. - Capture DES TEMPÉRATURES 100 200 3005 400 500 1928 1929 I930 1931 1932 1933 1934 1935 1937 1938 Fig. 8i. Prises annuelles moyennes de larves et de température moyenne à 1500 m. La dynamique est encore compliquée par l'existence de l'intermédiaire en croix chaud ils doivent traverser avant d'atteindre l'eau de surface. Où elle s'écoule directement au-dessous de la dérive de surface l'effet majeur de ce courant serait de détourner les larves provenant de leurs cours à l'Est, qui tend en général à les porter plus au sud. Plus le débit plus le détournement, impliquant parfois, il se
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. TEMPERATURE DEEP CATCH - 100 200 3005 4 00 500 1928 1929 I930 1931 1932 1933 1934 1935 1937 1938 Fig. 8i. Average annual catch of deep larvae and average temperature at 1500 m. The dynamics are further complicated by the existence of the warm crosswise intermediate current they must traverse before they reach the surface stream. Where it flows directly below the surface drift the major effect of this current would be to divert the deep larvae from their easterly course, tending in general to carry them farther south. The stronger the flow the greater the diversion, involving sometimes, it seems possible (p. 302), their transference from the Weddell to the East Wind zone. In general, however, its most likely effect would be to carry them away from a region where the surface drift was strong into another where it was weak, or vice versa, and so in the end again tend to advance or retard the eastward movement of the resultant surface population. As far as the bottom water is concerned, there does appear to be some measure of correlation between what might be described as the annual volume or activity of this current and the annual abundance of the deep larvae encountered during the spawning season. A graphical representation of this relationship is given in Fig. 81, which shows the average temperature at 1500 m. (taking that as 1 Although Fofonoff's (1956) work suggests that both temperature and sahnity of the water sinking into the bottom layer are likely to remain more or less constant, Deacon (1959) has pointed out that the volume of the transfer can vary, and that we should expect more sinking at the end of winter than at the end of summer. We should expect, too, as I have suggested, more sinking at the end of a severe winter than at the end of a mild one. Worthington (1959), discussing the formation of 'the 18° water' in the Sargasso Sea, notes that on the basis of existing measurements anomalously cold winters will produce a larger volume of this type of water
