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We kindly request that you cite the use of this data set in a publication using the following citation example. For more information, see our Use and Copyright Web page.Cavalieri, D. J., T. Markus, and J. C. Comiso. 2014. AMSR-E/Aqua Daily L3 12.5 km Brightness Temperature, Sea Ice Concentration, & Snow Depth Polar Grids. Version 3. [indicate subset used]. Boulder, Colorado USA: NASA DAAC at the National Snow and Ice Data Center. http://dx.doi.org/10.5067/AMSR-E/AE_SI12.003
Advanced Microwave Scanning Radiometer - Earth Observing System (AMSR-E)
North and south polar regions
Data were collected from 01 June 2002 to 3 October 2011.
Daily averages, daily ascending averages, and daily descending averages. Snow depths are five-day running averages.
Version 3. See the AMSR-E Data Versions Web page for previous version information.
Please see the Ordering AMSR-E Products from NSIDC Web page for a list of order options.
Donald J. Cavalieri
Laboratory for Hydrospheric Processes
NASA Goddard Space Flight Center
Laboratory for Hydrospheric Processes
NASA Goddard Space Flight Center
Laboratory for Hydrospheric Processes
NASA Goddard Space Flight Center
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
Data are stored in Hierarchical Data Format - Earth Observing System (HDF-EOS) format.
Refer to the Level-3 12.5 km Sea Ice Data Fields document for a list of HDF-EOS data fields.
This section explains the file naming convention used for this product with examples.
Example file name:
Refer to Table 1 for the values of the file name variables listed above.
|X||Product Maturity Code (Refer to Table 2 for valid values.)|
|##||file version number|
|hdf||Hierarchical Data Format (HDF)|
|P||Preliminary - refers to non-standard, near-real-time data available from NSIDC. These data are only available for a limited time until the corresponding standard product is ingested at NSIDC.|
|B||Beta - indicates a developing algorithm with updates anticipated.|
|T||Transitional - period between beta and validated where the product is past the beta stage, but not quite ready for validation. This is where the algorithm matures and stabilizes.|
|V||Validated - products are upgraded to Validated once the algorithm is verified by the algorithm team and validated by the validation teams. Validated products have an associated validation stage. Refer to Table 3 for a description of the stages.|
|Stage 1||Product accuracy is estimated using a small number of independent measurements obtained from selected locations, time periods, and ground-truth/field program efforts.|
|Stage 2||Product accuracy is assessed over a widely distributed set of locations and time periods via several ground-truth and validation efforts.|
|Stage 3||Product accuracy is assessed, and the uncertainties in the product are well-established via independent measurements made in a systematic and statistically robust way that represents global conditions.|
Table 4 provides examples of file name extensions for related files that further describe or supplement data files.
Extensions for Related Files
|.qa||Quality assurance information|
|.ph||Product history data|
Each daily granule is approximately 53 MB.
Figure 1. Northern Hemisphere
Figure 2. Southern Hemisphere
The spatial resolution of the polar grids is 12.5 km.
Brightness temperature grids are in a polar stereographic projection, which specifies a projection plane such as the grid, tangent to the Earth at 70 degrees. The planar grid is designed so that the grid cells at 70 degrees latitude are 12.5 km by 12.5 km. For more information on this topic please refer to Pearson (1990) and Snyder (1987).
The polar stereographic projection often assumes that the plane (grid) is tangent to the Earth at the pole. Thus, there is a one-to-one mapping between the Earth's surface and grid with no distortion at the pole. Distortion in the grid increases as the latitude decreases because more of the Earth's surface falls into any given grid cell. At the edge of the northern polar grid distortion reaches 31 percent. The southern polar grid has a maximum distortion of 22 percent. To minimize the distortion, the projection is true at 70 degrees rather than at the poles. This increases the distortion at the poles by three percent and decreases the distortion at the grid boundaries by the same amount. The latitude of 70 degrees was selected so that little or no distortion would occur in the marginal ice zone. Another result of this assumption is that fewer grid cells will be required as the Earth's surface is more accurately represented.
