Program Leader's Progress Report for Glaciology to the Antarctic Science Advisory Committee for the 2000-01 Antarctic Season

Research Output achieved against the strategic plan

[Numbers in square brackets refer to Assessment Milestones]

Shallow firn cores were collected from the Hallett peninsula 72 30.5 S, 170 05.6 E, in Northern Victoria Land, as part of a US-Australian collaborative project, and from the Amery Ice Shelf to determine the spatial and recent temporal variability of snow accumulation and other environmental parameters  These CORES contribute to the SCAR-ITASE program. [4]

Field studies of solar radiation processes in the pack and their role in the summer decay of the ice around 110°E were undertaken in conjunction with US collaborators during a 2000/01 cruise.  Measurements were made of the spectral albedo of sea ice from 320 to 2000 nm and of the vertical transmission profiles of diffuse radiation through the ice.  Spectral transmission through sea ice in seven wavebands (410, 440, 488, 510, 555, 650 and 676 nm) were also made and correlated with core salinity, chlorophyll concentration, particle concentration, particle size distribution (from 1.25 to 250 mm diameter). The combination of these measurements allows solar radiation incident on the snow/sea ice system to be partitioned into reflected, absorbed and transmitted fractions. [5, 6]

Major Research Output(s) completed in 2000-01 relating to previous seasons' activities

Not relevant

Research/Activities in the 2000-01 strategic plan NOT achieved and why

Investigation of the relationships between sea ice properties and biological processes during springtime were to be undertaken during the Ice-T project, which was cancelled.  Some of the proposed Ice-T activities were rescheduled for V3 2000/01, but these could only be partially completed because the ship became beset in heavy ice.  Although some activities have been further rescheduled for V1 2002/03, no comprehensive and integrated field programs that will completely address Milestones 5 and 6 are proposed for the next several years.

Goal 3 - To Understand the Role of Antarctica in the Global Climate System

Glaciology:  The Antarctic plays a significant role in global climate through interactions of ice and snow cover with the ocean and atmosphere.  Cryospheric feedback processes influence global climate response to change.  Variations in the extent of snow and ice may be linked to major components of climate variability.

Snow and ice masses are integrators of processes within the climate system, and can also be sensitive indicators of change in that system. Sea ice and sub-Antarctic glaciers are very sensitive to temperature variations because surplus energy is used for melting.  Their extent and thickness provide a strong climate signal.  In contrast, snowfall in the interior of the Antarctic undergoes little ablation and the ice sheet forms a natural sedimentary archive containing a detailed record of past changes in temperature, precipitation, and atmospheric chemistry, composition and circulation.

Key Scientific Outputs

Determine the roles in the global weather, climate and ocean circulation systems, of the Antarctic ice sheet, ice shelves and sea ice on atmospheric and oceanic circulation, and on the carbon cycle.  Contribute to the development of appropriate treatments of these processes and interactions in global and regional climate models.

Assessment Milestones

7. Improved meso-scale sea ice models of the Mertz Glacier Polynya (MGP) compared against field data.  Assessment of the impact of the MGP on Adelie Bottom Water production (2003).
8. Assessment of the links between Antarctic sea ice variability and Southern Hemisphere weather (2004).
9. Improved treatment of sea ice processes in fully coupled global climate models and high-resolution limited area models.  Assessment of the sensitivity of Antarctic sea-ice to global warming from the fully coupled models (2005).
10. Completed research utilising measurements within hot water drill holes on the Amery Ice Shelf of ice temperature, melt/freeze rate at the ice/ocean interface, ocean temperature, salinity and currents, etc (AMISOR) (2005).

*******************************

Determine the extent to which the Antarctic ice sheet and individual drainage basins are in balance with the present climate, using field and remote sensing techniques.  Determine the influence of ice shelves on ice sheet dynamics, and hence on this balance, and their interaction with the underlying ocean.  Determine whether, and over what time scale, global warming might lead to irreversible change in the ice sheet - ice shelf systems.

Assessment Milestones

• Assessment of the mass budget of different sectors of East Antarctica, using field and remote sensing measurements and models (coupled with atmosphere/ocean climate models) (Ongoing).
• Physical characteristics of the Amery Ice Shelf - Lambert Glacier system assessed.  Simulations of the present state of the Amery Ice Shelf and the sub-ice shelf ocean cavity computed using an ice sheet-ocean coupled model; and the responses of the system to future climate change predicted (2003).
• Changes over Ice Age cycle time-scales in the Lambert Basin-Amery Ice Shelf drainage system determined using a coupled ice sheet-ice stream-ice shelf model, and results compared with geomorphological evidence of past extent of the Lambert Glacier-Amery Ice Shelf system (2003).
• Relationships established between past changes in the Law Dome ice cap and ice core inferred paleoclimate parameters, by using a high-resolution dynamic/ thermo-dynamic computer model (2004).
• Inputs to Antarctic ice sheet palaeoclimate modelling improved by simulations through several Ice Age cycles of the variations in the major ice sheets, using global palaeoclimate records and climate models controlled by the cyclic orbital variation of insolation (2005).

