Oceanographic Literature Review (1989) 36 (6) The citations are those received in the editorial office during the period 1-31 March, 1989. Most are accompanied by a short annotation or abstract and, when obtainable, by the first author's address. The citations are classified under six main headings and about 130 sub-headings (see the table of contents). Subject and author indexes are published for the first three quarters of the year with an annual cumulation. See the preface for additional explanatory material. A. PHYSICAL OCEANOGRAPHY A10. Apparatus and methods 89:3137 Braning, Claus et al., 1988. Validation of a synthetic aperture radar ocean wave imaging theory by the Shuttle Imaging Radar-B experiment over the North Sea. J. geophys. Res., 93(C12):15,403- 15,425. European Centre for Med. Range Weather Forecasts, Reading, Berkshire, RG2 9AX, UK. 89:3138 Cadet, D.L. and Yarc6 Pafadnam, 1988. Marine data sets and the shift of Shilling routes. J. geophys. Res, 93(C 12): 15,639-15,641. Shipping routes of merchant ships have been changing since 1854, when the first observations over the ocean were organized. In certain areas where longitudinal and/or latitudinal gradients of surface parameters exist, spurious climatic signals due to the shift in shipping routes can appear even when space averaging is made over a large domain. This problem is documented, and two methods to correct the time series are presented. Fields resulting from an objective analysis of observations take into account the shift of shipping routes. Lab. de Meteorol. Dynam., CNRS, Ecole Polytech., 91128 Palaiseau Cedex, France. 89:3139 Frcnzen, C.L. and A.C. Warn-Varnas, 1988. Impli- cations of conservation equations for the deter- mination of absolute velocities. J. mar. Res., 46(4):701-714. The consequences of assuming that density is conserved in the problem of determining absolute velocities are investigated. Two questions are con- sidered: (1) the constraints that the density must satisfy to be compatible with the assumed geo- strophic and hydrostatic dynamics, and (2) whether and to what extent the indeterminancy in these dynamics is removed by this additional assumption. Dept. of Math., Southern Methodist Univ., Dallas, TX 75275, USA.
Transcript
Oceanographic Literature Review
(1989) 36 (6)
The citations are those received in the editorial office during the period 1-31 March, 1989. Most are accompanied by a short annotation or abstract and, when obtainable, by the first author's address. The citations are classified under six main headings and about 130 sub-headings (see the table of contents). Subject and author indexes are published for the first three quarters of the year with an annual cumulation. See the preface for additional explanatory material.
A. PHYSICAL OCEANOGRAPHY
A10. Apparatus and methods
89:3137 Braning, Claus et al., 1988. Validation of a synthetic
aperture radar ocean wave imaging theory by the Shuttle Imaging Radar-B experiment over the North Sea. J. geophys. Res., 93(C12):15,403- 15,425. European Centre for Med. Range Weather Forecasts, Reading, Berkshire, RG2 9AX, UK.
89:3138 Cadet, D.L. and Yarc6 Pafadnam, 1988. Marine data
sets and the shift of Shilling routes. J. geophys. Res, 93(C 12): 15,639-15,641.
Shipping routes of merchant ships have been changing since 1854, when the first observations over the ocean were organized. In certain areas where longitudinal and/or latitudinal gradients of surface parameters exist, spurious climatic signals due to the shift in shipping routes can appear even when space averaging is made over a large domain. This problem
is documented, and two methods to correct the time series are presented. Fields resulting from an objective analysis of observations take into account the shift of shipping routes. Lab. de Meteorol. Dynam., CNRS, Ecole Polytech., 91128 Palaiseau Cedex, France.
89:3139 Frcnzen, C.L. and A.C. Warn-Varnas, 1988. Impli-
cations of conservation equations for the deter- mination of absolute velocities. J. mar. Res., 46(4):701-714.