The polar stereographic formulae for converting between latitude/longitude and X-Y grid coordinates are taken from (Snyder 1982). This projection assumes a Hughes ellipsoid with a radius of 3443.992 nautical mi or 6378.273 km and an eccentricity (e) of 0.081816153 (or e2 = 0.006693883). The structural metadata (StructMetadata.0) built into the HDF-EOS data file lists the squared eccentricity value rounded to four significant digits (0.006694).
Northern Hemisphere: 608 columns by 896 rows
Southern Hemisphere: 632 columns by 664 rows
The origin of each x, y grid is the pole. The grids' approximate outer boundaries are defined in the following table. Corner points are listed; apply values to the polar grids reading clockwise from upper left. Interim rows define boundary midpoints.
For this product, there are files that contain geolocation and pixel-area tools, which provide the same functionality for all polar stereographic passive microwave sea ice data sets at NSIDC. These tools include a FORTRAN routine called locate.for, a latitude/longitude grid, and a pixel-area grid.
The following geocoordinate FORTRAN tools are available via FTP:
The latitude/longitude grids are in binary format and are stored as long word integers (4 byte) scaled by 100,000. Each array location (i,j) contains the latitude or longitude value at the center of the corresponding data grid cells. These files are available via FTP.
|pss||polar stereographic southern projection|
|psn||polar stereographic northern projection|
|06, 12, & 25||6 km, 12 km, and 25 km, respectively|
Data were collected from 01 June 2002 to 3 October 2011.
Brightness temperatures and sea ice concentrations are daily averages, daily ascending averages, and daily descending averages. Snow depths are five-day running averages.
Brightness Temperature (K)
Snow Depth on Sea Ice
Sea Ice Concentration
Sea Ice Concentration differences between Bootstrap Basic Algorithm (BBA) and Enhanced NASA Team (NT2)
Refer to the Level-3 12.5 km Sea Ice Data Fields document for more information regarding the Sea Ice parameters.
This data set contains the following gridded parameters:
Refer to the Ordering AMSR-E Products from NSIDC Web page for a list of order options.
Each HDF-EOS file contains core metadata with Quality Assessment (QA) metadata flags that are set by the Science Investigator-led Processing System (SIPS) at the Global Hydrology and Climate Center (GHCC) prior to delivery to NSIDC. A separate metadata file in XML format is also delivered to NSIDC with the HDF-EOS file; it contains the same information as the core metadata. Three levels of QA are conducted with the AMSR-E Level- 2 and -3 products: automatic, operational, and science QA. If a product does not fail QA, it is ready to be used for higher-level processing, browse generation, active science QA, archive, and distribution. If a granule fails QA, SIPS does not send the granule to NSIDC until it is reprocessed. Level-3 products that fail QA are never delivered to NSIDC (Conway 2002).
Weather filters are employed for the Level-3 sea ice products to eliminate spurious sea ice concentrations over open ocean resulting from varying atmospheric emission. The weather filters are based on threshold values for the spectral gradient radio and thresholds derived from brightness temperature differences. Sea ice products are checked to see if ice concentration values fall within reasonable limits. Diagnostics are based in part on satellite sea ice climatology developed since the Scanning Multichannel Microwave Radiometer (SMMR) era in 1978.
AMSR-E Level-2A data arriving at GHCC are subject to operational QA prior to processing higher-level products. Operational QA varies by product, but it typically checks for the following criteria in a given file (Conway 2002):
AMSR-E Level-2A data arriving at GHCC are also subject to science QA prior to processing higher-level products. If less than 50 percent of a granule's data is good, the science QA flag is marked suspect when the granule is delivered to NSIDC. In the SIPS environment, the science QA includes checking the maximum and minimum variable values, and percent of missing data and out-of-bounds data per variable value. At the Science Computing Facility (SCF), also at GHCC, science QA involves reviewing the operational QA files, generating browse images, and performing the following additional automated QA procedures (Conway 2002):
Geolocation errors are corrected during Level-2A processing to prevent processing anomalies such as extended execution times and large percentages of out-of-bounds data in the products derived from Level-2A data.
