|
|
Littot G.C., Mulvaney R., Öthlisberger R., Udisti R., Wolff E.W., Castellano E., De An. (2002). Comparison of analytical methods used for measuring major ions in the EPICA Dome C (Antarctica) ice core. Annals of glaciology, 35, 299–305.
|
|
|
|
Monnin, E.; Indermuhle, A.; Dallenbach, A.; Fluckiger, J.; Stauffer, B.; Stocker, T.F.; Raynaud, D.; Barnola, J.-M. (2001). Atmospheric CO2 Concentrations over the Last Glacial Termination. Science, 291(5501), 112–114.
Abstract: A record of atmospheric carbon dioxide (CO2) concentration during the transition from the Last Glacial Maximum to the Holocene, obtained from the Dome Concordia, Antarctica, ice core, reveals that an increase of 76 parts per million by volume occurred over a period of 6000 years in four clearly distinguishable intervals. The close correlation between CO2 concentration and Antarctic temperature indicates that the Southern Ocean played an important role in causing the CO2 increase. However, the similarity of changes in CO2 concentration and variations of atmospheric methane concentration suggests that processes in the tropics and in the Northern Hemisphere, where the main sources for methane are located, also had substantial effects on atmospheric CO2 concentrations
Programme: 960
|
|
|
|
Reijmer, C.H.; Oerlemans, J. (2002). Temporal and spatial variability of the surface energy balance in Dronning Maud Land, East Antarctica. J. Geophys. Res., 107.
Abstract: We present data of nine Automatic Weather Stations (AWS), which are located in Dronning Maud Land (DML), East Antarctica, since the austral summer of 1997. Potential temperature and wind speed are maximum at the sites with the steepest surface slope, i.e., at the edge of the Antarctic plateau. Specific humidity and accumulation decrease with elevation and distance from the coast. The annual average energy gain at the surface from the downward sensible heat flux varies between ?3 W m?2 and ?25 W m?2, with the highest values at the sites with the largest surface inclination and wind speeds. The net radiative flux is negative and largely balances this sensible heat flux and ranges from ??2 W m?2 to ??28 W m?2; maximum values can be linked to maxima in surface slope and wind speed, and suggest a strong connection between the heat budget and the katabatic flow in DML. The average latent heat flux is generally small and negative (??1 W m?2) indicating a slight net mass loss through sublimation.
Keywords: 1827 Hydrology: Glaciology; 1863 Hydrology: Snow and ice; 3307 Meteorology and Atmospheric Dynamics: Boundary layer processes; 3349 Meteorology and Atmospheric Dynamics: Polar meteorology; 9310 Information Related to Geographic Region: Antarctica
Programme: 960
|
|
|
|
Frezzotti M., Pourchet M., Flora O., Gandolfi S., Gay M., Urbini S., Vincent C., Becagli S., Gragnani R., Proposito M., Severi M.,Traversi R., Udisti R., Fily M. (2004). New estimations of precipitation and surface sublimation in East Antarctica from snow accumulation measurements,. Climate dynamics, 23, 803–813.
Abstract: Talos Dome is an ice dome on the edge of the East Antarctic plateau; because accumulation is higher here than in other domes of East Antarctica, the ice preserves a good geochemical and palaeoclimatic record. A new map of the Talos Dome area locates the dome summit using the global positioning system (GPS) (72?47’ 14’’S, 159?04’ 2’’E; 2318.5m elevation (WGS84)). A surface strain network of nine stakes was measured using GPS. Data indicate that the stake closest to the summit moves south-southeast at a few cma–1. The other stakes, located 8 km away, move up to 0.33ma–1. Airborne radar measurements indicate that the bedrock at the Talos Dome summit is about 400m in elevation, and that it is covered by about 1900m of ice. Snow radar and GPS surveys show that internal layering is continuous and horizontal in the summit area (15 km radius). The depth distribution analysis of snow radar layers reveals that accumulation decreases downwind of the dome (north-northeast) and increases upwind (south-southwest). The palaeomorphology of the dome has changed during the past 500 years, probably due to variation in spatial distribution of snow accumulation, driven by wind sublimation. In order to calculate a preliminary age vs depth profile for Talos Dome, a simple one-dimensional steady-state model was formulated. This model predicts that the ice 100m above the bedrock may cover one glacial–interglacial period.
Programme: 960
|
|
|
|
Magand O., Frezzotti M., Pourchet M., Stenni B., Genoni L. & Fily M. (2005). Climate variability along latitudinal and longitudinal transects in East antarctica. Annals of glaciology, 39, 351–358.
|
|
|
|
The Ismass Committee. (2004). Recommendations for the collection and synthesis of Antarctic ice sheet mass balance data. Global and planetary change, 42.
|
|
|
|
Siegenthaler U., Monnin E., Kawamura K., Spahni R., Schwander J., Stauffer B., Stocker T., Barnola J.M. & Fischer H. (2005). Supporting evidence from the EPICA dronning maud Land ice core for atmospheric CO² changes during the past millenium. Tellus series a-dynamic meteorology and oceanography, B-57, 51–57.
|
|
|
|
Raynaud D., Barnola J.M., Souchez R., Lorrain R., Petit J.R., Duval P. & Lipenkov V. (2005). The record for marine isotopic stage 11. Nature, 436, 39–40.
|
|
|
|
Monnin E., Steig E.J., Siegenthaler U., Kawamura K., Schwander J., Stauffer B., Stocker T.F., Morse D.L., Barnola J.M. & Bellier B. (2004). Evidence for substantial accumulation rate variability in Antarctica during the Holocene, through synchronization of CO2 in the Taylor Dome, Dome C and DML ice cores. Earth Planet. Sci. Lett., 224(1-2), 45–54.
|
|
|
|
Raynaud D., Blunier T., Ono Y., Delmas R., Barnola J.M., Joos F., Petit J.R. & Spahni R. (2003). The late quaternary history of atmospheric trace gases and aerosols: interactions between climate and biochemical cycles..
Abstract: Paleoclimate Global Change and the Future The IGBP series. K. D. Alverson Bradley R. S. Petersen T. F. (eds) Berlin Springer
Programme: 960
|
|
