GOES-R Proving Ground NSSL-WRF Simulated ABI Bands 8 -16

Click on band for time loop.

Click here to see GOES Imagery comparisons to WRF imagery

Band 8 (6.19 μm)

Band 9 (6.95 μm)

Band 10 (7.34 μm)

Band 11 (8.5 μm)

Band 12 (9.61 μm)

Band 13 (10.35 μm)

Band 14 (11.2 μm)

Band 15 (12.3 μm)

Band 16 (13.3 μm)

Band 2 (0.64 μm)

To see previous day's visible imagery, see wrfrun_YYYYMMDD directories at the bottom of the images archive.

NOTE: Images moved to archive at 03 UTC.
12-12UTC images start appearing around 06 UTC, complete to web by approximately 12 UTC.

For McIDAS AREA file access use the following: NSSLWRF/CONUS, SERVER: FLASH.SSEC.WISC.EDU

Simulated Radiance Details:
The radiance calculation for each ABI infrared channel involves several steps within the forward modeling system. First, CompactOPTRAN, which is part of the NOAA Community Radiative Transfer Model (CRTM), is used to compute gas optical depths for each model layer from the WRF-simulated temperature and water vapor mixing ratio profiles and climatological ozone data. Ice cloud absorption and scattering properties, such as extinction efficiency, single-scatter albedo, and full scattering phase function, obtained from Baum et al. (2006) are subsequently applied to each frozen hydrometeor species (i.e. ice, snow, and graupel) predicted by the microphysics parameterization scheme. A lookup table based on Lorenz-Mie calculations is used to assign the properties for the cloud water and rain water species. Visible cloud optical depths are calculated separately for the liquid and frozen hydrometeor species following the work of Han et al. (1995) and Heymsfield et al. (2003), respectively, and then converted into infrared cloud optical depths by scaling the visible optical depths by the ratio of the corresponding extinction efficiencies. The longer path length for zenith angles > 0 is accounted for by scaling the optical depth by the inverse of the cosine of the zenith angle. The surface emissivity over land was obtained from the Seeman et al. (2008) global emissivity data set, whereas the water surface emissivity was computed using the CRTM Infrared Sea Surface Emissivity Model. Finally, the simulated skin temperature and atmospheric temperature profiles along with the layer gas optical depths and cloud scattering properties, were input into the Successive Order of Interaction (SOI) forward radiative transfer model (Heidinger et al. 2006) to generate simulated TOA radiances for each ABI infrared band.