The Team Lead SIPS (TLSIPS) developed tools for use at SIPS and SCF for inspecting the data granules. These tools generate a QA browse image in Portable Network Graphics (PNG) format and a QA summary report in text format for each data granule. Each browse file shows Level-2A and Level-2B data. These are forwarded from RSS to GHCC along with associated granule information, where they are converted to HDF raster images prior to delivery to NSIDC.
Refer to the AMSR-E Validation Data Web page for information about data used to check the accuracy and precision of AMSR-E observations.
Refer to the AMSR-E Data Quality Web site for more information on quality assessment
Sea ice concentration products are used to understand the spatial characterization of sea ice cover and to calculate sea ice extent and area for time series analyses and process studies in the Arctic and Antarctic. Passive microwave data are particularly useful for sea ice studies because of the relatively high contrast in emissivities between open water and sea ice. This contrast is frequency-dependent; contrast increases with decreasing channel frequency. In most algorithms, atmospheric effects are assumed constant. The satellite-received radiation, expressed as a Brightness Temperature (Tb), is as follows (Cavalieri and Comiso 2000):
Tb = TbwCw + TbiCi
Tbw = brightness temperature of open water
Tbi = brightness temperature of sea ice
Cw = fraction of open water within instrument field-of-view
Ci = fraction of sea ice concentration within the instrument field-of-view
Sea ice concentration (CI), corresponding to an observed Tb over a sea-ice-covered region (Tb), is derived as follows:
Ci = (Tb - Tbw) / (Tbi - Tbw)
The AMSR-E sea ice algorithms use this equation, but the channels and methods to derive sea ice concentrations are different. Values of brightness temperature of open water, brightness temperature of sea ice, and brightness tempeature all include contributions from the intervening atmosphere. Brightness temperature of sea ice varies spatially because of spatial changes in emissivity and temperature of ice, while brightness temperature of open water is constant for open water within the ice pack.
Observations for the 18.7, 23.8, 36.5, and 89 GHz channels, at native resolutions, from the AMSR-E/Aqua L2A Global Swath Spatially-Resampled Brightness Temperatures are gridded into 12.5 km grid cells using a drop-in-the-bucket method where the grid cell that contains the center of the observation footprint is given the whole weight of the observation. With this procedure, the number of observations is always in whole numbers. All valid brightness temperature observations within the extent of the polar grids are binned into grid cells, including land observations.
Depending on the paramter being investigated, such as sea ice concentration or snow depth on sea ice, a different algorithm is used. Each algorithm is discussed in the following paragraphs.
The 12.5 km sea ice concentration product is generated using the Enhanced NASA Team (NT2) algorithm described by Markus and Cavalieri (2000) for both the Arctic and the Antarctic. NT2 sea ice concentrations are calculated using the individual Level 2-A swaths rather than using gridded averaged brightness temperatures in order to make the atmospheric corrections on an orbit-by-orbit basis before obtaining daily average ice concentrations. However, previous AE_SI12 versions employed the Bootstrap Basic Algorithm (BBA) described by Comiso (1995) for the Antarctic. Now the BBA is only used in the sea ice concentration difference between the BBA and the NT2 (BBA-NT2) for both hemispheres.
The original NASA Team algorithm is based on techniques described in Cavalieri et al. (1984) and Gloersen and Cavalieri (1986). The NT2 algorithm (Markus and Cavalieri 2000) identifies two ice types for both the Arctic and the Antarctic:
|first-year ice||Type A ice consists primarliy of first year ice|
|multiyear ice||Type B represents sea ice with a heavy snow cover resulting in increased scattering at 37V.|
In this algorithm, the primary source of error is attributed to conditions in the surface layer such as surface glaze and layering (Comiso et al. 1997), which can significantly affect the horizontally polarized 18.7 GHz brightness temperature (Matzler et al. 1984) leading to increased PR(18) values and thus an underestimation of sea ice concentration. The use of the horizontally polarized channels makes it imperative to resolve a third ice type to overcome the difficulty of surface effects on the emissivity of the horizontally polarized component.
