Three important calorimetric applications of a classic thermodynamic equation

2003 ◽  
Vol 32 (5) ◽  
pp. 264 ◽  
Author(s):  
Michael J. Blandamer ◽  
Paul M. Cullis ◽  
Peter T. Gleeson
Keyword(s):  
Thermodynamic Equation

scholarly journals Preface "An historical perspective on the development of the Thermodynamic Equation of Seawater – 2010"

Ocean Science ◽  
2012 ◽  
Vol 8 (2) ◽  
pp. 161-174 ◽  
Author(s):  
R. Pawlowicz ◽  
T. McDougall ◽  
R. Feistel ◽  
R. Tailleux
Keyword(s):  
Historical Perspective ◽  
Thermodynamic Equation

scholarly journals Modeling the Antarctic ice sheet

1997 ◽  
Vol 25 ◽  
pp. 259-268 ◽  
Author(s):  
Mikhail Verbitsky ◽  
Barry Saltzman
Keyword(s):  
Three Dimensional ◽  
Ice Sheet ◽  
Glacial Cycle ◽  
Antarctic Ice Sheet ◽  
Thermodynamic Equation ◽  
Last Glacial ◽  
Ice Stream ◽  
Basal Melting ◽  
The Antarctic ◽  
The Last Glacial

A three-dimensional (3-D), high-resolution, non-linearly viscous, non-isothermal ice-sheet model is employed to calculate the “present-day” equilibrium regime of the Antarctic ice sheet and its evolution during the last glacial cycle. The model is augmented by an approximate formula for ice-sheet basal temperature, based on a scaling of the thermodynamic equation for the ice flow. Steady-state solutions for both the shape and extent of the areas of basal melting (or freezing) are shown to be in good agreement with those obtained from the solution of the full 3-D thermodynamic equation. The solution for the basal temperature field of the West Antaretie Siple Coast produces areas at the pressure-melting point separated by strips of frozen-to-bed ice, the structure of which is reminiscent of Ice Streams A–E. This configuration appears to be robust, preserving its features in spite of climatic changes during the last glacial cycle. Ice Stream C seems to be more vulnerable to stagnation, switching to a passive mode at least once during the penultimate interglacial. We conjecture that the peculiarities of local topography determine the unique behavior of Ice Stream C: reduced basal stress and, consequently, relatively weak warming due to internal friction and basal sliding is not able to counteract the advective cooling during the periods of increased snowfall rate.

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