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Produce, from study of ice cores, records of past climatic and environmental variables.  Construct proxies for climate processes and interpret the records to better understand climate dynamics, and especially climate change.

Assessment Milestones

16. High-resolution records of ice core chemistry covering the last 1,000 years at Law Dome (2001).
17. Low-resolution ~100,000 year stable isotope proxy record of climatic temperatures at Law Dome, dated by trapped gas and other measurements (2001).
18. Extension of the high resolution Law Dome climate record temporally to about 2,000 years before present, and spatially by analysis of new cores from sites removed from Law Dome (2003).
19. Results from calibration and verification studies showing connections between climate forcings and observed data (2005).

*******************************

Monitor the spatial extent and surface properties of the snow and ice cover in the Antarctic, sub-Antarctic and Southern Ocean in order to identify changes in the Antarctic environment.

Assessment Milestones

20. monitor and detect change in Antarctic and Southern Ocean climatic parameters, eg.  air temperature and pressure, sea ice characteristics (including extent, thickness including snow cover, concentration and drift from buoys and from satellite techniques), and icebergs (including production rate, spatial distribution and dimensions derived from remotely sensed data and from ship based observations, drift rates and dissolution rates) (Ongoing).
21. Update climatology of inter-seasonal variability in fast ice extent and thickness, derived from Synthetic Aperture Radar and station-based measurements (Ongoing).
22. Records from satellite data, of the spatial distribution and natural variability of snow temperature, snow accumulation rate, surface melt, etc., and interpretation in the light of known climate fluctuations from other sources (Automatic Weather Station, ice cores, stratigraphy) (2005).
23. Monitor and analyse fluctuations in the physical characteristics of the ice sheet, ice shelves and glaciers, including the Heard Island glaciers to determine their response to climate change in the Antarctic and sub-Antarctic (Ongoing).

Research Output achieved against the strategic plan

[Numbers in square brackets refer to Assessment Milestones]

Sea Ice

A High Resolution Antarctic Limited Area Model is under development based on the CSIRO Limited Australian Limited Area Model.  This has a horizontal resolution of 127 km x 127 km, with 18 sigma levels in the vertical in the atmosphere. The model is a two-time-level, semi-implicit, hydrostatic primitive equation model and uses one-way nesting.  This will be coupled with a sea ice model including ice dynamics with complex rheology.  The model will be initially used to simulate the Mertz Glacier Polynya region, driven by ECMWF analyses for 10 years (1990-1999). [7]

Assessment of the sensitivity of Antarctic sea ice to global warming is also being undertaken using the CSIRO fully coupled global climate model, Mark 2 version. To examine the global warming over the past century and climate change in the future, the CSIRO coupled global climate model (atmosphere, ocean and sea ice) was forced with several increasing greenhouse gas scenarios over the past century and into the future.  The CSIRO model was started from 1880 AD. Although global changes are simulated, the focus of the study was simulation over the southern hemisphere and particularly the Antarctic region. The modelling results show reasonable agreement for the changes over the southern hemisphere for the past century, and future changes which include surface warming, increase of precipitation and evaporation,retreat of Antarctic sea ice, and reduction of Antarctic Bottom Water formation. The reduction in Bottom Water formation in both polar regions leads to a stagnant deep ocean before the end of the 21st century. Many of the changes continue towards the end of the 21st century even with a limit of double pre-industrial equivalent CO2. [9]

Amery Ice Shelf

AMISOR (Amery Ice Shelf - ocean research) is an 'umbrella' research project of the Antarctic CRC, AAD, and CSIRO Division of Marine Research aiming to investigate the interaction between the Amery Ice Shelf and the ocean.  The AMISOR project consists of both oceanographic and ice shelf field components, and numerical modelling.  The oceanographic component [Oceanography Program] includes detailed hydrographic sections across the front of the AIS of the characteristics and flow of the seawater entering and leaving the ocean cavity beneath the shelf.  The first of these measurements were made during the 2000/01 summer.  Ten instrumented oceanographic moorings were also deployed across the front of the shelf to record ocean salinity, temperature, current and sea ice thickness variations over a seasonalcycle. The ice shelf component of AMISOR used a new hot water drilling facility to penetrate through 373-m of ice into the ocean cavity in January 2001.  CTD measurements through the hole show that the top 40-m of the 440-m deep cavity beneath the shelf is a relatively fresh layer derived from basal melt under the shelf.  Instruments were deployed through the borehole and will be maintained for several years.  Sediment cores were collected from the ocean floor both through the borehole and at a number of locations off the front of the shelf to determine a history of ice shelf variability. [10]

