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298 JOURNAL OF APPLIED METEOROLOGY VOLUSE2The Infrared Radiation Temperature Correction for Spherical Temperature Sensors~ CLAUDE E. Dire_J-toN The U~iversity of Texas(Manuscript received 28 September 1962, in revised form 19 December 1962)ABSTRACT The steady-state radiation temperature correction for a spherical temperature sensor, defined as thedifference between the observed
298 JOURNAL OF APPLIED METEOROLOGY VOLUSE2The Infrared Radiation Temperature Correction for Spherical Temperature Sensors~ CLAUDE E. Dire_J-toN The U~iversity of Texas(Manuscript received 28 September 1962, in revised form 19 December 1962)ABSTRACT The steady-state radiation temperature correction for a spherical temperature sensor, defined as thedifference between the observed
) reported that optically thin cirrus clouds with visible optical depths less than 1.4 were found in 20% of the HIRS data from 1979 to 2001. The effect of cirrus clouds on the energy balance of the earth–atmosphere system is a topic of critical importance because on the one hand, they affect solar radiation, referred to as the albedo effect, and on the other hand, they trap a significant amount of thermal infrared radiation emitted from the atmosphere below and the surface, referred to as the greenhouse
) reported that optically thin cirrus clouds with visible optical depths less than 1.4 were found in 20% of the HIRS data from 1979 to 2001. The effect of cirrus clouds on the energy balance of the earth–atmosphere system is a topic of critical importance because on the one hand, they affect solar radiation, referred to as the albedo effect, and on the other hand, they trap a significant amount of thermal infrared radiation emitted from the atmosphere below and the surface, referred to as the greenhouse
Ju~E1965 WILFORD G. ZDUNKOWSKI AND FRANK G. JOHNSON 371Infrared Flux Divergence Calculations with Newly Constructed Radiation TablesWILFO~D G. ZI)UNKOWSX~ ANO FRANK G. Jom~soN, CAPZAIN, USAFUniversity of Utah, Salt Lake City(Manuscript received 25 September 1964, in revised form 10 December 1964)ABSTRACT This paper presents some sample computations of infrared radiative flux divergence due to atmosphericwater vapor
Ju~E1965 WILFORD G. ZDUNKOWSKI AND FRANK G. JOHNSON 371Infrared Flux Divergence Calculations with Newly Constructed Radiation TablesWILFO~D G. ZI)UNKOWSX~ ANO FRANK G. Jom~soN, CAPZAIN, USAFUniversity of Utah, Salt Lake City(Manuscript received 25 September 1964, in revised form 10 December 1964)ABSTRACT This paper presents some sample computations of infrared radiative flux divergence due to atmosphericwater vapor
2158 MONTHLY WEATHER REVIEW VoLu~4- 109The Near-Infrared Radiation Received by Satellites from Clouds G. J. BELL~ AND M. C. WONGRoyal Observatory, Hong Kong(Manuscript received 30 October 1980, in final form 2 April 1981)ABSTRACT On satellite images in the near-infrared 3.7/~m atmospheric window some low clouds appear warmerthan the sea. A simple analysis of the radiation balance of elements of
2158 MONTHLY WEATHER REVIEW VoLu~4- 109The Near-Infrared Radiation Received by Satellites from Clouds G. J. BELL~ AND M. C. WONGRoyal Observatory, Hong Kong(Manuscript received 30 October 1980, in final form 2 April 1981)ABSTRACT On satellite images in the near-infrared 3.7/~m atmospheric window some low clouds appear warmerthan the sea. A simple analysis of the radiation balance of elements of
. Furthermore, this work lays the foundation for the use of global infrared radiance measurements from satellite instruments to ascertain global climate trends and test general circulation models. Acknowledgments The data used in this analysis were obtained from the Atmospheric Radiation Measurement Program (ARM) sponsored by the U.S. Department of Energy, Office of Science, Office of Biological and Environmental Research, Climate and Environmental Sciences Division. This work was supported by NASA Grant
. Furthermore, this work lays the foundation for the use of global infrared radiance measurements from satellite instruments to ascertain global climate trends and test general circulation models. Acknowledgments The data used in this analysis were obtained from the Atmospheric Radiation Measurement Program (ARM) sponsored by the U.S. Department of Energy, Office of Science, Office of Biological and Environmental Research, Climate and Environmental Sciences Division. This work was supported by NASA Grant
