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Pr62-3.Pdf (6.555Mb) The UNIVERSITY of WISCONSIN Geophysical & Polar Research Center'- DEPARTMENT OF GEOLOGY SUMMARY AND DISCUSSION OF THE GEOPHYSICAL AND GLACIOLOGICAL WORK IN THE FILCHNER ICE SHELF AREA OF ANTARCTICA by John C. Behrendt RESEARCH REPORT NO. 62.3-APRIL, 1962 Research Report Series Number 62-3 April 1962 SUMMARY AND DISCUSSION OF THE GEOPHYSICAL AND GLACIOLOGICAL WORK IN THE FILCHNER ICE SHELF AREA OF ANTARCTICA by John C. Behrendt The University of Wisconsin Geophysical and Polar Research Center 6021 South Highland Road The Highlands Madison 5, Wisconsin PREFACE This report contains a previously published discussion of the cal and glaciological geophysi- work on the Filchner ice shelf (Behrendt, 1962) to- gether with a tabulation of data and photo copies of representative seismic records for each of the reflection stations. ABSTRACT Geophysical and glaciological data collected during the IGY in the Filchner ice shelf area have been reported previously, and some of the se are included here to present a more unified picture of the region. A large trough underlies the eastern section of the ice shelf and extends into the unexplored area at its head. Although the trough is not iso- statically compensated locally, the area as a whole is essentially in isostatic equilibrium. The elevation of the M discontinuity is about -31 kin, which is consistent with that expected for a continental margin, Berkner island is a grounded ice feature on Berkner bank, which gravity data indicate is probably composed of morainal material. The eastern section of the shelf is flowing seaward at a high rate, and the amount of ice lost at the ice front is greater than accumulation on the shelf, I I I CONTENTS Page Introduction . .... * * . 1 . .. • . • . • . • Gravity Data Reduction ...... • . • . • . Presentation of Results .... 6 . .. • . • . • . • Discussion of Geophysical Results 6 . Crustal Studies ........ 16 • • . .. • ... • . Ice Shelf Regimen . ... 17 • • . .. .. • . Conclusions.. ....... ... 19 . •. .. • . Acknowledgments 20 . • . • . References......... .. 21 Appendix I ... ....... 23 Appendix II .......... 42 ILLUSTRATIONS Page Figure 1. Filchner ice shelf traverse route ............ 2 Figure 2. Ellsworth to Dufek massif, profile of principal facts . 4 Figure 3. Dufek massif to Korff island, profile of principal facts 5 Figure 4. Bedrock elevation, Filchner ice shelf area ...... 7 Figure 5. Surface elevation, Filchner ice shelf area ........ 8 Figure 6. Ice thickness, Filchner ice shelf area. ......... 9 Figure 7. Free-air anomalies, Filchner ice shelf area ... 10 Figure 8. Reduced free-air anomalies, Filchner ice shelf area . 11 Figure 9. Bouguer anomalies, Filchner ice shelf area ........ 12 Figure 10. Echo sounder profile, Bowman peninsula to Moltke nunatak 13 Figure 11. Comparison of AsG vs. Adepth .............. 15 Table 1. Seismic Results . .. .. .. INTRODUCTION Preliminary reports on the geography, sub-ice topography, and seismic, gravity, magnetic, and glaciological measurements carried out in the Filch- ner ice shelf area of Antarctica during the International Geophysical Year have been presented respectively by NeuburR, Thiel, Walker. Behrendt, and Auqhenbaugh (1959), Behrendt and Thiel (1959), Thiel and Behrendt (1959a, b, c) Aughenbaugh, Neuburg, and Walker (1958). In the present paper an attempt is made to integrate much of the published and unpublished materi- al collected during the IGY in order to present a unified picture of the Filchner ice shelf and its surroundings. Most of the data were gathered by the Ellsworth traverse party at Ells- worth station and on a 2100-km trek into the interior of the ice shelf during the austral summer of 1957-1958. Seismic and glaciological measurements were made at intervals of 40 to 50 km, and gravity, magnetic, and elevation obser- vations were made every 8 km. Figure 1 illustrates the traverse route and the locations of the seismic stations. Names marked with an asterisk have not yet been acted on by the Board of Geographic Names. Discussions of field pro- cedures and preliminary data reduction may be found in the above references. Ice thicknesses were calculated from seismic data, making allowances for near-surface low velocities and using a maximum P wave velocity of 3810 m/sec (Thiel and Behrendt, 1959f). At ice shelf stations a velocity of 1445 m/sec was used for the water section of the reflection path. At a few stations PS or SS reflections were obtained from the ice-water interface, permitting cal- culation of shelf thickness using an S wave velocity of 1910 m/sec (Thiel and Behrendt, 1959a). At most