Ocean Currents in a Non-homogeneous Ocean 



481 



which is always permissible and integrating it between level ro(po.io) ^iid the level 

 ^liPx.v^ gives 



i\ = 



g 



./ 



idp. 



(XV.8) 



whereby p,„ is a mean density for the layer r^ — Zq. Denoting the tangents of the slope 

 angles of the isopycnals or isosteres drawn in a dynamic section with intervals A p 

 and Aa, respectively, by /, then equation (XV.8) can be transformed into the simple 

 relation 



S A p _ _ s Aa 



t\ = 



nf p, 



nf a, 



ZJ. 



(XV.9) 



The summation has to be taken over all the isopycnals or isosteres which cut a given 

 vertical line between levels Tq and z^ and n is the vertical exaggeration of the section. 

 Values of 7 can be read directly from the section using a transparent scale (Fig. 217). 

 If the isopycnals in a vertical section are plotted at intervals of 10~* and the isosteres at 

 intervals of 5 X 10""^ and if the vertical scale of the section is 1 :2500 and the horizontal 



Fig. 217. Tangent scale for the determination of the inclination (according to Werenskjold). 



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