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By Ekkehard Krätzel

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Dorrer (person­ al communication, 1980) suggests that small systematic theodolite turning errors may have been introduced to his traverse between R23 and R37, when appreciable friction was experienced in turning the alidade. Some of the data that we present in this paper have already been used to investigate the dynamics of parts of the ice shelf. 3 m y r " [Thomas and Bentley, 1978; MacAyeal and Thomas, 1979]. At the time of these analyses ice velocities in the (grid) east were not avail­ able, so some of the velocities, particular­ ly in the region between Crary Ice Rise and Roosevelt Island, were interpolated between the values of Dorrer et al.

Below this temperature, measurements could be made with the instruments enclosed within styrofoam-insulated boxes, but this tech­ nique was only partially successful. Fortu­ nately, temperatures on the Ross Ice Shelf during most of the field season (midNovember to late-January) are well above -20°C. 01 m for the CD-6 at the ranges involved in rosette measurement, was supported by field measurements every season of the same distance using each of the instruments. Although consistency be­ tween instruments does not provide a test of absolute accuracy, it does provide a suffi­ cient test of errors involved in the measure­ ment of strain, which is a change in length divided by a length.

1969] were made at 133 sta­ tions, but for the sake of clarity, they are not all included In Figure 11. Estimates of velocity based on comparison of astrofixes are of significantly lower accuracy, and they have not been included. The velocity at Little America V is from extrapolation of the RIGGS measurements, using the strain rates for LAV that were obtained by Crary [1961]. Our value is considerably larger than Crary's estimate, and there are small differences between our velocity estimates and those of Dorrer et al.

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