Thus, one advantage of using the NT2 algorithm is that it uses the 89 GHz channels because the horizontally polarized 89 GHz data are less affected by surface conditions than the horizontally polarized 18.7 GHz data (Matzler et al. 1984), and the 89 GHz channels have successfully been used in sea ice concentration retrievals under clear atmospheric conditions (Lubin et al. 1998). As a result, this algorithm can identify more complex ice types resulting from surface glaze and layering in the snow cover. The thin-ice bias is reduced through the use of the third ice type. The third ice type consists of surface glaze and layering of sea ice with snow cover. This type of ice primarily occurs in the Antarctic.
The Spectral Gradient Ratios (GR) and Polarization Ratios (PRs) are calculated from the observed and modeled brightness temperatures using the following two equations:
The Polarization Equation:
The Spectral Gradient Ratio Equation:
Tb is the brightness temperature at frequency ν for the polarized component p (vertical (V) or horizontal (H)).
The actual radiance ratios used in the NT2 algorithm are PRR(18), PRR(89), GR (89, 18, H-pol), and GR (89, 18, V-pol) where the subscript R refers to a rotation of axes. This rotation is done in the NT PR(18)-GR(37, 18, V-pol) domain, with the axes rotated through an angle, φ, until the ice-type lines (the FY-MY line for the Arctic and the A–B line for the Antarctic) are parallel to the GR axis. The rotated PR is defined by:
and is independent of the two ice types. Next, we make use of the difference between two gradient ratios
to resolve the ambiguity between pixels with true low sea ice concentration and pixels with significant scattering (defined as Ice Type C). Therefore, ΔGR serves as an indicator of the presence of Ice Type C. The higher the value of ΔGR the higher the amount of layering within a pixel. The retrieval of Ice Type C is applied to both, the Arctic and the Antarctic, oceans. Finally, a third parameter is defined to avoid the ambiguity between changes in sea ice concentration and changes in atmospheric conditions, because of the higher sensitivity of the 89-GHz channels to atmospheric variability compared to the lower frequency channels. This third parameter is the rotated PR(89), PRR(89), computed from the PR(89)-GR(37V18V) domain analogous to the calculation of PRR(18) but with a different angle.
The algorithm quantifies atmospheric effects by calculating brightness temperatures for each channel using a forward atmospheric radiative transfer model (Kummerow 1993) that incorporates four surface types: first-year ice, multiyear ice, Type C, and open water. Thus, the 89 GHz channels together with a forward radiative transfer model provide ice concentrations under all atmospheric conditions. Figure 3 shows the general flow of the algorithm. First brightness temperatures are calculated for the four surface types and all weather conditions, currently 12. The response of the brightness temperatures to different weather conditions is calculated using the atmospheric radiative transfer model. The input data for the model consists of several things such as: the emissivities of the different surface types taken from Table 4-1 in Eppler et al. (1992) with modifications to achieve agreement between modeled and observed ratios, different cloud properties, specifically cloud base, cloud top, and cloud liquid water, taken from Fraser et al. (1975), and average atmospheric temperature and humidity profiles for summer and winter conditions taken from Antarctic research stations. Brightness temperatures are calculated for all possible ice concentration combinations in one percent increments, and the following ratios were calculate for each increment: PRR(18), PRR(89), and ΔGR. This creates a prism in which each element within this space contains a vector with the three ratios: PRR(18), PRR(89), and ΔGR. The subscript R refers to a rotation of axes in PR-GR space by the angle so that PRR(18) and PRR(89) are independent of ice types A and B in the Antarctic, and first-year and multiyear ice for the Arctic. For each pixel, the observed brightness temperatures are used to create a vector with the same ratios. The ice concentration for a pixel is determined where the difference between an observed and a modeled ratio is smallest.