promise in simulating atmospheric radiation more accurately and efficiently. However, there are still unresolved issues surrounding gaseous transmission in climate models. In this work we focus on two of these unresolved problems. The first is the overlapping of solar and infrared spectra. In almost all radiation models the shortwave and longwave portions of atmospheric radiation are treated separately due to the different transfer properties within each wavelength range. Usually the solar (shortwave
promise in simulating atmospheric radiation more accurately and efficiently. However, there are still unresolved issues surrounding gaseous transmission in climate models. In this work we focus on two of these unresolved problems. The first is the overlapping of solar and infrared spectra. In almost all radiation models the shortwave and longwave portions of atmospheric radiation are treated separately due to the different transfer properties within each wavelength range. Usually the solar (shortwave
1. Introduction Radiative transfer is a critical part of the climate system. About 30% of the incoming solar energy is reflected by the Earth–atmosphere system ( Ellingson and Fels 1991 ), while the remaining part is absorbed. To maintain an equilibrium energy state, the thermal infrared radiation is emitted by Earth and the atmosphere. Most greenhouse gases in the atmosphere allow the solar rays to pass through and warm the Earth–atmosphere system but generally prevent infrared radiation from
1. Introduction Radiative transfer is a critical part of the climate system. About 30% of the incoming solar energy is reflected by the Earth–atmosphere system ( Ellingson and Fels 1991 ), while the remaining part is absorbed. To maintain an equilibrium energy state, the thermal infrared radiation is emitted by Earth and the atmosphere. Most greenhouse gases in the atmosphere allow the solar rays to pass through and warm the Earth–atmosphere system but generally prevent infrared radiation from
564 JOURNAL OF APPLIEI) METEOROLOGY Vor-u~3Analysis and Interpretation of TIROS H Infrared Radiation Measurements R. S. HAw~I.~sAir Force Cambridge Research Laboratories, Bedford, Mass.(Manuscript received 6 March 1964, in revised form 6 May 1964)ABSTRACT Infrared radiation data obtained by the TIROS II meteorological satellite are discussed in relation to afrontal system over North America. It
564 JOURNAL OF APPLIEI) METEOROLOGY Vor-u~3Analysis and Interpretation of TIROS H Infrared Radiation Measurements R. S. HAw~I.~sAir Force Cambridge Research Laboratories, Bedford, Mass.(Manuscript received 6 March 1964, in revised form 6 May 1964)ABSTRACT Infrared radiation data obtained by the TIROS II meteorological satellite are discussed in relation to afrontal system over North America. It
coverage results from the gaseous absorption present within these channels, while the window channels are relatively unaffected. In the following subsection, the temperature and water vapor profile information from AIRS is used to sort variability in Δ T b because both temperature and water vapor will affect the emission of infrared radiation in channels with gaseous absorption and may couple to spatial and spectral mismatches. b. Correlation of ΔT b to temperature and water vapor profiles In Fig. 6
coverage results from the gaseous absorption present within these channels, while the window channels are relatively unaffected. In the following subsection, the temperature and water vapor profile information from AIRS is used to sort variability in Δ T b because both temperature and water vapor will affect the emission of infrared radiation in channels with gaseous absorption and may couple to spatial and spectral mismatches. b. Correlation of ΔT b to temperature and water vapor profiles In Fig. 6
1. Introduction When thermal infrared (IR) radiation (often termed longwave radiation, in comparison to the solar radiation of shorter wavelength) emitted by the earth’s surface is transmitted through the atmosphere, it is absorbed by greenhouse gases such as water vapor, carbon dioxide, ozone, etc., as well as by clouds. The atmosphere radiates thermal emission back to the surface in return and thus maintains a much higher surface temperature than otherwise (if the atmosphere did not exist
1. Introduction When thermal infrared (IR) radiation (often termed longwave radiation, in comparison to the solar radiation of shorter wavelength) emitted by the earth’s surface is transmitted through the atmosphere, it is absorbed by greenhouse gases such as water vapor, carbon dioxide, ozone, etc., as well as by clouds. The atmosphere radiates thermal emission back to the surface in return and thus maintains a much higher surface temperature than otherwise (if the atmosphere did not exist