The consequences of assuming that density is conserved in the problem of determining absolute velocities are investigated. Two questions are con- sidered: (1) the constraints that the density must satisfy to be compatible with the assumed geo- strophic and hydrostatic dynamics, and (2) whether and to what extent the indeterminancy in these dynamics is removed by this additional assumption. Dept. of Math., Southern Methodist Univ., Dallas, TX 75275, USA.
476 A. Physical Oceanography OLR (1989) 36 (6)
89:3140 Kelly, K.A., 1988. Comment on 'Empirical orthogonal
function analysis of advanced very high resolution radiometer surface temperature patterns in Santa Barbara Channel' by G.S.E. Lagerloef and R.L. Bernstein. J. geophys. Res., 93(C12):15,753- 15,754. Dept. of Phys. Oceanogr., WHOI, Woods Hole, MA 02543, USA.
89:3141 Luchinin, A.G., 1987. Some properties of the back-
scattered signal in laser sounding of the upper ocean through a wavy surface. Izv. A tmos. Ocean Phys. (a translation of Fiz. Atmos. Okeana), 23(9):725-729. Inst. of Appl. Phys., Acad. of Sci., USSR.
Bennett and P.F. Cummins (reply), 1988. Dis- eussion of: 'Tracking fronts in solutions of the shallow-water equations.' J. geophys. Res., 93(C12): 15,749-15,751.
89:3143 Sanchez, B.V. and D.E. Cartwright, 1988. Tidal
estimation in the Pacific with application to SEASAT altimetry. Mar. Geod., 12(2):81-115.
Eigenfunctions of the velocity potential (Proudman functions) are calculated for the Pacific on a 6 ° × 6 ° grid. Tidal syntheses are derived from normal mode computation utilizing the frictionless dynamic equa- tions as well as by least-squares fitting of the Proudman functions to Schwiderski's (1983) tide gauge data; Proudman function fit is better for all cases. Processing techniques for fitting the Proud- man functions to Seasat altimetry data are de- scribed. NASA Goddard Space Flight Center, Geodynamics Branch, Greenbelt, MD 20771, USA. (sir)
89:3144 Varkey, M.J. and J.S. Sastry, 1988. Reference depth
for geostrophic computation--a new method. Indian J. mar. Sci., 17(2):91-93.
A new method based on the vertical profiles of mean and variance of the differences of mean specific volume anomaly for different layers of the water column for various pairs of stations is presented. The results agree well with published information for a region in the Indian Ocean. Natl. Inst. of Oceanogr., Dona Paula, Goa 403 004, India.
(May 1978--May 1980).1 Annls hydrogr., (5)15(762):43-186. (In French.)
The first two sections of this report outline the scope of the Pacific oceanographic mission including the organizational framework and the hydrographic methods used. The third section contains nine chapters chronicling surveys of different regions around New Caledonia and French Polynesia. These accounts are followed by a series of technical appendices on aspects of the hydrographic envi- ronment around corals, side-scan sonar application, tides and currents, and magnetic variation. (gsb)
89:3146 Hanawa, Kimio and Izumi Hoshino, 1988. Tem-
perature structure and mixed layer in the Kuro- shio region over the lzu Ridge. J. mar. Res., 46(4):683-700. Dept. of Geophys., Tohoku Univ., Sendai 980, Japan.
89:3147 Hanawa, Kimio et al., 1988. Surface thermal con-
ditions in the western North Pacific during the ENSO events. J. met. Soc. Japan, (Ser. II)66(3): 445-456.
Composite analyses of the SST anomaly fields were performed over the western North Pacific, and for the mixed layer in the Kuroshio current region at sections along the 137°E line and a line over the Izu Ridge. In the ENSO year winter, a well-ordered positive SST anomaly appears in a wide zonal band along the 30°N line, extending from the Asian coast to near 170°E. The distribution of SST anomalies in the ENSO+ 1 year winter is quite similar to that in the ENSO year winter with its sign reversed. During the ENSO year winter, the mixed layer in the Kuroshio region south of Japan was thinner and warmer. One possible cause is the strength of the east Asian winter monsoon, which is relatively weaker in the ENSO year winter. Dept. of Geophys., Tohoku Univ., Sendai 980, Japan.