A variety of different techniques combining numerical modelling and remote sensing have recently demonstrated that the Amery Ice Shelf (AIS) is floating as far south as 73.2°S.  Mass balance estimates for the AIS have been made using a variety of independent techniques including ground survey, numerical modelling, and remote sensing.  All show similar results with rapid basal melt (up to 30 m/a) under the deep parts of the shelf near the grounding zone and some subsequent refreezing of marine ice under the north east region of the shelf.  This pattern is also shown in basal melt-freeze rates derived from a sub ice-shelf/ocean circulation model. The marine ice accretion, which has maximum thickness of 190 m, has been confirmed and mapped using a novel technique combining a satellite derived DEM with airborne RES data.  There is a net loss by basal melt of up to 50% of the total ice discharged across the grounding zone, a result supported by measurements that quantify changes in the heat and salt content of water flowing across the front of the shelf. [11]

Horizontal velocities, strain rates and vertical movement on the Amery Ice shelf have beencomputed from terrestrial survey and GPS data. A new tide model, assimilating the GPS data time series, has shown the sensitivity of the model to knowledge of the ice thickness and geometry of the underlying ocean cavity. Continuous GPS measurements are being made to provide an accurate calibration baseline of the AIS for the coming Geoscience Laser Altimeter System (GLAS), to be launched on the Ice, Cloud and Land Elevation Satellite (ICESat). [11]

An improved numerical model of ice shelf dynamics has been applied to the Amery Ice Shelf.  Using measured ice thickness data the model provides good agreement with observed ice velocities for the northern region of the Amery Ice Shelf, but some further model development is needed to improve the results for the southern region. Model simulations of ocean circulation and ice-ocean interaction, with a more sophisticated treatment of the ice-ocean interface than previously used, suggest that the Amery Ice Shelf loses between 6 and 18 Gt (Gigatonne) of ice each year by basal melting. Model investigation of the response of the Amery Ice Shelf to changes in the climate of the Southern Ocean show that net basal melting would increase by 28.4 Gt per year per degree C of warming.  As the total ice flow into the Amery ice shelf is around 57 Gt per year this suggests that ocean warming would cause a substantial modification to the ice shelf, particularly near the grounding line.  New models of the ocean circulation in the ice shelf cavity are under development. [12]

Ice sheet Mass Balance

Techniques have been developed to measure ice sheet movement rate from satellite data.  For example more than 50,000 velocity vectors have been derived along the Lambert Glacier - Amery Ice Shelf.  A new, high precision baseline map of the coastline between 40°E and 160°E (both grounding line and edge of contiguous meteoric ice) has also been produced from Landsat 7 and Radarsat data. [11]

Development of the time dependent dynamical/thermodynamical ice sheet model is continuing and will be applied to the whole Antarctic and Greenland ice sheets.  Work on analysing the incorporation of the influence of anisotropic ice crystal fabrics in the treatment of ice deformation flow in computer models has demonstrated the importance of anisotropy to explaining the ice flow rates measured in the bore hole at Dome Summit South, on Law Dome, East Antarctica.  An inverse ice sheet model has been used to derive the bedrock elevation for those parts of Antarctica where there are no data.[14]

Ice Core Palaeo environmental records

High-resolution measurements of key atmospheric gases through the Holocene and into the glacial transition are also being made on the DSS and other cores.  Interpretation uses modelling tools developed at CSIRO such as the air diffusion and enclosure model, and the carbon cycle model. This work focuses on natural variability during several periods in the pre-industrial Holocene, such as 8.2 Kyr BP.  Emphasis is on the fine age resolution of the air in Law Dome ice and firn that is unique for the Holocene. [16]

Chemical measurements on ice cores from the Law Dome Summit show statistically significant correlations between MSA concentration and sea-ice extent, suggesting that future work may provide a useful proxy of sea-ice extent. [16]

Measurements of stable isotope ratios, which provide a proxy temperature record, have been completed over the full 1200 m length of an ice core from the Law Dome summit south (DSS), near Casey.  The record from this core extends back 140,000 years in the past, to the warm period before the last great ice age.  The temperature record over the full time period shows a very similar trend to that in the Vostok ice core, but the Law Dome record is of very much higher resolution over the last 20,000 years.  This permits investigation of the transition from the last ice age into the present warm period, and very detailed study of climate fluctuations over the last few thousand years. DSS data reveal significant timing differences between a northern climatic cooling, the Younger-Dryas event, and the Antarctic Cold Reversal in the Southern Hemisphere temperature. Analyses of the Law Dome deep ice core have provided a record of past volcanic activity, and demonstrated potential techniques for recovering records of past sea ice extent, and past solar proton events from the trace chemical record in the core. [18]

Shallow core and pit studies samples were collected at the site of the Law Dome summit Automatic Weather Station (which includes a snow accumulation sensor) in 1999/2000. Specific precipitation events under observed meteorological conditions were identified in the samples and used to improve the calibration of the ice-core/climate transfer function. [19]

