The following example shows how to cite the use of this data set in a publication. For more information, see our Use and Copyright Web page.
Norouzi, H., M. Temimi, W. B. Rossow, and R. Khanbilvardi. 2013. AMSR-E/Aqua Monthly Global Microwave Land Surface Emissivity. [indicate subset used]. Boulder, Colorado USA: NASA DAAC at the National Snow and Ice Data Center.
Norouzi, H., M. Temimi, W. Rossow, C. Pearl, M. Azarderakhsh, and R. Khanbilvardi. 2011. The Sensitivity of Land Emissivity Estimates from AMSR-E at C- and X-Bands to Surface Properties. Journal of Hydrology, Earth Systems Science 15:3577-3589. http://dx.doi.org/10.5194/hess-15-3577-2011.
July 2002 – June 2008
Land surface emissivity
Data are stored as 64-bit (8-byte) floating-point integers in Version 4 Hierarchical Data Format (HDF4) files. The files contain a data layer for each channel, such as the 6.9 V layer, which contains all the 6.9 GHz vertically-polarized measurements.
Data in compressed HDF files are arranged in a table format that image processing programs can easily visualize. This data compression should be transparent to most users since HDF-capable software tools automatically uncompress the data. Various software packages, such as HDFView, Panoply, or similar HDF-compatible applications, support the HDF data format. Visit the HDF–EOS Tools and Information Center Web page for more information about the HDF format, and for instructions on uncompressing and converting the data to binary format.
Data files are organized on the FTP site at: ftp://sidads.colorado.edu/pub/DATASETS/nsidc0543_amsre_emiss/
The files are named according to the following convention, which is parsed and described in Table 1:
|CREST||Identifies this as a file containing data compiled at the National Oceanic and Atmospheric Administration Cooperative Remote Sensing Science and Technology Center (NOAA-CREST)|
|VX||Version number (V1: Version 1)|
|.hdf||HDF file extension|
Each file is approximately 95 MB.
The volume of this data set is approximately 7.2 GB.
Data provide full global coverage at a quarter-degree latitude and longitude resolution.
The quarter-degree data are in one global cylindrical, equidistant latitude-longitude projection, and are gridded with 1440 columns and 720 rows.
The data span from July 2002 to June 2008 and are provided at a monthly resolution.
Land surface emissivity estimates for this data set were collected at the following vertically and horizontally polarized (H- and V-pol) frequencies: 6.9, 10.65, 18.7, 23.8, 36.5, and 89.0 GHz. Valid land surface emissivity values range from 0.000 to 1.000. Missing values are filled with -999.
Figure 2 shows a sample data record.
Figure 2. This sample data record shows land surface emissivity data values in the vertically-polarized 10.7 GHz channel for December 2005.
Data are available via FTP.
For information on AMSR-E, please refer to the AMSR-E Instrument Description document.
This product is a global land emissivity product using passive microwave observations from the Advanced Microwave Scanning Radiometer - Earth Observing System (AMSR-E). The developed product complements existing land emissivity products from the Special Sensor Microwave Imager (SSM/I) and from the Advanced Microwave Sounding Unit (AMSU) by adding land emissivity estimates at two lower frequencies, 6.9 and 10.65 GHz (in the C- and X-band, respectively). Observations at these low frequencies penetrate deeper into the soil layer.
Ancillary data used in the analysis, such as surface skin temperature and cloud mask, are obtained from International Satellite Cloud Climatology Project (ISCCP). Atmospheric properties are obtained from the TIROS Operational Vertical Sounder (TOVS) observations to determine the small upwelling and downwelling atmospheric emissions as well as the atmospheric transmission. This data set was extracted from instantaneous emissivity estimates.
Land surface emissivity estimates for this data set were derived from the AMSR-E/Aqua L2A Global Swath Spatially-Resampled Brightness Temperatures, Version 2 data set.