Figure 3. Flow Diagram of Enhanced NASA Team Algorithm
While for the Antarctic the algorithm resolves fractions between Ice Types A, B, and C, and open water, in the Arctic we also resolve a thin ice type. Using a GR(37V19V) threshold of -0.02, we either resolve Ice Type C for pixels where GR(37V19V) is below this threshold, or thin ice for pixels where GR(37V19V) is above this threshold. A limitation, of course, is that mixtures of thin ice and thicker ice with layering cannot be resolved.
The algorithm eliminates spurious sea ice concentrations over open ocean by employing weather filters previously used for SSM/I (Gloersen and Cavalieri 1986; Cavalieri et al. 1995). Ice concentrations for image pixels with GR(37V19V) values greater than 0.05 and GR(2219) values greater than 0.045 are set to zero.
Although a land mask is applied to the ice concentration maps, land spillover still leads to erroneous ice concentrations along the coast lines adjacent to open water. This makes operational usage of these maps cumbersome. Therefore, a land spillover correction scheme is applied on the maps.
The BBA (Comiso 1995) is used in the calculation of sea ice concentration differences between the BBA and the NT2 (BBA-NT2) for both hemispheres. Comiso calculated tie points for consolidated ice (Tbi) and open water (Tbw) with two sets of channels: 18.7V GHz and 37V GHz (called V1937), and 37H GHz and 37V GHz (HV37). Using these channels for the retrieval of sea ice concentration ensures consistency with historical sea ice products, beginning with SMMR.
Snow depth over sea ice is reported as a 5-day running average, which is based on the current day and the previous four days. The 12.5 km snow depth on sea ice product is generated
using the AMSR-E snow-depth-on-sea-ice algorithm described by Markus and Cavalieri (1998) for both the Arctic and the Antarctic. However, this algorithm is only valid over seasonal ice. The snow
depth on sea ice is calculated using the spectral gradient ratio of the 18.7 GHz and 36.5
GHz vertical polarization channels:
hs = a1 + a2 GRV(ice)
|hs||Snow depth in meters|
|GRV(ice)||Spectral gradient ratio corrected for the sea ice concentration|
|1Coefficients derived from the linear regression of in situ snow depth measurements on microwave data.|
GRV(ice) = [Tb(37V)-Tb(18V)-k1(1-C)] / [Tb(37V)+Tb(18V)-k2(1-C)]
|Tbo||The Open Water Brightness Temperatures (Tbo) are average values from open ocean areas and are used as constants.|
|C||Sea Ice Concentration|
The principal idea of the algorithm is similar to the AMSR-E snow-on-land algorithm (Kelly et al. 2003) utilizing the assumptions that scattering increases with increasing snow depth and that the scattering efficiency is greater at 36.5 GHz than at 18.7 GHz. For snow-free sea ice, the gradient ratio is close to zero and it becomes more and more negative as the snow depth and grain size increases. The correlation of regional in situ snow depth distributions and satellite-derived snow depth distributions is 0.81. The upper limit for snow depth retrievals is 50 cm, which is a result of the limited penetration depth at 18.7 and 36.5 GHz.
The algorithm is applicable to dry snow conditions only. At the onset of melt, the emissivity of both the 18.7 GHz and the 36.5 GHz channels approach unity (that of a blackbody) and the gradient ratio approaches zero initially before becoming positive. Thus, snow depth is indeterminate under wet snow conditions. Snow, which is wet during the day, frequently refreezes during the night. This refreezing results in very large grain sizes (Colbeck 1982), which leads to a reduced emissivity at 36.5 GHz relative to 18.7 GHz, thereby decreasing GRV(ice) and thus leads to an overestimate of snow depth. These thaw-freeze events cause large temporal variations in the snow depth retrievals. This temporal information is used in the algorithm to flag the snow depths as unretrievable from those periods with large fluctuations.