Cryospheric Monitoring

Drifting sea ice data buoys with sensors to measure meteorological and oceanographic variables are deployed each season as a contribution to the International Antarctic Buoy Programme. Two buoys were deployed in the 2000/01 season at 67 59.2 S, 76 43.4 E and at 65 07.6 S, 109 40.1 E.  [20]

East Antarctic sea ice motion derived from drifting buoys has been compared with velocity fields derived from 37 and 85 GHz satellite passive microwave data. Comparison of the mean distributions of daily velocity derived from the two data sets shows that while the velocity patterns agree well, the magnitude of the satellite derived sea-ice velocities is typically about 50 to 80% lower than for the velocities derived from buoy measurements. This difference occurs largely because the satellite-derived field represents the large-scale ice motion and buoy-derived field represents point measurements. [20]

Upward looking sonar buoys which monitor the keel depths (and hence estimate ice thickness) of pack drifting overhead) were deployed off the front of the Amery Ice Shelf in March 2001 in support of AMISOR.  These contribute to the Antarctic Sea Ice Thickness Program (AnSITP) . [20]

Procedures have been developed to improve the automatic derivation of shape and size characteristics of icebergs in satellite SAR images. A total of more than 20,000 observations of iceberg size have been extracted by analysis of Synthetic Aperture Radar images acquired by ERS-1, ERS-2, and Radarsat satellites. These observations span the entire coastal sector between longitudes 70°E and 135°E. They represent the first systematic survey of iceberg distribution and size characteristics along a large sector of the Antarctic coastline close to the sources of the icebergs. [20]

A network of more than 15 automatic weather stations continues to provide surface meteorological data from remote regions of the east Antarctic ice sheet.  Current and historic data from these are being made publicly available via the Internet in netCDF format (www.antcrc.utas.edu.au/argos). [20]

High-resolution satellite SAR data have been used to monitor the seasonal variability of land-fast sea ice to the west of the Mertz Glacier.  This study will be extended to cover most of the East Antarctic coast. Landfast sea ice thickness is routinely monitoredat Australian coastal Antarctic stations. [21]

Visible and near-infrared satellite images (ERS-ATSR) have been used to determine the spatial distribution of surface snow grain size and its temporal variability for the majority of the ice sheet in East Antarctic. The results show a large variation in grain size from low values around 60 micron to high values around 200 micron and bigger. In general, larger grain size is associated with warmer temperatures and lower elevations such as found over the major ice shelves, while smallest grain size occurs along the high ridges in the interior of East Antarctica. [22]

A time series of the area of Antarctic snow cover affected by melt has been derived from analysis of wind scatterometer (active microwave) data from the ERS satellites. The record now spans the period from 1991 to 2001.  The periods of maximum melt extent and duration occurred in the two summer seasons of 1991-92 and 1997-98. [22]

Heard Island

A detailed survey was made of the elevation, ice thickness, ice velocity, and surface mass balance of the Brown Glacier on the eastern end of Heard Island.  Since 1947 the Brown Glacier has retreated by 1.1 km, decreased in area by 3.7 km² (33%) and decreased in volume by 38%.  The survey data will enable a numerical model of the glacier to be developed and used to determine the climate change necessary to cause the glacier recession.  An automatic weather station was deployed to measure the present glacier climate. [23]

Major Research Output(s) completed in 2000-01 relating to previous seasons' activities

Ongoing analysis and synthesis of results from the July-September 1999 Mertz Glacier Polynya (MGP) experiment have provided estimates of the ice production rates in the polynya during winter, quantified the role of the MGP in production of Adelie Land Bottom Water (in conjunction with the Oceanography Program), and shown that the MGP is primarily a latent heat polynya.  A number of papers on the MGP have been accepted for publication.  [7]

Recent ice thickness and ice movement measurements made between Davis and Mirny have completed a field study of the mass outflow between that sector of the ice sheet 40°E and 130°E, about half of the total East Antarctic ice sheet.  These field estimates are being compared with the modelled mass flux required to maintain balance for different estimated accumulation distributions over the ice sheet. A comparison of the balance fluxes for the Lambert Glacier basin with the in-situ data shows that across the 2500-m contour any mass imbalance is less than the variability between the different accumulation distributions (-24% to +20%).  For some of the accumulation distributions the imbalance estimates vary significantly between different portions of the line.  Residual balance estimates further downstream (1500-m elevation) also show large variability between input accumulation distributions, but most distributions suggest a positive mass budget for this lower elevation sector.  These results, indicating thickening of the ice sheet in this drainage basin, are supported by ice sheet modelling studies. [11]

Upward looking sonar data from an instrument deployed at 63°18S, 107°49E in 1994 show the seasonal evolution of the sea ice draft distribution from May when predominantly thin ice is present, through October when substantially thicker ice caused by deformation has been formed. The mean ice thickness peaks in August at 1.21 m, consistent with the results of ship-based observations in the same region.  [20]

Research/Activities in the 2000-01 strategic plan NOT achieved and why

Milestones 13, 14 and 15 all involve some component of palaeo-ice sheet modelling over Ice Age cycle time-scales.  Although palaeo modelling is an important validation tool, this is seen as of lower priority than development of current and predictive models of the ice sheet system.  Suitably qualified students are not available through the Antarctic CRC to complete all modelling projects, and it is envisaged that the palaeo modelling will not be completed within the scheduled time.