89:3148 Iwasaka, Naoto, Kimio Hanawa and Yoshiaki Toba,
1988. Partition of the North Pacific Ocean based on similarity in temporal variations of the SST anomaly. J. met. Soc. Japan, (Ser. II)66(3):433- 443.
A cluster analysis with respect to similarities in their temporal variation is made of the SST anomaly field. A subdomain of coherent SST anomaly fluctuations is extracted for the middle latitude part of the
OLR (1989) 36 (6) A. Physical Oceanography 477
western North Pacific, although previous studies did not extract such a subdomain. In all, four major subdomains are found: the aforementioned, the western tropical subdomain, the central North Pacific, and the eastern boundary region. Oceanic and atmospheric conditions characterizing such subdomains are discussed. Dept. of Geophys., Tohoku Univ., Sendal 980, Japan.
89:3149 Rahm, Lars, 1988. A note on some hydrographic
properties of the Eastern Gotland Basin. Beitr. Meeresk., 58:47-58.
AS0. General hydrography (distribution of c o m m o n oceanic proper t ies)
89:3150 Leach, Harry et al., 1987. SEA ROVER Data Report
II. North Atlantic summer 1983: [structures in the seasonal boundary layer]. NOA '83. Ber. Inst. Meeresk. Christian-A lbrechts-Univ., 175:91pp.
Part of a long-term seasonal boundary layer research program, this experiment was conducted in the North Atlantic region bounded by the Azores, Greenland, and Great Britain. Data reported here concern primarily (1) large-scale variability of the seasonal boundary layer between the Azores and 55°N, and (2) 3-D mesoscale structure of the Polar Front near the Gibbs Fracture Zone. Copies are available from Abt. Region. Ozeanogr., Inst. fur Meeresk. an der Univ. Kid, Dusternbrooker Weg 20, D 2300 Kiel 1, FRG.
89:3151 Semenov, E.V., 1988. [Some aspects of plannlog and
interpreting hydrological observations in the energy active zone of the ocean.] Beitr. Meeresk., 58:59-64. (In German, English abstract.) Schir- schow Inst. for Oceanol., Krasikova 23, 117218 Moscow, USSR.
AS0. Circulation
89:3152 Craig, P.D., 1988. Space and time scales in shelf
A time-dependent analytic solution is used to assess common numerical techniques used in continental shelf modelling. The analytic model describes a well-mixed, constant-eddy-viscosity ocean, forced
from rest by a unidirectional wind stress sinusoidal in both space and time, allowing both a space and a time scale to be imposed on the system. There are also natural time scales (wave periods) and natural space scales (depth of wind influence). To avoid aliased solutions, motion at these scales must be either resolved or removed in numerical modelling. Numerical results are calculated using both explicit and implicit time-stepping for the depth-averaged velocity, and an eigenfunction representation and a Crank-Nicholson scheme for the depth-dependent velocity. CSIRO Div. of Oceanogr., G.P.O. Box 1538, Hobart, Tas. 7001, Australia.
89:3153 Doney, S.C. and W.J. Jenkins, 1988. The effect of
boundary conditions on tracer estimates of ther- mocline ventilation rates. J. nor. Res., 46(4):947- 965.
Using a simple box mixing model, we show that ventilation rate estimates obtained from tracer box models may be significantly smaller than fluid replacement rates depending on the surface bound- ary condition for a given tracer. Ventilation rates for rapidly exchanging tracers (e.g. 3He) are close to the fluid ventilation rate while tracers with limited surface exchange (e.g. tritium) ventilate more slowly. For box mixing models, the ratio of ventilation rates for limited surface exchange tracers to rapidly exchanging tracers approaches the ratio of summer to winter mixed layer depths. Further, the distri- bution of rapidly equilibrating tracers more accu- rately tracks climatological fluctuations in water mass formation rates. Box models using limited surface exchange tracers can underpredict oxygen utilization rates by up to 3 times due to differences in tracer boundary conditions, while a tracer like 3He may overestimate by 10-20%. Chem. Dept., WHOI, Woods Hole, MA 02543, USA.
