Search Results

You are looking at 1 - 4 of 4 items for :

  • Middle atmosphere x
  • Third THORPEX International Science Symposium x
  • All content x
Clear All
Elizabeth Satterfield and Istvan Szunyogh

15 February 2004. Fig . 2. The time evolution of TV (squares), TVS (triangles), and V (circles) for the NH extratropics. Results are shown for experiments that assimilate (top) randomly distributed simulated observations, (middle) simulated observations at the locations of conventional observations, and (bottom) observations of the real atmosphere. Note the scale is exponential. Also note the different scale in (bottom) panel. Interestingly, the difference between TVS and V at longer lead

Full access
John E. Janowiak, Peter Bauer, Wanqiu Wang, Phillip A. Arkin, and Jon Gottschalck

semblance of MJO-related variations in precipitation forecasts out to 15 days. Today, with the advantage of model improvements, advances in data assimilation systems, and ocean–atmosphere coupling in some models, the following question comes to mind: How do present-day model forecasts perform? After all, much better information about oceanic precipitation is available in the present-day compared to what was available when the studies referred to earlier were conducted. More accurate estimates of

Full access
Munehiko Yamaguchi and Sharanya J. Majumdar

stability of the atmosphere. In addition to this, the eddy available potential energy needs to be converted into the eddy kinetic energy ( K ′) in order for the perturbation to obtain kinetic energy through the baroclinic process. This conversion is given by We focus on the first term in Eq. (3) , the radial eddy heat flux, to demonstrate how ECMWF perturbations cause the growth of the steering and asymmetric propagation vector through the baroclinic energy conversion in a vortex

Full access
Sharanya J. Majumdar, Kathryn J. Sellwood, Daniel Hodyss, Zoltan Toth, and Yucheng Song

from 7 to 0 days (where t υ is fixed). Several decades after observations of downstream development of baroclinic waves in the middle and upper troposphere were documented (beginning with Namias and Clapp 1944 ), numerical investigations determined that downstream baroclinic development was achieved by examining the response of a baroclinically unstable atmosphere to a local initial perturbation ( Simmons and Hoskins 1979 ). A series of papers in the 1990s investigated this phenomenon in greater

Full access