Goal 4 - To Undertake Work of Practical, Economic and National Significance.

[Numbers in square brackets refer to Assessment Milestones]

Glaciology:  Snow and ice on the continent and the ocean are major constraints on Antarctic transport and operations.  A sound knowledge of ice and snow material properties are essential for operations involving, for example, compression of snow for aircraft runway or road construction, ice navigation and ice breaking, melt-water supplies, and inland station construction.

Key Scientific Outputs

A data base of the basic properties, conditions and extent of snow and ice in the Antarctic and Southern Ocean from which information and expert advice can be provided for expedition operations, scientific research, and other activities related to the region

Assessment Milestones

24. Maintenance of records of sea ice conditions, iceberg distributions, and other relevant parameters for use in voyage planning, etc. (Ongoing).
25. Information and advice (on a needs basis) on snow and ice conditions relevant to engineering, operations, building activities, etc. (Ongoing).
26. Data sets for production of maps, geographic information, reports, submissions and other documents, public information material, etc. (Ongoing).

Research Output achieved against the strategic plan

Glaciological studies were undertaken at the sites of proposed compressed snow runways near Lanyon Junction, approximately 12 km inland of Casey, and at a site about 33 km from Casey on the ice inland of the Peterson Glacier. The Lanyon site is suitable for construction of a compressed snow runway whereas the Peterson Glacier site is not.  However at Peterson Glacier the surface appeared to consist of blue (glacier) ice which may be suitable for a minimally prepared runway. [25]

Glaciological and geophysical data collected by both Australian and Russian Antarctic expeditions over the last 20 or so years from the Lambert Glacier/Amery Ice Shelf region have been compiled and merged.  These will be used to produce a number of glaciological thematic maps of the region. [26]

Major Research Output(s) completed in 2000-01 relating to previous seasons' activities

Not relevant

Research/Activities in the 2000-01 strategic plan NOT achieved and why

None

  

Research Output for Glaciology Program published in 2000

[Numbers in square brackets refer to Project Numbers]

Papers in refereed journals: (25)                                  

Bindoff, N. L., S. R. Rintoul, and R. Massom, 2000.  Polynyas and Bottom Water formation south of Tasmania, Papers and Proc. Roy. Soc. Tasmania, 133(3), 51-56.  [189]                 

Curran, M.A.J. and Jones, G.B. 2000. Dimethyl Sulfide in the Southern Ocean:  Seasonality and flux.  J. Geophy. Res.  Vol 105 No D16, p20451-20459. 2000. [757]

Delmotte, M., V. Masson, J.  Jouzel, and V. Morgan (2000). A seasonal deuterium excess signal at Law Dome, coastal Eastern Antarctica: a Southern Ocean Signature. J. Geophys. Res., 105(D6):7187-7197.  [757]          

Featherstone, W.E., Stewart, M.P., Rizos, C., Han, S., Coleman, R., Tregoning, P. and Morgan, P.J. 2000.  GPS-geodetic research at some Australian universities Australian Surveyor, 45(1): 20-30. [1120]

Francey, R. J., Trudinger, C. M., and Levchenko, V. A. (2000). 14C variations in the atmosphere: a southern perspective. In: 50 years of cosmic ray research in Tasmania. M. L. Duldig (editor). (ANARE Research Notes; 102) Kingston, Tas.: Australian Antarctic Division. p. 193-209.

Fricker, Helen A.,  Roland C. Warner and Ian Allison (2000) Mass budget of the Lambert Glacier-Amery Ice Shelf system, East Antarctica: a comparison of computed balance fluxes and measured fluxes.  J. Glaciol., 46(155), 561-570. [3, 1261]        

Fricker, H.A., Hyland, G., Coleman, R., Young, N.W. (2000). Digital elevation models for the Lambert Glacier - Amery Ice Shelf System, East Antarctica, from ERS-1 satellite radar altimetry.  J. Glaciol., 46(155), 553-560. [2224]                      

Gillett, R. W., T. D. van Ommen, A. V. Jackson, and G. P. Ayers (2000) Formaldehyde and peroxide concentrations in Law Dome firn and ice cores. J. Glaciol. 152, 15-19. [757]            

Goodwin, I. D. and Zweck, C.  (2000).  Glacio-isostasy and glacial ice load at Law Dome, Wilkes Land, East Antarctica. Quaternary Research. 53, 285-293.