stations no reflection was obtained from the base of the float- ing ice, so the shelf thickness was calculated from the surface elevation using curves presented by Thiel and Ostenso (1961). Values obtained by the two methods agreed fairly well at stations where reflections from the ice- water interface were observed. The standard deviation in absolute elevation estimated from the reoccupation of six stations is + 18 m; relative errors between neighboring stations are probably much smaller. A positive error of 18 m in elevation would cause an error in ice thickness of +180 m and in depth to the sea floor of +110 m. Table 1 shows the vertical travel times, ice thickness, depth to bed- rock (i.e., sediments, till, or actual rock), and attitude of bedrock for the traverse stations. The reflection results are plotted along with other data in the profiles in Figures 2 and 3 and will be discussed more fully in a later section. Gravity Data Reduction A Frost low-drift gravimeter was used for the traverse observations. The base station at Ellsworth was tied to the world network in February 1959 using LaCoste and Romberg geodetic gravimeter No. 1; this instrument had a drift rate of 1 mgal/month and a world range (Behrendt and Woollard, 1961). Fig. 1. Filchner ice shelf traverse route. I m TABLE I Seismic Results Seismic Reflection Surface Ice Rock Attitude of Station Time. Elevation, Thickness, Elevation Rock Surface sec. +18 meters meters +40 meters Dip Strike 1 0.995 42 230 - 790 40S E -W 2 1.152 69 470 -1040 20 N N 520 W 3 1.349 72 500 -1200 4*E N 34 0 E 4 1.086 80 570 -1040 3*N N 72 0 W lS 5 1.124 73 510 -1040 N 750 W 6 1.359 86 620 -1270 4*E N 18OW 7 NR 74 520 -1010* 8 .355 599 680 - 80 4*E N 18 0 2*SW W 9 . 448 694 850 - 160 NW- SE 10 NR 153 660 - 240* 11 1.014 81 580 -1000 4*W N 70 W 12 1.334 96 670 -1270 6N E -W 13 1.382 90 660 -1310 4*N E -W 14 NR 275 400 - 610* 15 .212 523 400 - 120 230 W N 34"E 16 1.633 129 1040 -1680 7*W N 30*W 17 1.242 158 1310 -1540 40 E N 15 0 W 18 .866 131 1050 -1130 20 W N 360W 19 .461 224 850 - 630 20 NR 78 550 - 580* 21 .487 82 590 - 620 40 E N 60 W low 22 .462 77 540 - 580 N 220 E 23 .498 64 420 - 550 2 0 E N 22 0 W 24 ,300 400 570 - 170 0 25 NR 57 360 - 700* 0 26 .401 162 760 - 600 5 E N 36"W 27 .948 105 800 -1060 4*E N 14 0 E Gravity-determined rock elevation. +50 MGL. -r 0 -50 MGL. + IOOMGL. i +50 MGL.- +1000 M.- I 3 4 0 M.- ICE -*0 -1000 SEA M. WhTER ROCK BERKNER ISLAND OUFEK MASSIF Fig. 2. Ellsworth to Dufek massif, profile of principal facts. I-- I - +50 MGL. -50 MGL. 4IOOMGL. "+50MGL.- + 1000 M.- 1 11 is19 214 220 . 0 M. -1000 Iw DUFEK MASSIF MALVILLE PENINSULA KORFF 151AND Fig. 3. Dufek massif to Korff island, profile of principal facts. 6 Free-air anomalies were calculated for the 224 field stations. The Bouguer anomaly calculated at each seismic station included appropriate corrections for mass deficiencies between sea level and bedrock, assuming densities of 2.67, 0.9, and 1.03 g/cm3 for rock, ice, and water, respectively. In calculating the depth to bedrock for each gravity station free-air corrections were made for stations on floating ice, and free-air corrections, adjusted by a Bouguer correction from snow surface to sea level, were made for stations on grounded ice. Density differentials of 1.64 g/cm3 for water- rock and 1.77 g/cm3 for ice-rock give ratios of change in rock elevations to change in gravity of 14.6 and 13.5 m/mgal, respectively. The use of seismic reflection depths for control helped to eliminate errors caused by incorrect assumed density, terrain irregularities, or geologic change at depth. Presentation of Results Figures 2 and 3 show ice surface elevations, ice thicknesses, rock sur- face elevations, free-air anomalies, and Bouguer anomalies for the stations on the three legs of the traverse. These results have also been plotted on maps (Figs. 4-9) and contoured in an attempt to reveal some areal signifi- cance. In addition to the data from the Ellsworth traverse upon which most of this work is based, soundings from every other available source have been used, including two depths from the Ellsworth-Byrd 1958-1959 traverse, many from the ships Wyandot, Staten Island, and Edisto, extending over the period 1956-1959, and several from the Deutschland in 1912 (Filchner, 1922) and the Endurance in 1915 (Shackleton, 1919). Even with all the data available, the paucity of information has necessitated much extrapolation. Discussion of Geophysical Results The most striking feature of the profiles in Figures 2 and 3 is the deep trough underlying the thick ice of the eastern section of the Filchner ice shelf.
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