48 EIGHTH PACIFIC SCIENCE CONGRESS 



of the same concentration as in ordinary Knudsen-Mohr's method. As 

 the absorption indicator, sodium fluorescenate is used. They are in- 

 tending to save both time and expenses without losing accuracy (in 

 press). 



K. Hishida applied Einstein's formula in order to find out the 

 direct influence of the chlorine in the sea water upon the turbidity, and 

 found that practically it does not affect the turbidity for the variation 

 of salinity usually found in the sea (OM, 3, 1951, 103). 



In 1952, Miyake completed the calculation of the saturated vapor 

 pressure of sea water for the range of temperature from— 2°C to 40 °C 

 at 0.1 °C interval and that of chlorinity from P/oo to 22°/oo at 

 P/oo interval (GM, 4, 1952, 95-118). 



Miyake and his collaborators have long been engaged in the study 

 of the formation of the bubbles in sea water. Miyake tried to find 

 out the possibility and allowable limit of an air bubble formation 

 in the sea and a formula was obtained for the saturation amount of 

 dissolved air in sea water. Since bubble formation in the sea water 

 depends on the pressure in situ, new concepts, the saturation amount 

 m situ and the saturation percentage m situ are introduced. Possible 

 causes for bubble formation were discussed and a graphical method is 

 given to compute the depth and the quantity of air to be evolved 

 (MGP, 2, 1951, 95-101). 



T. Abe, one of his collaborators, studied the thickness of the bub- 

 ble layer, that is, the layer in which the bubbles are formed in the 

 test tube by shaking it by hand. He found that this thickness increases 

 slightly with temperature and exponentially with CI, and that bubbles 

 are hardly seen in inorganic salt solutions (in press). 



K. Saruhashi, one of Miyake's collaborators, applied Conway's mi- 

 cro-diffusion method to the analysis of the total carbon dioxide in the 

 sea water. She deduced a theoretical relation between pH and the total 

 carbon dioxide in sea water (MGP, 3, 1953, 202-206). 



In the diurnal variation of dissolved oxygen in surface water, the 

 maximum occurs at about 4 P.M. and the minimum at 6 A.M. or so. 

 The difference between the maximum and minimum is dependent on 

 the solar radiation, temperature and the amount of phytoplankton. 

 Y. Sugiura obtained a formula giving the amount of dissolved oxygen, 

 in which the yield of oxygen were taken into account. The results of 

 calculation agreed fairly well with observations (in press). 



Miyake, Sugiura, and K. Kameda made observations of chemical 

 elements in the sea water around Hachijo Island in July, 1951, and in 

 December, 1952. A marked inverse correlation between chlorinity and 

 silicate content was noticed. Chemical analysis gave the result that the 



