Climate Studies with a Multi-Layer Energy Balance Model. Part I: Model Description and Sensitivity to the Solar Constant

Li, Peng; Chou, Ming-Dah; Arking, Albert

doi:10.1175/1520-0469(1982)039<2639:cswaml>2.0.co;2

Cited by 48 publications

(30 citation statements)

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“…Values of p c were taken from ISCCP-D2 for low, mid, and high-level clouds. The ISCCP-D2 does not provide dp c data, so these were estimated from Peng et al (1982) for the Northern Hemisphere, as explained in the work by Hatzianastassiou and Vardavas (1999), while dp c values for Southern Hemisphere were estimated in the way described by Hatzianastassiou and Vardavas (2001), by combining the values from Peng et al and those derived from Liou (1992). A complete topography scheme is included in the model, which uses surface pressure, p s , data taken either from NCEP/NCAR or from ECMWF Global Reanalysis Projects gridded in 2.5 • by 2.5 • pixels for each month of the period 1984-1997.…”

Section: Aerosol Particlesmentioning

confidence: 99%

“…On a 14-year basis (1984)(1985)(1986)(1987)(1988)(1989)(1990)(1991)(1992)(1993)(1994)(1995)(1996)(1997), the Earth is found to reflect back-to-space 101.2 Wm −2 from the global mean received 341.5 Wm −2 , resulting in a long-term planetary albedo equal to 29.6%. The inter-hemispherical differences are equal to 0.34 Wm −2 for ISR, 1.1 Wm −2 for OSR, 1.43 Wm −2 for the (1985)(1986)(1987)(1988)(1989) 101.0 100.8 100.9 30.10 29.10 29.6 Hatzianastassiou and Vardavas (2001) 103.0 29.6 Hatzianastassiou and Vardavas (1999) 100.8 29.6 NCEP Reanalysis (1982-1994 115.7 33.87 ECMWF Reanalysis (1985Reanalysis ( -1993 103.7 30.36 NASA Reanalysis (1981Reanalysis ( -1992 94.7 27.72 Yang et al (1999) 115.3 Wild et al (1998-ECHAM4) 105.0 30.7 Wild et al (1998-ECHAM3) 107.0 31.29 Li et al (1997) 94.8-111.5 27.6-32.6 Chen and Roeckner (1996) 106.4 31.0 Rossow and Zhang (1995) 111.5 32.6 Vardavas and Koutoulaki (1995) 30.6 Kiehl et al (1994) 96.6 28 Hartmann (1993) 29.20 Liou (1992) 30.0 111.0 Rossow and Lacis (1990) 33.0 Smith and Smith (1987) 29.0 Stephens et al (1981) 30.0 29.7 29.85 Peng et al (1982) 31.0 Ohring and Addler (1978) 31.3 Hoyt (1976) 32.1 34.7 Bridgman (1969) 40.0 …”

Section: Time Seriesmentioning

confidence: 99%

“…Early models for atmospheric radiation transfer attempted to predict the TOA SWRB (e.g. London and Sasamori, 1972;Ohring and Adler, 1978;Stephens et al, 1981;Peng et al, 1982) but they suffered from the lack of reliable model input data with global coverage, since they used mostly surface-based data. The availability of accurate global satellite data of cloud, atmospheric and surface properties has made modelling more reliable.…”

Section: Introductionmentioning

confidence: 99%

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Long-term global distribution of earth's shortwave radiation budget at the top of atmosphere

et al. 2004

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Abstract. The mean monthly shortwave (SW) radiation budget at the top of atmosphere (TOA) was computed on 2.5 • longitude-latitude resolution for the 14-year period from 1984 to 1997, using a radiative transfer model with long-term climatological data from the International Satellite Cloud Climatology Project (ISCCP-D2) supplemented by data from the National Centers for Environmental Prediction -National Center for Atmospheric Research (NCEP-NCAR) Global Reanalysis project, and other global data bases such as TIROS Operational Vertical Sounder (TOVS) and Global Aerosol Data Set (GADS). The model radiative fluxes at TOA were validated against Earth Radiation Budget Experiment (ERBE) S4 scanner satellite data (1985)(1986)(1987)(1988)(1989). The model is able to predict the seasonal and geographical variation of SW TOA fluxes. On a mean annual and global basis, the model is in very good agreement with ERBE, overestimating the outgoing SW radiation at TOA (OSR) by 0.93 Wm −2 (or by 0.92%), within the ERBE uncertainties. At pixel level, the OSR differences between model and ERBE are mostly within ±10 Wm −2 , with ±5 Wm −2 over extended regions, while there exist some geographic areas with differences of up to 40 Wm −2 , associated with uncertainties in cloud properties and surface albedo. The 14-year average model results give a planetary albedo equal to 29.6% and a TOA OSR flux of 101.2 Wm −2 . A significant linearly decreasing trend in OSR and planetary albedo was found, equal to 2.3 Wm −2 and 0.6% (in absolute values), respectively, over the 14-year period (from January 1984 to December 1997)

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Section: Aerosol Particlesmentioning

confidence: 99%

Section: Time Seriesmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Long-term global distribution of earth's shortwave radiation budget at the top of atmosphere

et al. 2004

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“…This parameter is estimated (as in Hatzianastassiou et al, 1999) from the ISCCP-D2 cloud-top pressure and the cloud physical thickness values given by Peng et al (1982).…”

Section: Input Datamentioning

confidence: 99%

Ten-year global distribution of downwelling longwave radiation

Pavlakis

Hatzidimitriou²,

Matsoukas³

et al. 2004

Atmos. Chem. Phys.

