Global Monthly Vegetation CoverReprint of Original Document |
2. Information content of AVHRR measurements over land
The AVHRR is flown onboard the NOAA polar-orbiting satellites, the first of which was launched in 1978. These satellites are nearly sun-synchronous flying at the altitude of about 850 km. With each pass, data are collected in a cross-track scanning mode along a swath about 2700 km wide, covering a range of viewing angles up to 56o. Each 24 h, global coverage consisting of 14.1 orbits is achieved, with one look during the daytime and one during the night. Under normal conditions, NOAA operates two polar orbiters, one in the morning and one in the afternoon. The second-generation GVI contains data only from daytime orbits of the afternoon satellites NOAA-9 (April 1985-November 1988) and NOAA-11 (November 1988-September 1994). These satellites cross the equator between 1400 and 1700 local solar time, with the equator crossing time drifting to a later hour as the satellite ages (Price 1991). Satellite orbit drift results in a systematic change of illumination conditions and local time of observation -- one of the main sources of nonuniformity in multiannual satellite time series.
The AVHRR has five channels in the visible, near-infrared and thermal infrared (IR) regions of spectrum: channels 1 (0.58-0.68 12), 2 (0.73-1.0 12), 3 (3.6-3.9 12), 4 (10.3-11.3 12), and 5 (11.5-12.5 12). All these channels have been chosen within the relatively transparent atmospheric windows to allow observations of the surface. The first two channels measure solar-reflected light, whereas the land-atmosphere Planck emittance dominates in the thermal IR channels 4 and 5. Channel 3 is the most complicated case since both emitted and reflected solar components are comparable in this waveband. That was one of the reasons, in addition to frequent noisiness, for excluding channel 3 from the GVI dataset, and, therefore, analysis of its information content is not given here. A brief review below discusses the information content of AVHRR measurements over land in cloud free conditions. In studying the land surface, clouds should be excluded from the data since they obscure the signal from the surface in AVHRR wavebands.
a. Solar channels (channels 1 and 2)
There is, however, an ambiguity in what NDVI measures, which stems from the unresolved combination of the amount and state of the vegetation in the radiometer field of view (Curran 1980). Usually, these two quantities are correlated since development of vegetation is associated with the increase of both chlorophyll amount and area coverage by the vegetation. The NDVI signal, however, saturates before other measures of vegetation amount, such as leaf area index (LAI) (e.g. Carlson et al. 1990). In any event, because of strong seasonal and spatial signals, this "simple" index of vegetation has been used extensively by the research community for more than a decade. In addition to analyzing vegetation distribution, monitoring its seasonal and interannual variability, and relating it to ecological variables (e.g. Malingreau 1986; Cihlar et al. 1991), it has also been suggested that NDVI be used in numerical models (see review by Gutman (1990)) for estimating the ratio of actual to potential evapotranspiration (Mintz and Walker 1990), the ratio of soil heat flux to net radiation (Kustas et al. 1994), canopy resistance and photosynthesis (Sellers 1985), and green vegetation fraction and LAI (Carlson et al. 1990; Price 1990), [i.e. geophysical parameters identified by GEWEX (Global Energy and Water Cycle Experiment) as important for studying the land surface energy and water budget].
b. Thermal IR (channels 4 and 5)
The brightness temperatures in AVHRR channels 4 and 5, T4 and T5 (K), depend mainly upon the surface temperature, total-column atmospheric water vapor and surface-atmosphere temperature gradient, so that the former two parameters can be estimated using split-window techniques (see e.g. Dalu 1986; Kerr et al. 1992; Prata 1993).
c. Combining solar and thermal IR channels
A combination of NDVI and LST was proposed as a method for assessing the surface moisture
status and fractional vegetation cover over nonuniform land surface (Carlson et al. 1990; Price
1990; Nemani et al. 1993). The basic physical assumption is that the more heavily vegetated
surfaces are associated with greater evapotranspiration and hence should be cooler than the less
vegetated ones. Another reason that soil temperatures are higher than canopy foliage
temperatures is the greater efficiency of the leaves at shedding absorbed energy (Choudhury
1989). Friedl and Davis (1994) indicate that in "well-watered" conditions the proportion of the
soil background in the radiometer field of view, rather than evapotranspiration, explains the
observed NDVI-LST negative correlation.
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