OLR (1988) 35 (6) A. Physical Oceanography 515

88:3226 Quadfasel, Detlef and Jens Meincke, 1987. Note on

the thermal structure of the Greenland Sea gyres. Deep-Sea Res., 34(11A): 1883-1888.

Closely spaced temperature profile measurements during August 1986 reveal the existence of two cyclonic gyres, one in the northern Greenland Basin and one in the Boreas Basin. Their western bound- aries and the shear zone in between them are expected to be areas of winterly deep water for- mation. Inst. fur Meeresk., Univ. Hamburg, 2000 Hamburg 13, FRG.

A50. General hydrography (distribution of common oceanic properties)

88:3227 Kool, L.V. and L.I. Koprova, 1986. Heat balance of

the ocean surface in the energy-active zone of the Gulf Stream in winter. Izv. Atmos. Ocean Phys. (a translation of Fiz. Atmos. Okeana), 22(9):780- 782.

A detailed knowledge of the Gulf Stream's air-sea heat balance is important to understanding the current's role in North Atlantic climatology. Here, results of tropical, wintertime observations made aboard R/V Vityaz are described and analyzed. Inst. of Oceanol., Acad. of Sci., USSR. (fcs)

88:3228 Molchanov, S.A., L.I. Piterbarg, A.A. Ruzmaykin

and D.D. Sokolov, 1986. Variability of the ocean-surface temperature field. Dokl. Earth Sci. Sect. (a translation of Dokl. Akad. Nauk SSSR), 286(1-6):207-209.

Equations for annual variation in the SST field and the correlation function for the deviation (anoma- lous SST) field are derived and analyzed. The analysis relies upon integration of the true stochastic equation for temperature over random paths, a method devised by the authors to avoid classical closure methods, which preclude the possibility of sharp anomalies (alternations) in the temperature distribution. Univ. of Moscow, USSR. (emm)

AS0. Circulation

88:3229 Fujimoto, Minoru, 1987. On the flow types and

current stability in Tosa Bay [Japan] and adjacent seas . Umi to Sofa, 62(4):127-140. (In Japanese,

English abstract.) Nansei Reg. Fish. Res. Lab., Kochi, Japan.

88:3230 Gorbunov, A.Ye., 1986. Modeling the circulation of

the Black Sea. Izv. A tmos. Ocean Phys. (a translation of Fie. Atmos. Okeana), 22(9):775- 779. Inst. of Oceanol., Acad. of Sci., USSR.

88:3231 Griffin, D.A., J.H. Middleton and Lance Bode, 1987.

The tidal and longer-period circulation of Capri- cornia, southern Great Barrier Reef. Aust. J. mar. Freshwat. Res., 38(4):461-474. School of Math., Univ. of New South Wales, P.O. Box 1, Ken- sington, NSW 2033, Australia.

88:3232 Huang, R.X. and Kirk Bryan, 1987. A multilayer

model of the thermohaline and wind-driven ocean circulation. J. phys. Oceanogr., 17(1 !): 1909-1924.

The model includes a mixed layer at the surface specified by Eulerian coordinates, and three moving layers below, specified by quasi-Lagrangian, iso- pycnal coordinates. Initial tests have been carried out with a 22 × 22 horizontal grid mesh covering a subtropical-subpolar basin. Numerical results dem- onstrate strong interaction between wind-driven and thermally driven circulations, including outcropping of the lower isopycnal layers, a Gulf Stream-like interior boundary current, and convection which produces mode water and abyssal water. The model provides insight into the potential vorticity balance and its relation to the wind-driven and thermohaline components of the circulation not previously avail- able from Eulerian numerical models or analytical models based on the'assumption of an ideal fluid thermocline. WHOI, Woods Hole, MA 02543, USA.

88:3233 Killworth, P.D., 1987. A continuously stratified

nonlinear ventilated thermocline. J. phys. Oceanogr., 17(I I): 1925-1943.

Three exact (the flow is exactly geostrophic, hydro- static, and mass and buoyancy conserving) closed- form analytical solutions for the subtropical gyre are presented for the ideal fluid thermocline equations. Ekman pumping and density can be chosen as arbitrary functions at the surface. No flow is permitted through the ocean's eastern boundary, or through its bottom. The solutions are continuous extensions of existing layered models; all the problems reduce to linear homogeneous second- order differential equations when density replaces depth as the vertical coordinate. The importance of the bottom boundary for closing the problem is