. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography 140 E. AUGSTEIN ET AL. 40 A 6. Cmb] 7no - 800 - 1000 I I I I 0 4. I I I I I 4 0 4 i i i—r-n—n— 4 8 12 16 [°K] Fig. 8. The difference of potential temperature {A9) on the left and equivalent potential temperature (A6e) on the right between the second and the first periods of ATEX. Difference between the second period without an inversion and the first period at 'Meteor' is presented by dashed lines. an increase of total static energy in all layers. F
. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography 140 E. AUGSTEIN ET AL. 40 A 6. Cmb] 7no - 800 - 1000 I I I I 0 4. I I I I I 4 0 4 i i i—r-n—n— 4 8 12 16 [°K] Fig. 8. The difference of potential temperature {A9) on the left and equivalent potential temperature (A6e) on the right between the second and the first periods of ATEX. Difference between the second period without an inversion and the first period at 'Meteor' is presented by dashed lines. an increase of total static energy in all layers. Figure 4 indicates that this change is nearly completely due to an increase of water vapor. Since evaporation at the sea surface was smaller in the second period than in the first period, the growth of water- vapor content and thus the static energy must be attributed mainly to the effect of horizontal convergence. The rather constant 0e-value with height in situations without an inversion supports the hypothesis that cumulus convection provides a strong upward transport of water vapor and by this reduces the 0e-minimum in the layer between 800 and 700 mb. THE VERTICAL WIND DISTRIBUTION As already noted by Riehl (1954), the atmospheric motion in undisturbed trades below the inversion is characterized by a high degree of wind steadiness S defined as |v| S = = x 100, |v| where |v| denotes the magnitude of the vector resultant wind and |v| the magnitude of the wind speed during the observational period. This steadiness has been supported by a number of observations. As an average for the layer between sea surface and the inversion, Riehl et al. (1951) derived a steadiness of about 90% for a three-month 1205. Please note that these images are extracted from scanned page images that may have been digitally enhanced for readability - coloration and appearance of these illustrations may not perfectly resemble the original Atlantic Oceanographic and Meteorological Lab
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