, since 1985–86 new figures have only been put down as triangles with a double central point and have merely been observed from the central points. For the orientation of the figures and the establishment of the rates of rotation, gyro-and/or astronomical and magnetic azimuths were observed. An evaluation of all the deformation measurements has been made by the Institut für Vermessungskunde of the Technical University of Braunschweig.

Despite systematic simplifications of the figures in order to accelerate the measurements, a relative accuracy of 1–2 × 10⁻⁵ was achieved, so that strain parameters with relative errors of <1 × 10⁻⁴ a⁻¹ significance can be established from repeat measurements.

The results already available from Filchner Ice Shelf have been published (Reference Kock and WiegandKock and Wiegand 1986). Results from Ekström Ice Shelf are on the point of being completed. Figure 1 shows the principal deformation values for the area near Georg von Neumayer Station. The strain parameters here are one order of magnitude greater than on Filchner Ice Shelf. In Figure 2, preliminary values for the ice shelf are shown (Reference Hinze, Karsten, Lindner, Oswald, Ritter and TimmenHinze and others, in press). Figure 3 shows results for the area near the station, in accordance with an application of the collocation method developed byReference Kohler Köhler (1986). This method can also yield isopleths of speed and shearing for whole areas.

Least-squares collocation is a generalized estimation method that combines adjustment, filtering and prediction. In addition to the parameters, two sets of random variables are considered: the measuring errors (or noise) and another set, called signal; these random variables are related through their co-variances. This method can be applied, for instance, to various problems which arise in geodesy (Reference MoritzMoritz 1973).

Both on Ekström and on Filchner ice shelves, we were able to select observation points according to glaciological criteria from excellent maps produced by the Institut für Angewandte Geodäsie, Frankfurt, using Landsat data.

Heights

Height measurements on ice shelves are nowadays normally carried out together with position determinations by satellite methods (Transit, GPS) at points far apart from one another. As a figure of reference, an Earth ellipsoid (e.g. WGS 72) is used, and heights above the geoid cannot be derived without hypotheses. The accuracy of these heights may well be satisfactory for some purposes, but —for specific applications — heights above sea-level may be needed at closer intervals.

Fig. 1.

Fig. 1. Strain behaviour near Neumayer Station.

Fig. 2.

Fig. 2. Strain behaviour on Ekström Ice Shelf.

Fig. 3.

Fig. 3. Predicted strain behaviour near Neumayer Station.

In order to obtain heights above sea-level, the height of Filchner Station was established in 1979–80 by means of trigonometric levelling, and height transfers were later carried out for further points near the ice front. These ground measurements were also used to control the doppler heights. Errors of ²5 m or more were found for single-point solutions of the satellite data.

Exact heights above sea-level are, for example, used in:

glaciology, in the determination of mass balance on the basis of repeated strain and height measurements;

geophysics, in the reduction of gravimetric observations and in the interpretation of seismic measurements (strength of the ice, density–depth function);

geodesy, as a contribution to the establishment of geoid undulations.

Three methods of measuring height have been used on polar ice sheets up to now: barometric altimetry, trigonometric levelling, and optical levelling with horizontal sights.

Of these, trigonometric levelling fulfils most easily the requirements listed below:

daily rate of progress of work ≥30 km, with point intervals of approximately 1 km;

satisfactory height accuracy, ≤30 mm/km;

satisfactory positional accuracy of the measuring points, < 0.1 m/km;

ease of automatic indication and recording of all observations, and determination of the refraction relationships at the time of the observation.

The principle of motorized trigonometric levelling as applied in the Antarctic in the austral summer of 1986–87 is shown in Figure 4 (Reference Karsten and RitterKarsten and Ritter 1987).

Fig. 4.

Fig. 4. Measuring procedure for trigonometric levelling.