Jacka, T. H. and J. Li (2000). Ice Flow in Compression at Low Temperature and Stresses. In: Hondo (ed), International Symposium on Physics of Ice-Core Records, p 83-102. International Symposium on Physics of Ice-Core Records. Shikotsukohn, Japan, The International Commission on Snow and Ice. [8]

Keiffer, H., Kargel, J.S., Barry, R., Bindschadler, R., Bishop, M., MacKinnon, D., Ohmura, A., Raup, B., Antoninetti, M., Bamber, J., Braun, M., Brown, I., Cohen, D., Copland, L., DueHagen, J., Engeset, R.V., Fitzharris, B., Fujita, K., Haeberli, W., Hagen, J.O., Hall, D., Hoelzle, M., Johansson, M., Kaab, A., Koenig, M., Konovalov, V., Maisch, M., Paul, F., Rau, F., Reeh, N., Rignot, E., Rivera, A., de Ruyter de Wildt, M., Scambos, T., Schaper, J., Scharfen, G., Schroder, G., Solomina, O., Thompson, D., van der Veen, K., Wohlleben, T., and Young, N.  (2000)  New eyes in the sky measure glaciers and ice sheets.  EOS, Transactions, AGU, 81(24) 265-271. [2224]

King, M.A, Nguyen, N.L., Coleman, R. and Morgan, P.J. 2000. GPS measurements on the Amery Ice Shelf, East Antarctica. GPS Solutions, 4(1): 2-12. [1120]         

King, M.A., Coleman, R., and Morgan, P.J. 2000. Treatment of Horizontal and Vertical Tidal Signals in GPS Data:  A Case Study on a Floating Ice Shelf. Earth, Planets and Space, 52(11): 1043-1047. [1120]

Li, J., Jacka, T.H. and Budd, W.F. (2000) Strong single-maximum crystal fabrics developed in ice undergoing shear with unconstrained normal deformation.  Annals of Glaciology 30 . 88-92.  [8]               

Lytle, V.I., R. A. Massom,  N. Bindoff, A.P. Worby,  and  I. Allison (2000)  The wintertime heat flux to the underside of east Antarctic pack ice.  J. Geophys. Res. 105(C12), 28,759-28769. [189]

Manson, R., Coleman, R., Morgan, P.J., and M.A. King. 2000. Ice velocities of the Lambert Glacier from static GPS observations. Earth, Planets and Space, 52(11): 1031-1036. [1120]

Masson, Valerie, Francoise Vimeux, Jean Jouzel, Vin Morgan, Marc Delmotte, Philippe Ciais, Claus Hammer, Sigfus Johnsen, Ya Lipenkov, Vladimir, E. Mosley-Thompson, Jean-Robert Petit, Eric J. Steig, Michel Stievenard, and Rein Vaikmae (2000). Holocene climatic variability in Antarctica: what can be inferred from 11 ice core isotopic records? Quaternary Research, 54:348-358. [757]       

Marmo, B.A. and Wilson, C.J.L., 2000, The stress distribution related to the boudinage of a visco-elastic material: examples from a polar outlet glacier. In A.J. Maltman, Hambrey, M.J. & Hubbard, B. (Editors) Deformation of Glacial Materials. Geological Society, London, Special Publications, 176, 115-134. [1170]

Smith, A.N., D. Fink, D. Child, V. A. Levchenko, V. I. Morgan, M. Curran, D. M. Etheridge, and G. Elliott.  (2000) 7Be and 10Be concentrations in recent firn and ice at Law Dome, Antarctica. Nucl. Instr. and Meth. B, 172:847-855. [757]

Smith, A. M., Levchenko, V. A., Etheridge, D. M., Lowe, D. C., Hua, Q., Trudinger, C. M., Zoppi, U., and Elcheikh, A. (2000). In search of in-situ radiocarbon in Law Dome ice and firn. Nuclear Instruments and Methods in Physics. Research Section B, 172 (1-4): 610-622.

Warner, R.C. and W. F. Budd.  2000. Derivation of ice thickness and bedrock topography in data-gap regions over Antarctica.  Annals of Glaciology 30, 191–197. [1261]

Watkins, A. B., and I. Simmonds, 2000: Current trends in Antarctic sea ice: The 1990s impact on a short climatology. Journal of Climate, 13, 4441-4451. [1080]

Wilson, C.J.L., 2000, Experimental work on the effect of pre-existing anistropy on fabric development in glaciers. In A.J. Maltman, Hambrey, M.J. & Hubbard, B. (Editors) Deformation of Glacial Materials. Geological Society, London, Special Publications, 176, 97-113. [1170]

Wilson, C.J.L. and Marmo, B.  2000, Flow in Polycrystalline Ice. In: Stress, Strain and Structure, A volume in honour of W D Means. Eds: M.W. Jessell and J.L.Urai. Volume 2, Journal of the Virtual Explorer. ISSN 1441-8126 (Print) ISSN 1441-8134 (CD-ROM) ISSN 1441-8126  (On-line at http://virtualexplorer.com.au/VEjournal/Volume2/ ). [1170]

Worby, A. P. and S. F. Ackley.  2000.  Antarctic research yields circumpolar sea ice thickness data.  Eos, 81(17), 181,184-185. [189]

Other publications: (9)                                                  

Etheridge, D. M. (2000). The changing composition of the global atmosphere [Electronic publication]. In: Australia's science future, Canberra, ACT. Canberra, ACT: Australian Academy of Science: a symposium organised by the Academy.