89:3154 Greenberg, D.A. and B.D. Petrie, 1988. The mean
barotropic circulation on the Newfoundland shelf and slope. J. geophys. Res., 93(C12):15,541- 15,550.
Results of a numerical model calculation of the barotropic mean circulation in the Grand Banks region show qualitative and some quantitative agreement with available current data. The model accounts for the general flow of the Labrador Current along the shelf edge, its splitting into two branches north of Flemish Pass and south of Cabot Strait, and the circulation over the Grand Banks, but it underestimates the strength of the clockwise circulation over Flemish Cap and the width of the Labrador Current. Neglect of the influence of the
478 A. Physical Oceanography OLR (1989) 36 (6)
Gulf Stream and North Atlantic Current may give rise to local discrepancies between observed and modeled flows. Bedford Inst. of Oceanogr., Dart- mouth, NS B2Y 4A2, Canada.
89:3155 Lass, H.U., 1988. A theoretical study of the barotropic
water exchange between the North Sea and the Baltic and the sea level variations of the Baltic. Beitr. Meeresk., 58:19-33.
Model parameters include the fresh water balance of the Baltic, water level of the Kattegat, and both the wind field and the pressure over the Baltic. With typical values, the water exchange response is stationary for a fresh water surplus and transient for both Kattegat water level and meteorological forcing over the Baltic. Characteristic system response time is about 10 days. System responses to step functions, pulses, and sinusoidal functions, as well as the necessary conditions for a barotropic inflow to the Baltic, are evaluated. Inst. fur Meeresk. Akad. der Wissenschaften der DDR, DDR-2530 Rostock Warnemunde, DRG.
89:3156 Marshall, J.C., A.J.G. Nurser and R. Brugge, 1988.
On the time-averaged flow of quasi-geostrophic wind-driven gyres. J. geophys. Res., 93(C12): 15,427-15,436.
The flow of a 3-layer eddy-resolving quasi-geo- strophic model is considered in the light of two analytical models in which the vertical structure of the gyre is set by assuming that potential vorticity is uniform beneath layers exposed to forcing. The first (Young and Rhines, 1982), supposes that the depth- integrated meridional transport is set by the imposed wind-stress curl. In the baroclinic Fofonoff gyres of the second (Marshall and Nurser, 1986, 1988), inertial aspects of the flow are emphasized without imposing a Sverdrup constraint. The mean fields lie between the two extremes represented by these analytical solutions. In the interior of the gyre away from inertial boundary currents and jets, the Sver- drup constraint is obeyed, and the mean flows resemble the Young and Rhines solution. However, the essential character of the overspun recirculation, including the weakly depth-dependent nature of the currents in its return flow, seem to be well captured in the inertial limit considered by Marshall and Nurser. Dept. of Phys., Imperial Coll., Prince Consort Rd., London SW7 2BZ, UK.
89:3157 Semtner, A.J. Jr. and R.M. Chervin, 1988. A
simulation of the global ocean circulation with resolved eddies. J. geophys. Res., 93(C12): 15,502-15,522.
A multilevel primitive-equation model has been constructed for the purpose of simulating ocean circulation on modern supercomputing architec- tures. The model is designed to take advantage of faster clock speeds, increased numbers of processors, and enlarged memories of machines expected to be available over the next decade. The model allows global eddy-resolving simulations to be conducted in support of the World Ocean Circulation Experiment. Furthermore, global ocean modeling is essential for proper representation of the full range of oceanic and climatic phenomena. The first such global eddy-resolving ocean calculation is reported here. Naval Postgrad. Sch., Monterey, CA 93943, USA.