AMSR-E is a twelve-channel, six-frequency, total power passive-microwave radiometer system. It measures brightness temperatures at 6.925, 10.65, 18.7, 23.8, 36.5, and 89.0 GHz (Njoku and Li, 1999). Vertically and horizontally polarized measurements are made at all frequencies. The Earth-emitted microwave radiation is collected by an offset parabolic reflector 1.6 m in diameter that scans across the Earth along an imaginary conical surface, maintaining a constant Earth incidence angle of 55 degrees. The spatial resolution of the individual measurements varies from 5.4 km at 89.0 GHz to 56 km at 6.9 GHz. AMSR-E/Aqua L2A Global Swath Spatially-Resampled Brightness Temperatures (for both ascending and descending overpasses) were used for the analysis and were obtained from the National Snow and Ice Data Center (NSIDC). Higher frequency observations are resampled to match the lower frequencies spatial resolution. For each frequency, we select the resampled data having the closest location to the original satellite footprint and re-project these footprints to a 0.25 degree grid that is equidistant at the equator.
Satellite infrared-visible-based products from the International Satellite Cloud Climatology Project (ISCCP) provide cloud cover and surface skin temperatures. The ISCCP-DX data provides information every three hours since 1983 at approximately 30 km spatial resolution, based on merged observations from geostationary and polar-orbiting satellites (Rossow and Schiffer, 1999). The ISCCP quantities were chosen for the satellite view closest to nadir from among all available results and resampled to match the quarter-degree equidistant grid adopted for the passive microwave observations. The infrared-based skin temperatures represent the top surface temperature, which can be the top of very dense vegetation canopies or a mix of canopy and soil temperatures for less dense vegetation.
The TOVS data set available with ISCCP (Rossow and Schiffer, 1991) provides global information on air temperature and water vapor profiles at nine vertical layers ranging from the surface to 1 mb pressure. These profiles are available on a daily basis. We assume that the impact of diurnal variations on the observed brightness temperature is minimal. Data are originally available in a 280 km equal-area map, but are regridded to coincide with the AMSR-E data. These atmospheric parameters are used to calculate the upwelling and downwelling brightness temperatures, as well as the atmospheric transmission. TOVS data were selected in this study to be consistent with ISCCP products such as skin temperature, which is also based on TOVS data. See Zhang et al. (2006) for comparisons of the TOVS product with other atmospheric data sets.
Assuming that land surface is flat and specular, and considering the atmosphere as a non-scattering plane-parallel medium, the emissivity can be written as:
where and are the land surface emissivity and the measured brightness temperatures at polarization p (horizontal, H, or vertical, V) and frequency , respectively. Ts is the skin temperature and and are the downwelling and upwelling brightness temperatures from the atmosphere, respectively:
In these equations, is the atmospheric temperature profile, the atmospheric absorption at altitude , the cosine of incidence angle, and the atmospheric extinction between two altitudes, which is written as:
The implementation of this algorithm requires an accurate characterization of the atmospheric temperature and humidity to determine atmospheric transmissivity. Another key parameter is the thermal skin temperature.
AMSR-E overpass times are near 1:30 a.m. (ascending) and 1:30 p.m. (descending) local time at the equator. Since skin temperatures from ISCCP-DX data are available every three hours, microwave and thermal observations are not necessarily coincident. Therefore, a Spline interpolation between the eight available skin temperature measurements every day is used to infer the complete skin temperature diurnal cycle. The Spline method estimates the daily maxima and minima that can occur between two 3-hour samples (Aires et al., 2004). Actual acquisition time for each microwave pixel at each swath is used in the Spline interpolation to estimate more accurately the physical temperature. This may be critical in arid regions where the temperature diurnal cycle has much larger amplitude. Also, if either of two consecutive (before and after AMSR-E acquisition times) cloud flags indicates cloudy conditions, the microwave pixel is flagged as cloudy.