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Abstract. Downwelling longwave fluxes, DLFs, have been derived for each month over a ten year period (1984)(1985)(1986)(1987)(1988)(1989)(1990)(1991)(1992)(1993), on a global scale with a spatial resolution of 2.5×2.5 degrees and a monthly temporal resolution. The fluxes were computed using a deterministic model for atmospheric radiation transfer, along with satellite and reanalysis data for the key atmospheric input parameters, i.e. cloud properties, and specific humidity and temperature profiles. The cloud climatologies were taken from the latest released and improved International Satellite Climatology Project D2 series. Specific humidity and temperature vertical profiles were taken from three different reanalysis datasets; NCEP/NCAR, GEOS, and ECMWF (acronyms explained in main text). DLFs were computed for each reanalysis dataset, with differences reaching values as high as 30 Wm −2 in specific regions, particularly over high altitude areas and deserts. However, globally, the agreement is good, with the rms of the difference between the DLFs derived from the different reanalysis datasets ranging from 5 to 7 Wm −2 . The results are presented as geographical distributions and as time series of hemispheric and global averages. The DLF time series based on the different reanalysis datasets show similar seasonal and inter-annual variations, and similar anomalies related to the 86/87 El Niño and 89/90 La Niña events. The global ten-year average of the DLF was found to be between 342.2 Wm −2 and 344.3 Wm −2 , depending on the dataset. We also conducted a detailed sensitivity analysis of the calculated DLFs to the key input data. Plots are given that can be used to obtain a quick assessment of the sensitivity of the DLF to each of the three key climatic quantities, for specific climatic conditions corresponding to different regions of the globe. Our model downwelling fluxes are validated against available data from ground-based stations distributed over the globe, as given by the Baseline Surface Radiation Network.Correspondence to: I. Vardavas (vardavas@iesl.forth.gr) There is a negative bias of the model fluxes when compared against BSRN fluxes, ranging from −7 to −9 Wm −2 , mostly caused by low cloud amount differences between the station and satellite measurements, particularly in cold climates. Finally, we compare our model results with those of other deterministic models and general circulation models.

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“…Another cloud parameter that is particularly relevant to LW radiative fluxes at the Earth's surface, and not provided by ISCCP, is the cloud-base temperature (or height). This parameter is estimated as in Hatzianastassiou et al (1999) from the ISCCP-D2 cloud-top pressure and the cloud physical thickness values given by Peng et al (1982). This approximate treatment of the cloud-base temperature is shown (Pavlakis et al, 2004) to be sufficient if the required accuracy for the LW radiation at the surface is of the order of 1-2 W m −2 .…”

Section: Climatological Datamentioning

confidence: 99%

Ten year radiation budget of the Earth: 1984–93

Hatzianastassiou

Matsoukas

Hatzidimitriou

et al. 2004

Intl Journal of Climatology

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A 10 year climatology is given of the global distributions of net shortwave (SW), net longwave (LW) and net all-wave radiation budget at both top-of-atmosphere (TOA) and at the Earth's surface, on a mean monthly basis, computed with a radiative transfer model with input data for key atmospheric and surface parameters. The model input data were taken from complete and comprehensive global climatological data sets, such as the International Satellite Cloud Climatology Project, the National Centers for Environmental Prediction and National Center for Atmospheric Research Global Reanalysis or the TIROS Operational Vertical Sounder, among others. Seasonal and latitudinal variations and mean annual and mean hemispherical and global averages are given, based on model results computed for each month of the period from January 1984 to December 1993. At TOA, the net incoming SW radiation has larger latitudinal variation and range of values (0-400 W m −2 ) than the outgoing LW radiation (100-350 W m −2 ). At the surface, the net downward SW radiation has similar features to that at TOA, but with smaller magnitudes. The net upward LW radiation is quite different than at TOA, with a smaller seasonal and geographical variability than the surface net SW radiation. The global system of Earth-atmosphere is found to be net radiatively heated at TOA by 3 W m −2 ; the Earth's surface is net heated by 98 W m −2 , mainly due to solar absorption equal to 147 W m −2 , a value in agreement with surface-based measurements. At TOA, there is a radiative energy surplus between 40°S and 30°N and a radiative loss poleward; however, at the surface the surplus regions extend from 70°S to 70°N. Globally, the atmosphere is found to absorb 27% of the incoming solar radiation at TOA, while it emits 79% of the outgoing terrestrial radiation.

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Climate Studies with a Multi-Layer Energy Balance Model. Part I: Model Description and Sensitivity to the Solar Constant

Cited by 48 publications

References 0 publications

Long-term global distribution of earth's shortwave radiation budget at the top of atmosphere

Long-term global distribution of earth's shortwave radiation budget at the top of atmosphere

Ten-year global distribution of downwelling longwave radiation

Ten year radiation budget of the Earth: 1984–93

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