89:3158 Simmons, R.C. et al., 1988. Verification of a numer-
ical ocean model of the Arabian Sea. J. geophys. Res., 93(C12): 15,437-15,453.
A case study evaluating the predictive capability of an upper layer circulation model of the n,wthwest Indian Ocean is presented. The model is a nonlinear, reduced gravity model incorporating realistic bound- ary geometry and is forced by observed winds. Ship wind observations are converted to wind stress for model forcing by a procedure developed by Legler and Navon (1988). Given accurate wind informa- tion, the model appears highly effective in dynam- ically active regions and demonstrates potential as a useful prognostic tool for evaluation of the Arabian Sea when real time winds become available. NAVWEST Ocean Center, Box 113, Pearl Harbor, HI 96860, USA.
89:3159 Yefimov, V.V. and A.B. Polonskiy, 1988. Circulation
in the northwestern tropical Atlantic and merid- ional heat transport. Dokl. Earth Sci. Sect. (a translation of Dokl. Akad. Nauk SSSR), 293(1- 6):213-215.
The main object of this study was to elucidate the transport of heat from the tropical Atlantic to higher latitudes. A series of surveys done in 1984-1985 indicates that 'there is no meridional heat transport by currents in the western tropical zone.' Thus, elucidating the physics still remains a top priority. 'The most probable mechanism is simple wind currents in the upper ocean.' Mar. Hydrophys. Inst., UkSSR, Sevastopol, USSR. (fcs)
OLR (1989) 36 (6) A. Physical Oceanography 479
A90. Currents
89:3160 Birr, H.-D., 1988. [Currents of the Strelasound Strait
(Baltic Sea).] Beitr. Meeresk, 58:3-8. (In Ger- man, English abstract.) Sektion Geogr., Ernst Moritz Arndt Univ., F.-L. Jahn Sir. 16, DDR- 2200, Greifswald, DRG.
89:3161 Boudra, D.B., Rainer Bleck and Friedrich Schott,
1988. A numerical model of instabilities in the Florida Current. J. mar. Res., 46(4):715-751.
An isopycnic coordinate numerical model is con- figured as an infinitely long channel with the width and bottom topography of the Straits of Florida at 27°N to investigate the possibility that Florida Current meanders are due to dynamical instabilities. The current is found to be baroclinically unstable in the classical sense to perturbations with wavelengths greater than ~85 km, and the meanders which develop eventually dominate the channel flow pattern. When the topography is included, the instability is greatly reduced, but the primary source of perturbation energy remains the baroclinic one. RSMAS, Univ. of Miami, FL 33149, USA.
89:3162 Coachman, L.K. and K. Aagaard, 1988. Transports
through Bering Strait: annual and interannual variability. J. geophys. Res., 93(C12):15,535- 15,539.
We find (1) a long-term mean transport of 0.8 Sv, (2) an annual transport cycle of amplitude 0.6 Sv, with the maximum in June, minimum in February, and a secondary maximum in January, and (3) an inter- annual variability marked by a number of low-flow years in the past two decades, including three of the four lowest-transport winter periods during this century. An anomalously strong and persistent northerly flow, during a 2-month period in which the current/wind correlation breaks down, occurred during a prolonged period with southerly winds, indicating an asymmetry in the dynamical response of the Bering Strait flow to major changes in wind direction. School of Oceanogr., Univ. of Washing- ton, Seattle, WA 98195, USA.
89:3163 Culver, S.J., C.A. Brunner and C.A. Nittrouer, 1988.
Observations of a fast burst of the Deep Western Boundary Undercurrent and sediment transport in South Wilmington Canyon from DSRV Alvin. Geo-Marine Letts, 8(3): 159-165.