As in situ grain size measurements are even less frequently collected than snow depth measurements, the influence of grain size variations could not be incorporated into the algorithm. Because of the uncertainties in grain size and density variations as well as sporadic weather effects, AMSR-E daily snow depth products are five-day running averages similar to the AMSR-E snow depth on land product.
Figure 4 summarizes the snow depth algorithm. Snow depths are retrieved for the entire Southern Ocean, but only for the seasonal sea ice zones in the Arctic because the retrieval of Arctic snow depth is complicated by the presence of multiyear ice, which has a signature similar to snow cover on first-year ice. Both multiyear ice and deep snow on top of first-year ice results in increasingly negative values for the spectral GR; therefore, the algorithm only retrieves snow depth in the seasonal sea ice zones and in regions where the value of GR(37V19V) is greater than -0.02. This threshold corresponds to multiyear ice concentration of less than 20 percent. Where GR(37V19V) is less than -0.02, the algorithm flags pixels as multiyear ice. Because of the higher sensitivity of snow depth retrievals to ice concentration less than 20 percent, the algorithm limits snow depth retrievals to ice concentration between 20 -100 percent. Ice concentrations less than 20 percent appear almost exclusively near the ice edge.
Figure 4. Processing Sequence for AMSR-E 25 km Sea Ice Products
Figure 5 summarizes the input products and algorithms used to create gridded AMSR-E 12.5 km sea ice products.
Figure 5. Processing Sequence for AMSR-E 12.5 km Sea Ice Products
The AMSR-E/Aqua L2A Global Swath Spatially-Resampled Brightness Temperatures are binned into 12.5 km grid cells using a drop-in-the-bucket method where the grid cell that contains the center of the observation footprint is given the whole weight of the observation. With this procedure, the number of observations is always in whole numbers. All valid brightness temperature observations within the extent of the polar grids are binned into grid cells, including land observations.
After input Level-2A brightness temperatures are binned into 12.5 km grid cells, the ascending, descending, and daily data are averaged. The daily average is not simply an average of ascending and descending orbits because a given pixel could have, for example, three measurements from ascending orbits and two from descending orbits. Instead, the daily average is of all the observations for that grid cell. For example, if A = ascending and B = descending:
((A1 + A2) / 2 + (B1 + B2 + B3) / 3 ) / 2
is not equal to:
(A1 + A2 + B1 + B2 + B3) / 5
However, this biases day-time ascending orbits over night-time descending.
Northern Hemisphere Masks
Beginning with Version 12 data, the sea ice and snow
melt masks used for the Northern Hemisphere snow depth on sea ice parameter
are stored within this data set. The masks from the most recent HDF
file are used to generate each new HDF file. If the masks used are more than
seven days old, the metadata science quality flag is set to Suspect.
The multiyear mask field in the HDF file refers to the multiyear sea ice mask. A default mask is used to initialize the multiyear mask on the first day of mission and also to reset the mask on the first processing date in October of each year.
The variability 5day field in the HDF file refers to the snow melt mask. The snow melt mask corresponds to the running 5-day snow melt product, and its date must match that of the multiyear mask. The snow melt mask is reset at the same time as the multiyear mask.
Changes to the Version 3 algorithm for these data include:
Refer to the AMSR-E Data Versions Web page for a summary of changes since the start of mission.
Ashcroft and Wentz (2000) discuss errors in the source Level-2A brightness temperatures that were binned into 12.5 km grid cells for this sea ice product. In the sea ice concentration algorithm, the primary source of error is attributed to conditions in the surface layer such as surface glaze and layering (Comiso et al. 1997), which can significantly affect the horizontally polarized 18.7 GHz brightness temperature (Matzler et al. 1984) leading to increased PR(18) values and thus underestimates in ice concentration.
Sources of error in the retrieval of snow depth on sea ice also include inherent errors in sea ice concentration, uncertainty in the linear relationship between snow depth and the AMSR-E brightness temperatures, undetected snow wetness, snow grain size and snow density variability, and sensitivity to extreme weather effects.
