SEA ICE RADAR ALTIMETER SIGNATURE MODELLING EXPERIMENTS CONTACT: RASMUS TONBOE (1) SØREN ANDESEN (1) LEIF TOUDAL PEDERSEN (2) (1) Danish Meteorological.

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SEA ICE RADAR ALTIMETER SIGNATURE MODELLING EXPERIMENTS CONTACT: RASMUS TONBOE (1) SØREN ANDESEN (1) LEIF TOUDAL PEDERSEN (2) (1) Danish Meteorological Institute Lyngbyvej 100 Dk-2100 Copenhagen Ø (2) Ørsted●Technical University of Denmark Building Kgs. Lyngby snow/ice profile parameters dielectric properties radiative transfer radar specific parameters pulse form backscatter output BACKSCATTER MODELLING PRINCIPLES AND TERMS Abstract: Scattering at the large horizontal dielectric contrasts of the snow/sea ice system i.e. the snow and ice surface dominate the altimeter total backscatter coefficient. To investigate the temporal and seasonal altimeter backscatter signature variability a forward model is coupled to a thermodynamic and mass model for the snow and sea-ice temperature profile, accumulation, growth, melt and metamorphosis. The thermodynamic and mass model uses an initial snow and ice profile and meteorological data input. In situ data collected during the 2003 CRYOVEX joint Danish-German-ESA campaign and the 2004 GreenIce ice camp are used. Our results show that the snow cover is indeed important for the microwave signature of sea ice as well as its buoyant balance. BACKSCATTER MODELLING RESULTS First-year ice in Fram Strait 2003Multiyear ice in Lincoln Sea 2004 BACKSCATTER SIGNATURE RESPONSE TO METEOROLOGY AND STATE OF THE SNOW/ICE PROFILE USING A COUPLED BACKSCATTER AND THERMODYNAMIC MASS MODEL Snow and ice profiles collected at the 2003 CRYOVEX joint Danish-German-ESA campaign (two first-year ice profiles from Fram Strait) and the 2004 GreenIce ice camp (typical multiyear ice profile from the Lincoln Sea) are used as examples to illustrate the significance of the snow cover for the altimeter backscatter signature. The permittivity of two first-year ice profiles used in the simulation of the backscatter leading edge (right). The range measured by the altimeter is the sum of 'range' and '½ - power' time. The '1/2-power elevation' is not a physical interface in the snow/ice profile, but rather a function of snow depth and other snow properties. REFERENCES Fetterer, F. M., M. R. Drinkwater, K. C. Jezek, S. W. C. Laxon, R. G. Onstott, & L. M. H. Ulander, In: F. D. Carsey, Ed.,. Microwave Remote Sensing of Sea Ice, Geophysical Monograph 68 (pp ). Washington DC: American Geophysical Union, Ridley, J. K. & K. C. Partington, Int. J. Rem.Sens.9(4), , Rothrock, D. A., In: N. Untersteiner (Ed.) The Geophysics of Sea Ice (pp ). NATO ASI series, Series B: Physics Vol Plenum Press, Ulander, L. M. H., & A. Carlström, Proc. IGARSS'91, , The meteorological record from the GreenIce camp in the Lincoln Sea 2004 is used in the coupled thermodynamic mass and backscatter model. The thermodynamic mass model ensures a realistic description of the snow/ ice profile under different meteorological forcing. The initial snow and multiyear ice profile consist of 25cm snow and 350cm ice. Ice and Remote Sensing Division ● Danish Meteorological InstituteØrsted ● Technical University of Denmark Polar bear weight Free-board weight Ice buoyancy In the real world snow cover may not be the only force acting on sea ice buoyancy e.g. ice density, ridges & reology and there are also other properties complicating the analysis of the altimeter radar backscatter e.g. inhomogeneous distribution of scattering elevation, snow depth and density. Our modelling experiments can be seen as an attempt to model multiyear ice melt-pond altimeter backscatter. The snow cover plays a vital role for the melt-pond signature. (photo: National Ice Center). output density thickness Sea ice conditions even within a CRYOSAT resolution cell are often diverse. Large myltiyear ice floes have undulating topography with refrozen melt-ponds and hummocks caused by differential melt in summer, uneven snow cover distribution and pressure ridges. These features all add the backscattered signal and complicates its analysis. However, the melt-pond altimeter backscatter is much higher than backscatter from ridges and hummocks. Therefore, if the model describes backscatter from the melt-ponds adequately it is possible to explain the most important backscatter processes. Our modelling experiments can be seen as an attempt to model multiyear ice melt-pond altimeter backscatter. The snow cover plays a vital role for the melt-pond signature (photo: National Ice Center).