On October 3 and 4, 1986, a strong current was
encountered at 2300 m in South Wilmington Can- yon. The current, estimated at 1 knot, transported surficial sediment and constructed and modified bedforms. The observed current was probably a burst of fast flow in a region of slow average currents in the Deep Western Boundary Undercurrent. Such episodic events may have a greater influence on the stratigraphic record than the temporally-longer more tranquil flow conditions. Dept. of Geol. Sci., Old Dominion Univ., Norfolk, VA 23529-0496, USA.
89:3164 Garvine, R.W. et al., 1988. The morphology of
shelfbreak eddies. J. geophys. Res., 93(C12): 15,593-15,607.
Eddylike features were always present at the shelf- break front in the Middle Atlantic Bight throughout the 15-day period of observations. Hydrographic features in across-shelf transects that appeared to represent the detached parcels of shelf water often reported in the literature were, in fact, part of the 3-D structure of shelfbreak eddies. Adequate along- shelf resolution showed that no detached parcels were present. The two prominent features of the eddy groups were plumes of lighter shelf water that protruded into slope water, curling 'backward' opposite the direction of mean shelf flow, and neighboring cyclones with warmer, saltier slope water in their cores, partly or wholly encircled by the plumes. The plumes have the potential for producing vigorous across-front exchanges of heat, salt, and nutrients. Coll. of Mar. Studies, Univ. of Delaware, Newark, DE 19716, USA.
89:3165 Huyer, Adriana et al., 1988. Currents off south-
eastern Australia: results from the Australian Coastal Experiment. Aust. J. mar. Freshwat. Res., 39(3):245-288.
The Australian Coastal Experiment was conducted off the east coast of New South Wales between September 1983 and March 1984. The experiment was conducted with arrays of current meters span- ning the continental margin at three latitudes (37.5 °, 34.5 °, and 33.0°S), additional shelf moorings at 29 ° and 42°S, coastal wind and sea-level measurements, monthly CTD/XBT surveys, and two satellite- tracked buoys. Observations and analyses are re- ported. Coil. of Oceanogr., Oregon State Univ., Corvallis, OR 97331, USA.
89:3166 MUller, T.J., 1987. Analysis of low frequency current
fluctuations in the northeast Atlantic Ocean. Bet. Inst. Meeresk. Christian-Albrechts-Univ., 170: 135pp. (In German, English abstract.)
480 A. Physical Oceanography OLR (1989) 36 (6)
Eulerian current measurements were made in the North Atlantic east of 27°W between 28 ° and 42°N. Most data are from the main thermocline and cover periods exceeding 200 days. Together the barotropic and first baroclinic modes account for >80% of energy fluctuations, with the barotropic mode alone contributing 31-72%. Higher modes are energetically unimportant. Abt. Meeresphysik, Inst. fur Meere- skunde, Univ. Kiel, Dusternbrooker Weg 20, 2300 Kiel, FRG.
89:3167 Sugimoto, Takashige, Shingo Kimura and Kuniaki
Miyaji, 1988. Meander of the Kuroshio front and current variability in the East China Sea. J. oceanogr. Soc. Japan, 44(3): 125-135.
The current over the East China Sea slope fluctuates over an 11-14 day period. When the Kuroshio front approaches the shelf-break and the crest of the meander encounters the moored current meter, the current direction moves toward the downstream direction of the Kuroshio, and water temperature increases. However, when the trough of the meander crosses the mooring site, the current direction changes in the upstream direction of the Kuroshio, and water temperature decreases. Ocean Res. Inst., Univ. of Tokyo, 1-15-1, Minamidai, Nakano-ku, Tokyo 164, Japan.
89:3168 Vukovich, F.M., 1988. Loop Current boundary
variations. J. geophys. Res., 93(C12):15,585- 15,591.
The period between separation of warm rings from the Loop Current was highly variable, but averaged ~10.9 months (range 6-17 mos.). For the data set used, ring separations occurred most often in the winter. Cold perturbations were most pronounced along the northern and eastern portions of the Loop Current boundary, less pronounced south of 27°N along the western boundary. The large effects along the eastern boundary of the Loop Current were thought to be associated with the movement of the intense perturbations that are initially found along the northwestern portions of the boundary. Office of Geosci. Prog., Res. Triangle Inst., P.O. Box 12194, Research Triangle Park, NC 27709, USA.
