Computer Modeling Laboratory 3

Written report due: 20 September

Spectral absorption of atmospheric gases and the transmission function.

Lecture 5, 6, 7

HITRAN database



High spectral resolution remote sensing has a wide range of applications in studying the atmosphere and surface. Examples of satellite high spectral resolution IR sensors include the Atmospheric Infrared Sounder (AIRS) and the Infrared Atmospheric Sounding Interferometer (IASI). AIRS has 2378 spectral bands in the IR spectral range from 650 to 2700 cm-1. The IASI sensor covers the spectral range from 645 to 2760 cm-1 at a constant spectral sampling interval of 0.25 cm-1. An example of a high spectral resolution ground-based IR sensor is the Atmospheric Emitted Radiance Interferometer (AERI) that covers the spectral range from 520 to 3300 cm-1 with a spectral resolution of 1 cm-1. Retrievals from this type of observations involve a modeling of radiances at very high spectral resolution (called line-by-line radiative transfer). This is necessary to correctly account for absorption/emission by individual lines of atmospheric gases. The spectroscopic information required for line-by-line modeling is provided by the HITRAN database.

To gain a better understanding of the nature of absorption of atmospheric gases and the spectral signature of the Earth's atmosphere, in this task you are asked to work with a few lines of water vapor. Then in task 2 you will analyze the spectral transmission of the atmosphere calculated with a line-by-line numerical model developed at ATMOSPHERIC AND ENVIRONMENTAL RESEARCH INC.

Table 1 gives a very small subset of data from HITRAN database in the vicinity of the 1.38 μm H2O band.

  1. Calculate and plot the spectral absorption coefficient kν as a function of wavenumber. Consider standard pressure, temperature, and the Lorentz profile.
  2. Pick any individual line from Table 1. Show how kν plot for this line will change if atmospheric pressure P will decrease at constant temperature. What spectral resolution will be required for a sensor to resolve this line at P = 200 mb? Consider the Lorentz line profile.
  3. Calculate the monochromatic transmittance Tν at ν = 7281.72912 cm-1 of a layer containing H2O only. Take a path length of u= 10 (atm cm).

Table 1. Subset of HITRAN line data for H2O (P =1013 mb; T=273 K)

Line center νo(1/cm) Line intensity
S (cm-1/(atm cm))
Line half-width
α (1/cm)
7280.31512 4.194E-03 0.0704
7280.47400 8.872E-04 0.0846
7281.08200 3.764E-02 0.0994
7281.72912 4.033E-03 0.0602


To run the line-by-line model, click on RUN LBLRTM.
NOTE: The standard atmospheric models (see Lecture 5 Notes, Figure 3.1) are built into the radiative transfer codes. Each standard atmospheric model is represented by the profile of temperature, pressure, air density and atmospheric gases. In this task the radiative transfer model uses a midlatitude summer standard atmosphere.

  1. For the spectral resolution of 1 cm-1, calculate and compare transmission of the 0-13 km atmospheric layer and 13-50 km atmospheric layer. Explain the differences.
  2. Based on the above results, predict how the transmission of the 0-50 km atmospheric layer should look like (i.e., similar to 0-13 km or 13-50 km in terms of spectral features). Run LBLRTM to get a right answer. Was your guess right? Why or why not?
  3. Now consider a finer spectral resolution. Will you expect to see more fine spectral features in the 0-13 km transmission or in the 13-50 km transmission? Explain why and then run LBLRTM to verify your predictions.