532 
man model(1968) was referred to as a basic model, whose op 
acity stems from the absorption and scattering processes due 
to molecules and aerosols, in addition to the ozone absorp 
tion. The stratified optical inhomogeneity of atmosphere co 
nsists of three layers,i.e., O-lkm, l-3km, and 3-50km,in El- 
terman' table averaged. The vertical optical inhomogeneity 
results in the level-dependent phase function in initial- 
value solutions of the scattering and transmission functions. 
The horizontal inhomogeneity of the diffuse reflectance on 
sea surface enables us to deal with the albedo of calm sea 
surface as the specular reflector. Then, extending the qua 
silinearization to the case of specular reflector (cf. Ueno 
19 81 ), the optical thickness of the atmosphere bounded by 
specular reflector was determined. On the other hand, in 
the case of diffuse reflector, the quasilinearization has 
been applied to the determination of the overall optical 
thickness of the atmosphere by several authors(cf.Bellman 
and Kalaba 19 6 5; Kagiwada, Kalaba , and Ueno 1975). 
Once when the direction of the incident solar rays at the 
transit time in the center of Kanazawa area has been provi 
ded, based on the atmospheric model under consideration, the 
ground albedo mapping can be performed, allowing for the 
weighted mean albedo ft(x,y) , which depends on the distribu 
tion of surface albedo around target and background. The 
last part of the computational algorithm in ground albedo 
mapping consists in the recurrence of the classification 
procedure given in the preceding section. The mean value 
and covariance for the ground albedo in eleven taining si 
tes are computed for uncorrected pixels and resampled pi 
xels via NN,BI and CC in band 4,5, and 6. Table 5 shows 
RCR of the mean ground albedos at uncorrected and resampled 
pixels in training sites in band 4,5, and 6. Finally, it is 
of interest to mention that in recent years, from the aspect 
of radiative transfer, the atmospheric scattering effects 
on on-board multispectral data have actively been discussed 
by several authors(cf.Chandrasekhar 1960;Ueno 1960;Bellman 
and Kalaba 19 65;Kagiwada,Kalaba and Ueno 1975;Odell and Wei 
nman 1975; Otterman and Fraser 1976;Ueno,Haba,Kawata,Kusaka, 
and Terashita 1978; Kawata,Haba,Kusaka,Terashita and Ueno 
19 78;Haba,Kawata, Kusaka, and Ueno 19 79 ;Dave 19 80;Otterman 
1981;Tanre,Herman,and Deschamps 1981;Kaufman and Fraser 1981 
and 19 82; Ueno 19 81 and 1982). 
Resampling Effects on Ground Albedo Napping 
In this section the distribution of diffuse reflectance in 
classification map is shown in ground albedo mapping. From 
the aspect of the mean value of ground albedo and its cova 
riance, the situation of resampling effects on ground albe 
do mapping seems to be similar in form to that on the clas 
sification map. In other words, the overall statistics of 
class occupancy are almost negligibly affected by the geo 
metric correction. However, the effects on a point-by-point 
level are noticeable for a few land use classes,i.e., waters 
and broad-leaved trees, in a manner similar to the classifi 
cation maps. Then, it seems that such a peculiarity of radi 
ometric fidelity in classification maps does not depend on 
the atmospheric effects on Landsat M3S data.