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Brian E. J. Rose and David Ferreira

is driven by a dynamical moistening and redistribution of water vapor. OHT weakens the Hadley circulation, allowing moist convection to spread out of the deep tropics into its flanks, which moistens the subtropical troposphere and allows for increased greenhouse trapping. In the low latitudes, the oceanic redistribution of heat is felt through a deep tropospheric layer by means of moist convection, with important consequences for the radiative budget. In the more stably stratified midlatitudes

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M. M. Poc and M. Roulleau

1628 JOURNAL OF CLIMATE AND APPLIED METEOROLOGY VOLUME22Water Vapor Fields Deduced from METEOSAT-1 Water Vapor Channel Data M. M. Poc AND M. ROULLEAUl Laboratoire de Meteorologie Dynamique du C.N. KS., Ecole Polytechnique, ~?1128 Palaiseau Cedex, France (Manuscript received 4 May 1982, in final form 3 April 1983) ABSTRAC~I' A quasi-operational process for the

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De-Zheng Sun and Richard S. Lindzen

15JUNE 1993 SUN AND LINDZEN 1643Distribution of Tropical Tropospheric Water Vapor DE-ZHENG SUN AND RICHARD S. LINDZENCenter for Meteorology and Physical Oceanography, Massachusetts Institute of Technology, Cambridge, Massachusetts(Manuscript received 30 December 1991, in final form 11 August 1992)ABSTRACT Utilizing a conceptual model for tropical convection and observational data for water vapor, the

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Bryce E. Harrop and Dennis L. Hartmann

1. Introduction Climate feedbacks involving water vapor and clouds are very important for the magnitude and structure of climate change, and the strongest energy exchanges are in the tropics. Hartmann and Larson (2002) proposed a constraint on the temperature of tropical anvil clouds derived from the Clausius–Clapeyron relation and the emission lines of water vapor. This so called “fixed anvil temperature” (FAT) hypothesis suggests that the temperature where anvil clouds detrain is tied to

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Da Yang and Seth D. Seidel

questions. The importance of water vapor seems to be widely recognized in the literature of climate feedbacks ( Manabe and Wetherald 1967 ; Ingersoll 1969 ; Held and Soden 2000 ; Flato et al. 2013 ). Previous studies have focused on three basic effects of water vapor: E1) water vapor is a greenhouse gas; E2) water vapor can condense to liquid water and release latent heat; and E3) saturation vapor pressure increases with temperature exponentially. The combination of E1 and E3 gives rise to the water

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P. M. Kuhn and S. K. Cox

142 JOURNAL OF APPLIED METEOROLOGY VOLIJME 6Radiometric Inference of Stratospheric Water Vapor P. M. Kurus' AND S. K. Cox~ Weather Bureau, ESSA, Madison, Wi~-. (Manuscript received 26 May 19~, ~ tevhed form 29 September 19~) ~STRACT By v~r~ug the amount of water vapor ~ iuput to the m~ative po~ver transfer equation, ~suming sconstant car

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Angela Kao, Xun Jiang, Liming Li, James H. Trammell, Guang J. Zhang, Hui Su, Jonathan H. Jiang, and Yuk L. Yung

1. Introduction Observational studies suggest that the total mass of water vapor increases as a response to the increase in temperature ( Trenberth et al. 2005 ; Wentz et al. 2007 ; Santer et al. 2007 ). Similar trends are also seen in the total mass of water vapor from models ( Bosilovich et al. 2005 ; Held and Soden 2006 ). Unlike the simple relationship between water vapor and temperature, the variations of precipitation are more complex ( Trenberth and Shea 2005 ; Adler et al. 2008

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Agnieszka A. Mrowiec, Stephen T. Garner, and Olivier M. Pauluis

1. Introduction Intertwining dynamics and thermodynamics across scales ranging from 10 m to 1000 km, hurricanes are arguably the most complex type of coherent structure found in the earth’s atmosphere. Not surprisingly, a unified theory for their intensity, scale, and variability is still elusive. Here we propose an approach based on the suppression of one of the most complex components of hurricane dynamics: water vapor. Specifically, we show that the theoretical framework of Emanuel (1986

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N. Fukuta and C. M. Gramada

1. Introduction Vapor pressure of supercooled water is one of the most fundamental properties required when the liquid phase of water substance is studied under subfreezing temperatures, such as microphysical processes of clouds at high altitudes or low temperatures. The best data currently available for the saturation vapor pressure are those listed in the Smithsonian Meteorological Table or the International Meteorological Table, mostly due to Goff (1942 , 1949 ) and Goff and Gratch (1945

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G. W. K. Moore and Gerald Holdsworth

1. Introduction Mount Logan, Canada’s highest mountain, is located in the heavily glaciated Saint Elias Mountains of the Yukon Territory just to the east of the Gulf of Alaska ( Figs. 1 and 2 ). The mountain is situated in a region of significant climatological importance. For example, it is located at the end of the major North Pacific storm track ( Blackmon 1976 ; Hoskins and Hodges 2002 ) along the main atmospheric pathway by which water vapor enters the Gulf of Alaska ( Newell and Zhu

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