The upwelling and downwelling atmospheric emissions are estimated using the Liebe MPM model to determine the atmospheric absorption (Liebe et al., 1993). Upwelling and downwelling brightness temperatures, as well as atmospheric transmission, are calculated using Equations 2, 3, and 4 for the AMSR-E incidence angle of 55 degrees. Atmospheric corrections are applied to the ascending and descending overpasses. Because of the TOVS daily resolution, the same atmospheric profiles are used to correct atmospheric effects for both the ascending and descending overpasses.
Monthly composite emissivity maps are created for each frequency and polarization from the instantaneous cloud-free land surface emissivity maps. In the case of persistent cloud cover (longer than 30 days, which is possible in some tropical locations), land emissivity is not retrieved (resulting in a data value of -999).
The uncertainty in the atmospheric water vapor profile can be as much as 20-25 percent (English, 1995; Lin and Rossow, 1994; Zhang et al., 2006). A 25 percent change in water vapor leads to a global mean 0.0016 change of emissivity at 6.9 GHz and 0.03 at 89.0 GHz. TOVS data may include climatological values when actual measures are missing which can introduce an error in the atmospheric corrections (Prigent et al., 1998).
The physical skin temperature plays an important role at lower frequencies, since the microwave radiation is more sensitive to the surface than to the atmosphere. Recent studies show that available global skin temperatures have significant differences, generally only a few degrees but up to 20 K in deserts (Jimenez et al., 2011). ISCCP skin temperature has some uncertainties that tend to increase as temperature increases. The recent study shows that root mean square (rms) differences between ISCCP and MODIS skin temperature could be 5 K and 2.5 K for day and night, respectively (Moncet et al., 2011). The sensitivity analysis showed that the difference in global mean emissivity retrieval could be as much as 0.025 for skin temperature differences of 5 K. Although possible biases in skin temperatures from ISCCP can affect the absolute emissivity value, its effect on emissivity variability should not be significant during the AMSR-E operational life time because the ISCCP results are homogeneous in quality over this time period (Zhang et al., 2006). ISCCP-DX also was used for cloud detection. Possible discrepancies in cloud mask can affect the retrieval.
A 3 K decrease in observed brightness temperature leads to 0.01 decrease of emissivity at 36.5 GHz (H. polarization). The absolute accuracy of AMSR-E brightness temperatures has been reported as 1.0 K (Kawanishi et al., 2003).
Several quality controls have been conducted and the standard deviation of instantaneous emissivity estimates within each month to be less than 0.015. The results have been also evaluated with other available global data such as SSM/I.
Aires, F., C. Prigent, and W. B. Rossow. 2004. Temporal Interpolation of Global Surface Skin Temperature Diurnal Cycle over Land under Clear and Cloudy Conditions. Journal of Geophysical Research-Atmospheres. 109. doi:10.1029/2003jd003527.
English, S. J. 1995. Airborne Radiometric Observations of Cloud Liquid-Water Emission at 89 and 157 GHz – Application to Retrieval of Liquid-Water Path. Quarterly Journal of the Royal Meteorological Society. 121:1501-1524.
Jimenez, C., C. Prigent, B. Mueller, S. I. Seneviratne, M. F. McCabe, E. F. Wood., W. B. Rossow, G. Balsamo, A. K. Betts, P. A. Dirmeyer, J. B. Fisher, M. Jung, M. Kanamitsu, R. H. Reichle, M. Reichstein, M. Rodell, J. Sheffield, K. Tu, and K. Wang. 2011. Global Intercomparison of 12 Land Surface Heat Flux Estimates. Journal of Geophysical Research-Atmospheres. 116. doi:10.1029/2010jd014545.
Kawanishi, T., T. Sezai, Y. Ito, K. Imaoka, T. Takeshima, Y. Ishido, A. Shibata, M. Miura, H. Inahata, and R. W. Spencer. 2003. The Advanced Microwave Scanning Radiometer for the Earth Observing System (AMSR-E), NASDA's Contribution to the EOS for Global Energy and Water Cycle Studies. IEEE Transactions on Geoscience and Remote Sensing, 41:184-194. doi:10.1109/tgrs.2002.808331.