Noone, D., and I. Simmonds, 2000: A GCM module for tracing stable water isotopes. Research Activities in Atmospheric and Oceanic Modelling, Report No. 30, WMO/TD-No. 987. H. Ritchie, Ed., World Meteorological Organization, 4.28-4.29. [987]

Noone, D., and I. Simmonds, 2000: Synoptic disturbances, climate variability and interpretation of ice core data.  Proceedings of the Sixth International Conference on Southern Hemisphere Meteorology and Oceanography, Santiago, Chile, 3-7 April 2000. American Meteorological Society, 232-233. [987]

Rosman, K., K.Van de Velde, P. Vallelonga, J-P. Candelone, F. Planchon, C. Boutron V.I. Morgan (2000).  TIMS for the Reliable Determination of Lead Concentrations and the Isotopic Ratios in Antarctic Snow and Ice. [Contribution Number: 1100] Procedings of Internat. Conf.  Heavy Metals Environ.,  Ann Arbor, Michigan, U.S.A., August 6-10, http://www.sph.umich.edu/eih/heavymetals [1092]  

Shevlin, J. (2000) Antarctic Air Transport 1999/2000 Investigations Australian Antarctic Division Internal Report; [1222]

Trudinger, C. M. (2000). The carbon cycle over the last 1000 years inferred from inversion of ice core data: submitted for the degree of Doctor of Philosophy, Monash University. Clayton, 76 p.

Wilson, C.J.L. and Marmo, B.  2000. Flow in Polycrystalline Ice - On-line at http://web.earthsci.unimelb.edu.au/wilson/ice1 [1170]

Worby, A.P. (2000) Observing Antarctic Sea Ice: A practical guide for conducting sea ice observations from vessels operating in the Antarctic pack ice. CD-ROM produced for the Antarctic Sea Ice Processes and Climate Program (ASPeCt).; [Ref:189]

Worby, A. P. and S. F. Ackley.  2000.  Sea ice thickness methodically measured in the Antarctic.  Earth in Space, 12(7), pp. 15. [189]

Conference abstracts:  (26)

Allison, I. 2000. Seasonal and short-term variability of East Antarctic snow accumulation SCAR Working Groups on Glaciology and Physics and Chemistry of the Atmosphere, Symposium on Antarctic Precipitation and Mass Balance, Tokyo, 13 July 2000 (abstract). [187]

Budd W.F. and Wu X. Antarctic and Southern Ocean influences on Australian climate and expected long term changes from increasing greenhouse gases. In 13th Australia New Zealand Climate Forum, Hobart 10-12 April 2000, 12, 2000. [2333]

Etheridge, D. M., Steele, L. P., Smith, A. M., Trudinger, C. M., Langenfelds, R. L., Lowe, D. C., Levchenko, V. A., Sturrock, G. A., Francey, R. J., Fraser, P. J., Morgan, V. I., Levin, I., and Barnola, J.-M. (2000). Records of atmospheric trace gases and some isotopic ratios from Law Dome firn air. In: Geophysical research abstracts: 25th General Assembly, Nice, France. Katlenburg-Lindau, Germany : European Geophysical Society. p. OA41.

Fricker, Helen Amanda, Ian Allison, Neal Young. 2000  Mass balance components of the Amery Ice Shelf AGU Fall Meeeting, San Francisco, December 2000. [1164]  

Heil, P., C.W. Fowler, J. Maslanik, W.J. Emery and I. Allison.  2000. A comparison of East Antarctic sea-ice motion derived using drifting buoys and remote sensing. International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000 [Abstract 131] [742]

Heil, P., Ian Allison and V.I. Lytle.  2000. The impact of deformation on the local sea-ice growth rate in the East Antarctic sector. International Union of Theoretical and Applied Mathematics, Sympopsium on Scaling Laws in Ice Mechanics and Ice Dynamics, Fairbanks, June 2000. [189, 742]

Heil, P.  2000  The Fast ice and overlying Snow Cover near Davis Station, Antarctica: I. Observations AGU 2000 Fall Meeeting, San Francisco, December 2000. [189] 

Jacka, T.H.  2000. Review of techniques for Antarctic Ice Sheet mass balance studies. SCAR Working Groups on Glaciology and Physics and Chemistry of the Atmosphere, Symposium on Antarctic Precipitation and Mass Balance, Tokyo, 13 July 2000 (abstract).