Refer to the AMSR-E Instrument Description document.
Cavalieri, D. and J. Comiso. 2000. Algorithm Theoretical Basis Document for the AMSR-E Sea Ice Algorithm, Revised December 1. Landover, Maryland USA: Goddard Space Flight Center.
Comiso, J. and K. Steffen. 2001. Studies of Antarctic Sea Ice Concentrations from Satellite Data and Their Applications. Journal of Geophysical Research 106(C12): 31,361-31,385.
Comiso, J. C., D. J. Cavalieri, C. L. Parkinson, and P. Gloersen. 1997. Passive Microwave Algorithms for Sea Ice Concentration - A Comparison of Two Techniques. Remote Sensing of the Environment 60: 357-384.
Fraser R. S., N. E. Gaut, E. C. Reifenstein, and H. Sievering. 1975. Interaction Mechanisms Within the Atmosphere Including the Manual of Remote Sensing. American Society of Photogrammetry 181-233. Falls Church, VA.
Markus, Thorsten and Donald J. Cavalieri. 2008. [Supplement] AMSR-E Algorithm Theoretical Basis Document: Sea Ice Products. Greenbelt, Maryland USA: Goddard Space Flight Center. (PDF file, 2.10 MB)
Markus, T. and D. Cavalieri. 1998. Snow Depth Distribution over Sea Ice in the Southern Ocean from Satellite Passive Microwave Data. IN: Antarctic Sea Ice: Physical Processes, Interactions, and Variability. Antarctic Research Series 74: 19-39. Washington, DC: American Geophysical Union.
Markus, T., D. Cavalieri, and A. Ivanoff. 2011. Algorithm Theoretical Basis Document for the AMSR-E Sea Ice Algorithm, Revised December 2011. Landover, MD: Goddard Space Flight Center. (PDF file, 528 KB)
Worby, A. P., T. Markus, A. D. Steer, V. I. Lytle, and R. A. Massom. 2008. Evaluation of AMSR-E Snow Depth Product over East Antarctic Sea Ice Using In Situ Measurements and Aerial Photography, Journal of Geophysical Research 113(C05): Art. #C05S94. doi:10.1029/2007JC004181.
For more information regarding related publications, see the Research Using AMSR-E Data Web page.
Sea Ice Products at NSIDC
This site offers a complete summary of sea ice data derived from passive microwave sensors and other sources, and is useful for users who want to compare characteristics of various sea ice products to understand their similarities and differences. This site also provides links to tools for passive microwave data and a list of other sea ice resources.
Sea Ice Trends and Climatologies from SMMR and SSM/I-SSMIS
This site provides a suite of value-added products to aid in investigations of the variability and trends of sea ice cover. These products provide users with information about sea ice extent, total ice covered area, ice persistence, monthly climatologies of sea ice concentrations, and ocean masks.
The acronyms used in this document are listed in Table 11.
|AMSR-E||Advanced Microwave Scanning Radiometer - Earth Observing System|
|BBA||Bootstrap Basic Algorithm|
|DAAC||Distributed Active Archive Center|
|EASE-Grid||Equal-Area Scalable Earth Grid|
|EOS||Earth Observing System|
|GHCC||Global Hydrology and Climate Center|
|GR||Spectral Gradient Ratios|
|HDF-EOS||Hierarchical Data Format - Earth Observing System|
|MSFC||Marshall Space Flight Center|
|NASA||National Aeronautics and Space Administration|
|NSIDC||National Snow and Ice Data Center|
|NT2||Enhanced NASA Team Algorithm|
|PNG||Portable Network Graphics|
|RSS||Remote Sensing Systems|
|SCF||Science Computing Facility|
|SIPS||Science Investigator-led Processing System|
|SMMR||Scanning Multichannel Microwave Radiometer|
|SSM/I||Special Sensor Microwave/Imager|
|SMMIS||Special Sensor Microwave Imager/Sounder/td>|