<?xml version="1.0" encoding="UTF-8"?><xml><records><record><source-app name="Biblio" version="6.x">Drupal-Biblio</source-app><ref-type>17</ref-type><contributors><authors><author><style face="normal" font="default" size="100%">Magnusdottir, G.</style></author><author><style face="normal" font="default" size="100%">Saravanan, R.</style></author></authors></contributors><titles><title><style face="normal" font="default" size="100%">The response of atmospheric heat transport to zonally-averaged SST trends</style></title><secondary-title><style face="normal" font="default" size="100%">Tellus Series a-Dynamic Meteorology and Oceanography</style></secondary-title><alt-title><style face="normal" font="default" size="100%">Tellus Ser. A-Dyn. Meteorol. Oceanol.</style></alt-title></titles><keywords><keyword><style  face="normal" font="default" size="100%">1000</style></keyword><keyword><style  face="normal" font="default" size="100%">balance</style></keyword><keyword><style  face="normal" font="default" size="100%">budget</style></keyword><keyword><style  face="normal" font="default" size="100%">circulation</style></keyword><keyword><style  face="normal" font="default" size="100%">community-climate-model</style></keyword><keyword><style  face="normal" font="default" size="100%">Content Type: Biblio</style></keyword><keyword><style  face="normal" font="default" size="100%">equilibrium</style></keyword><keyword><style  face="normal" font="default" size="100%">large-scale eddies</style></keyword><keyword><style  face="normal" font="default" size="100%">Magnusdottir Modeling Lab</style></keyword><keyword><style  face="normal" font="default" size="100%">meridional energy transports</style></keyword><keyword><style  face="normal" font="default" size="100%">ocean</style></keyword><keyword><style  face="normal" font="default" size="100%">static stability</style></keyword><keyword><style  face="normal" font="default" size="100%">weather</style></keyword></keywords><dates><year><style  face="normal" font="default" size="100%">1999</style></year><pub-dates><date><style  face="normal" font="default" size="100%">Oct</style></date></pub-dates></dates><urls><web-urls><url><style face="normal" font="default" size="100%">&lt;Go to ISI&gt;://000083609700019</style></url></web-urls></urls><number><style face="normal" font="default" size="100%">5</style></number><volume><style face="normal" font="default" size="100%">51</style></volume><pages><style face="normal" font="default" size="100%">815-832</style></pages><isbn><style face="normal" font="default" size="100%">0280-6495</style></isbn><language><style face="normal" font="default" size="100%">English</style></language><abstract><style face="normal" font="default" size="100%">&lt;p&gt;We compute the atmospheric heat transport in a realistic atmospheric general circulation model under five different configurations of implied heat transport in the ocean. The implied oceanic heat transport is varied by changing the meridional gradient of sea surface temperature (SST). Climatological SSTs are employed for the control run. The other runs differ in that a zonally symmetric component is added to or subtracted from the climatological SST held. The meridional structure of the Variation in SST gradient is based on the observed change in zonally averaged SST over the last century. The SST trend has maxima of about 1 K at high latitudes of both hemispheres. Elsewhere, the change in SST over the last century is fairly uniform at about 0.5 K. We find that in the annual mean, the atmosphere adjusts so that the total meridional heat transport (by atmosphere and ocean) is rather insensitive to the change in zonally averaged SST. Interannual variability in the annual mean heat transport is minor in each of these cases. There is a large degree of compensation even between the different components of atmospheric heat transport such that changes in latent heat transport usually go hand in hand with changes in dry static energy transport of an opposite sign. The radiative flux at the top of the atmosphere is affected the most by the change in SST in the tropics, where the shortwave component shows a strong negative feedback and the longwave component shows a weak positive feedback. Concentrating on the winter season in the Northern Hemisphere, we find that when we decrease the meridional SST gradient (i.e., warm the sea surface at high latitudes the most), the stationary waves accomplish more of the poleward heat transport than before. When we increase the meridional SST gradient, the heat Aux due to both transient and stationary waves increases, although not by nearly as much as most eddy parameterization schemes would predict. The winter season in the Southern Hemisphere shows a substantial increase in hear transport by transient waves when the meridional SST gradient is increased. Their maximum heat transport is greater and extends over a wider band of latitudes than in the control case. Because the Southern Hemisphere is mostly covered by ocean, the stationary waves are weak and play a minor role in atmospheric heat transport.&lt;/p&gt;</style></abstract><work-type><style face="normal" font="default" size="100%">Proceedings Paper</style></work-type><accession-num><style face="normal" font="default" size="100%">ISI:000083609700019</style></accession-num><notes><style face="normal" font="default" size="100%">&lt;p&gt;ISI Document Delivery No.: 254KDTimes Cited: 5Cited Reference Count: 31Cited References:      BROECKER WS, 1985, NATURE, V315, P21     BRYAN F, 1986, NATURE, V323, P21     BUDYKO MI, 1969, TELLUS, V21, P611     CARISSIMO BC, 1985, J PHYS OCEANOGR, V15, P82     GREEN JSA, 1970, QUART J ROY METEOR S, V96, P157     HOUGHTON JT, 1996, CLIMATE CHANGE 1995     KASAHARA A, 1974, M WEATH REV, V102, P509     KEITH DW, 1995, TELLUS A, V47, P30     KERR RA, 1994, SCIENCE, V265, P1528     KIEHL JT, 1996, DESCRIPTION NCAR COM     KIEHL JT, 1998, J CLIMATE, V11, P1131     KIEHL JT, 1998, J CLIMATE, V11, P1151     LARGE WG, 1997, J PHYS OCEANOGR, V27, P2418     LORENZ EN, 1979, J ATMOS SCI, V36, P1367     MANABE S, 1985, J GEOPHYS RES, V90, P11689, DOI 10.1029/JC090IC06P11689     MANABE S, 1988, J CLIMATOL, V1, P841     NORTH GR, 1975, J ATMOS SCI, V32, P2033     PRESS WH, 1989, NUMERICAL RECIPES AR     RAHMSTORF S, 1995, J PHYS OCEANOGR, V25, P787     RAMANATHAN V, 1991, NATURE, V351, P27     RAMANATHAN V, 1995, SCIENCE, V267, P499     RAYNER NA, 1995, 69 HADL CTR MET OFF     SARAVANAN R, 1995, J CLIMATE, V8, P2296     STOMMEL H, 1961, TELLUS, V13, P224     STONE PH, 1978, DYNAM ATMOS OCEANS, V2, P123     STONE PH, 1980, J ATMOS SCI, V37, P1708     STONE PH, 1992, J ATMOS SCI, V49, P355     TRENBERTH KE, 1994, CLIM DYNAM, V10, P107     ZHANG YC, 1997, J CLIMATE, V10, P2358     ZHOU ST, 1993, J CLIMATE, V6, P1871     ZHOU ST, 1993, J CLIMATE, V6, P985Munksgaard int publ ltdCopenhagen&lt;/p&gt;</style></notes><auth-address><style face="normal" font="default" size="100%">&lt;p&gt;Univ Calif Irvine, Dept Earth Syst Sci, Irvine, CA 92697 USA. Natl Ctr Atmospher Res, Boulder, CO 80307 USA.Magnusdottir, G, Univ Calif Irvine, Dept Earth Syst Sci, Irvine, CA 92697 USA.&lt;/p&gt;</style></auth-address></record></records></xml>