Lytle, V., A. Worby, R. Massom, M. Paget, I. Allison, X. Wu and A. Roberts.  Ice formation and drift in the Mertz Glacier polynya during winter. International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000. [Abstract 31]  [189, 742]

Lytle, V., I. And S.F. Ackley.  2000.  Snow ice growth: a freshwater flux from new ice growth in the Weddell Sea, Antarctica. International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000  [Abstract 1] [189]

Lytle, V. I., K. Golden and P. Heil, Measurements of brine flow rates through Antarctic sea ice,  EOS trans., AGU Vol 81, No. 22, May 30, 2000, Proc. of 2000 Western Pacific Geophysics Meeting, p 65, 2000. [1060]

Lytle, V. I., I. Allison, R. Massom, A. P. Worby, Ice formation rates within the Mertz Glacier Polynya, EOS trans., AGU Vol 81, No. 22, May 30, 2000, Proc. of 2000 Western Pacific Geophysics Meeting, p 69, 2000. [189]

Massom, R.A., V.I. Lytle, K. Hill, A.P. Worby and I. Allison.  Effects of regional fast- and pack- ice distribution on the behaviour of the Mertz Glacier polynya, East Antartica. International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000. [Abstract 32]   [189]

Noone, D., and I. Simmonds, 2000: Climate variability of modeled polar °18O from sensitivity to boundary conditions.  Proceedings Volume, Seventh National Australian Meteorological and Oceanographic Society Conference (Australian Meteorological and Oceanographic Society Publication Number 16), Melbourne, Australia, 7-9 February, 2000, 89. [987]

Noone, D., and I. Simmonds, 2000: Reassessing the stable water isotope record in understanding past climate. Geological Society of Australia, Abstracts No. 62. M. Purss, Ed., Geological Society of Australia, 4. [987]

Paget, M.J., A.P. Worby and K.J. Michael. Determining the floe size distribution of East Antarctic pack ice from digital aerial photographs. International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000. [Abstract 45]  [189]

Roberts, A., I. Allison and V.I. Lytle.  2000.  Latent and sensible heat flux estimates over the Mertz Glacier polynya from in-flight measurements. International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000. [Abstract 135]   [189]

Roberts, D., T. D. van Ommen, A. McMinn, V. Morgan, and J. L. Roberts. (2000) A tale of two proxies: Lake and ice cores unite for antarctic paleoclimate analyses. In 8th International Symposium on Paleolimnology. Queen's University, Kingston, Ontario, Canada (Conference poster). [757]

Sheedy,J., G. Wendler, A. Worby.  2000. The surface energy budget in the Antarctic summer sea-ice pack. International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000. [Abstract 194]  [189]

Trudinger, C. M., Etheridge, D. M., Levchenko, V. A., Francey, R. J., Enting, I. G., Allison, C. E., Battle, M. O., and BenderM. (2000). The use of a firn diffusion model in the reconstruction of atmospheric records. In: Geophysical research abstracts: 25th General Assembly, Nice, France. Katlenburg-Lindau, Germany : European Geophysical Society. p. OA41.

Trudinger, C. M., Etheridge, D. M., Sturrock, G. A., Rayner, P. J., Fraser, P. J., Enting, I. G., Steele, L. P., Lowe, D. C., and Smith, A. (2000). Reconstructing atmospheric records from firn and ice core measurements. In: Cape Grim Baseline Air Pollution Station Annual Scientific Meeting: abstracts, Aspendale, Victoria, N. W. Tindale, and N. Derek (editors). [Aspendale, Victoria]: [CSIRO Atmospheric Research, Bureau of Meteorology] . p. 37.

Williams, G. and N. Bindoff  (2000)  Sea ice growth and water mass modification in the Mertz Glacier polynya. International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000.  [Abstract 122]  [189]

Worby, A.,  G. Bush and I. Allison. (2000) Seasonal development of the ice thickness distribution in East Antarctica from upward looking sonar data. International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000. [Abstract 30]  [189]

Wu X., Budd W.F. and Hirst A.C. Climate change in a coupled global climate model. In Proceedings of 7th AMOS Conference, Melbourne University, Melbourne, 7-9 February 2000, 130, 2000. (Abstract.) [2333]

Wu, Xingren., W.F. Budd, A.P. Worby and Ian Allison   2000 Sensitivity of the Antarctic sea ice distribution to oceanic heat flux in a coupled atmosphere-sea ice model.  International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000. [Abstract 118] [2333]

Wu, Xingren., W.F. Budd and Ian Allison   2000. A GCM study of the impacts of persistent Antarctic polynyas. International Symposium on Sea Ice and its Interactions with the Ocean, Atmosphere and Biosphere, Fairbanks, Alaska, U.S.A., 19-23 June 2000. [Abstract 119]  [2333]