Two Nansen sledges pulled by Skidoos each formed a complete measurement and reflector base. On each of the sledges, an electronic theodolite (Wild Theomat Τ 2000) with an electronic distance measurer (Wild Di 5) was fixed to a heavy tripod. Above and below the theodolite there were combined targets for the distance and angle measurements at a constant interval. Instruments and targets could be levelled quickly by means of a ball-joint system. The values observed (slope distance, horizontal and vertical angles) were stored in an electronic data collector (Wild GRE) and, if necessary, could be written down. All equipment was fed from an external high-capacity 12 V d.c. battery. Reference stakes with further targets (K1, K2) were placed at a distance of 20–50 m from the sledge and sighted both before the start and after the finish of each measurement in order to check the stability of the sledge. The front sledge was not moved between a back-sight and a fore-sight after the rear sledge had advanced 2 km. The distance between two control stakes was always used for the redundant transfer of height and position between two observing days.

A decisive advantage of the measuring method was the reciprocal and simultaneous observation of zenith angles, so that alterations in refraction with time could have no effect. After reduction of the two observed zenith angles, z _u and z _d, to the height of the neighbouring theodolite, calculation of the differences in height and the coefficients of refraction was easily possible with the following equations:

whereby

further, Δh_ij represents the difference in height between the points i and j, s′ is the slope distance, z_ij is the zenith angle between instruments i and j, k is the coefficient of refraction, and r is the radius of the Earth.

The coefficient of refraction is defined as the relationship between the radius of curvature of the Earth (r) and the target beam (R).

In temperate latitudes, the coefficient is about 0.13 and is subject to alteration, depending upon the time of day, the weather, and the nature of the surface, averaging 0.05. Alterations in refraction up to a hundred times as much are, however, to be expected on sunny days over polar ice masses and, in the case of short-term alterations, it cannot be assumed that rays describe a circular path. If differences of refraction Δk are admitted, then Equation (equ.1) is given an additional element and becomes:

On the basis of Equation (equ.5), the following error influences can be derived for a transfer of height:

zenith-angle measurement:

measurement of distance:

differential refraction

In the case of a target distance of 1 000 m, we have for

m_z = 0.001 gon

m_s = 0.010 m

m_Δk = 0.5

m_Δk(z) = ²11 mm

m_Δh(s) = ²0 mm

m_Δh(Δk) = ²20 mm i.e. a total error influence of

The principal errors are introduced by the differences in refraction between neighbouring stations, so it is important in this context that times of observation with high and greatly differing coefficients of refraction are discovered immediately, in order either to reduce drastically the target distance or alternatively to stop measurements. From simultaneous evaluation of the differences in height a reliable indication of large coefficients or quick alterations with time can be obtained.

Fig. 5.

Fig. 5. Daily variation in refraction coefficient k during cloudy and sunny days.

The refraction conditions on Ekström Ice Shelf in the course of 4 d of measurement are shown in Figure 5. Two typical curves can be found:

the relatively constant course of the refraction on cloudy days, partly with white-out or with slight precipitation. k only exceeded the 1.0 mark occasionally after 17.00 (local Sun time) and Δk was probably smaller than ²0.5 at all times;

the coefficients of refraction, which increased and varied greatly after 17.00 on cloudless, windless days. Refraction jumped within a few minutes, and values > 6.0 led us to presume that the error estimate Δk < 0.5 could not be guaranteed.

The standard deviations of differences in height of neighbouring points at a distance of 1 km remained for the most part below ²25 mm. On a few occasions a standard deviation of around 50 mm was found. In accordance with the law of propagation of errors, the result was about ²0.60 m over the complete length of the profile, 220 km. The profile was recorded from 24 January to 1 February 1987. It runs from Atka Bay (70°36′S, 08°08′W) via Neumayer Station to drilling camp A (72°30′S, 09°06′W). In Atka Bay, the levelling was related to the height above actual sea-level. The section of the profile from Neumayer Station to camp A is shown in Figure 6. The transition from Ekström Ice Shelf to the ascent into Ritscher Upland at km 125 can be seen clearly. Numerous waves in the ice surface are, however, not shown clearly at this scale.

The positional determination was based on ten absolute positions with standard deviations of ²15 m in latitude and longitude.

Fig. 6.

Fig. 6. Height profile, Neumayer Station — Ritscher Upland.