Liebe, H. J., G. A. Hufford, and M. G. Cotton. 1993. Propagation Modelling of Moist Air and Suspended Water/Ice Particles at Frequencies below 1000 GHz. Specialist Meeting of the Electromagnetic Wave Propagation Panel Symposium, AGARD Conference Proceedings 542, Atmospheric Propagation Effects through Natural and Man–Made Obscurants for Visible through MW-Wave Radiation, March 1–10, 1993: Palma de Mallorca, Spain.
Moncet, J., P. Liang, A. Lipton, J. Galantowicz, and C. Prigent. 2011. Discrepancies between MODIS and ISCCP Land Surface Temperature Products Analyzed with Microwave Measurements. J. Geophys. Res. doi:10.1029/2010JD015432.
Norouzi, H., M. Temimi, W. Rossow, C. Pearl, M. Azarderakhsh, and R. Khanbilvardi. 2011. The Sensitivity of Land Emissivity Estimates from AMSR-E at C- and X-Bands to Surface Properties. Journal of Hydrology, Earth Systems Science. 15:3577–3589. doi:10.5194/hess-15-3577-2011.
Norouzi, H., W. Rossow, M. Temimi, C. Prigent, M. Azarderakhsh, S. Boukabara, and R. Khanbilvardi. 2012. Using Microwave Brightness Temperature Diurnal Cycle To Improve Emissivity Retrievals Over Land. Remote Sensing of Environment. 123:470–482. doi:10.1016/j.rse.2012.04.015.
Zhang, Y. C., Rossow, W. B., and Stackhouse, P. W. 2006. Comparison of Different Global Information Sources used in Surface Radiative Flux Calculation: Radiative Properties of the Near-Surface Atmosphere. Journal of Geophysical Research-Atmospheres. 111. doi:10.1029/2005jd006873.
New York City College of Technology, The City University of New York (CUNY)
NOAA Cooperative Remote Sensing Science and Technology Center (NOAA-CREST)
300 Jay Street, Vorhees 424
Brooklyn, New York USA 11201
Marouane Temimi, William B. Rossow, Reza Khanbilvardi
The City College of New York (CCNY), CUNY
NOAA Cooperative Remote Sensing Science and Technology Center (NOAA-CREST)
160 Convent Ave, Steinman Hall (T-107)
New York, New York USA 10031
NSIDC User Services
National Snow and Ice Data Center
CIRES, 449 UCB
University of Colorado
Boulder, CO 80309-0449 USA
phone: +1 303.492.6199
fax: +1 303.492.2468
form: Contact NSIDC User Services
This study was partially supported by National Oceanic and Atmospheric Administration (NOAA) under grant NA06OAR4810162, and NASA Energy and Water Study (NEWS) under grant NNXD7AO90G.
The acronyms used in this document are listed in Table 2.
|AMSR-E||Advanced Microwave Scanning Radiometer - Earth Observing System|
|AMSU||Advanced Microwave Sounding Unit|
|CCNY||City College of New York|
|CUNY||City University of New York|
|CREST||Cooperative Remote Sensing Science and Technology Center|
|EOS||Earth Observing System|
|FTP||File Transfer Protocol|
|HDF-EOS||Hierarchical Data Format - EOS|
|ISCCP||International Satellite Cloud Climatology Project|
|MODIS||Moderate Resolution Imaging Spectroradiometer|
|NASA||National Aeronautics and Space Administration|
|NEWS||NASA Energy and Water Study|
|NOAA||National Oceanic and Atmospheric Administration|
|NSIDC||National Snow and Ice Data Center|
|RFI||Radio Frequency Interference|
|RMS||Root Mean Square|
|SSM/I||Special Sensor Microwave Imager|
|TIROS||Television Infrared Observation Satellite Program|
|TOVS||TIROS Operational Vertical Sounder|