. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography The transmlttance, T , it defined •• the ratio Hz/Haa. Thus, T repreaente the transmlttance of broad-band aolar lrradlance In the mixed layer without the effect of sur- face albedo. Measurement Results in 210 .197 .198 .164 171 .164 .154 .128 129 .125 .111 .097 080 .070 .061 .052 The transmlttance, T , defined this way clearly will depend on the solar zenith angle, because the path length of the direct aolar beam changes with zenith angle. This
. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography The transmlttance, T , it defined •• the ratio Hz/Haa. Thus, T repreaente the transmlttance of broad-band aolar lrradlance In the mixed layer without the effect of sur- face albedo. Measurement Results in 210 .197 .198 .164 171 .164 .154 .128 129 .125 .111 .097 080 .070 .061 .052 The transmlttance, T , defined this way clearly will depend on the solar zenith angle, because the path length of the direct aolar beam changes with zenith angle. This dependence Is shown In the data of Table for varloua depths. Thus, the transmittance profile will vary over certain limits during the day because of the changing zenith angle of the aun. TABLE 1 Transmlttance valuea as a function of solar zenith angle for varloua deptha SOLAR ZENITH ANGLE (a«g.) Depth («) T 5 10 15 30 We have used profiles on six daya during the Mixed Layer Experiment and one profile each from the Gulf Stream and Tongue of the Ocean In order to calculate a mean tranamlttance profile, shown In Figure 5. The solid curves with error bara show the profile for downward and upward lrradlance*. It can be aeen that the upward lrradlance Is between one and two ordera of magnitude leaa than the downward lrradlance for these particular depths. At much greater deptha, these two components become very nearly equal. Also In Figure 5 are the trana- mlttance curves aa given by Jerlov (1948). The I, II, and III curves Indicate the oceanic water profIlea, and the 1-5 curves Indicate the coaatal water profilea. Our curve for downward lrradlance haa somewhat lower transmlttance valuea than Jerlov's I curve. This may be due to the "emersion effect" of the instrument, which * The upward lrradlance waa obtained by in- verting the pyranometer and platform la dlacuaaed by H. Gordon in a companion paper In this publication. If we accept hla con- tenti
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