All0. Water masses and fronts
89:3169 [Irosin, H.-J. et al., 1988. [Mesoscale structures in the
southeastern Baltic Sea in May 1995.] Beitr.
Meeresk., 58:9-18. (In German, English ab- stract.) Inst. fur Meeresk., Akad. der Wissen- schaften der DDR, DDR-2530 Rostock Warnemunde, DRG.
89:3170 Sekine, Yoshihiko and Yasushi Matsuda, 1987.
Observation on surface mixed layer around the Tosa-Bae, the bump off Shikoku south of Japan in November 1985. Umi to Sora, 63(1):1-14. (In Japanese, English abstract.) Natl. Defense Acad., Yokosuka, Japan.
89:3171 Sun, Huili et al., 1987. A preliminary study on
uranium distribution and its isotopic composition in Zhujiang estuarine water. Tropic Oceanol., 6(4):55-60. (In Chinese, English abstract.) South China Sea Inst. of Oceanol., Acad. Sinica, People's Republic of China.
89:3172 Viehoff, T. and J. Fischer, 1988. Satellite sea surface
temperature at the North Atlantic Polar Front related to high-resolution towed conductivity- temperature-depth data. J. geophys. Res., 93(C 12): ! 5,551-15,560.
The average SST differences of the independently calibrated CTD and satellite data were less than 0.2 K for those mixed-layer CTD data measured within I day of the satellite images. A strong decline of the temporal cross correlations between mixed-layer temperatures and SST was observed shortly after the transition of an atmospheric front. A comparison of the SST with the isopycnic temperature distribution revealed the longer persistence of the structures in the stably stratified layers just beneath the mixed layer. Alfred Wegener Inst. fur Polar- und Meeres- forschung, Postfach 120161, 2850 Bremerhaven, FRG.
AI20. Convergences, divergences, up- welling
89:3173 Jury, M.R., 1988. Case studies of the response and
spatial distribution of wind-driven upwelling off the coast of Mrica: 29-34 ° south. Continent. Shelf Res., 8(11): 1257-1271.
Differing scales, intensities and response lags in wind-driven coastal upwelling were documented through the analysis of selected aerial survey data. The upwelling centered at 30°S was of greater spatial
OLR (1989) 36 (6) A. Physical Oceanography 481
extent than the upwelling plumes associated with the capes at 33 and 34°S. Variations in the depth of the atmospheric boundary layer affected the structure of equatorward winds and upwelling activity off the capes. When the air temperature inversion was relatively low, wind stress was enhanced seaward of the capes, while equatorward, a wind shadow reduced offshore Ekman transport and upwelling. Oceanogr. Dept., Univ. of Cape Town, Rondebosch, 7700, South Africa.
89:3174 Legeckis, Richard, 1988. Upwelling off the gulfs of
Panama and Papngayo in the tropical Pacific during March 1985. J. geophys. Res., 93(C12): 15,485-15,489.
Unusually persistent upwelling was observed SW of the gulfs of Panama and Papagayo. The SST was depressed by 6 ° to 10°C relative to the surrounding waters. The cooler waters off Panama extended for over 1000 km and reached the Galapagos Islands. The northern SST front off Panama was wavelike in appearance, and long waves of 600-km length moved southwestward at a phase speed of about 30 km/d. The SST fronts off the Gulf of Papagayo remained relatively stationary, with a large area of colder water centered at 88°W and 10°N. During these events, the upwelling off the Gulf of Tehuantepec was relatively weak. NOAA Natl. Environ. Satellite Data Info. Service, Suitland Professional Center, Washington, DC 20233, USA.
AIS0. Tides and sea level
89:3175 Biollay, Yves and Julien Kravtchenko, 1988. [Ana-
lytical study of a model of coastal tides with the aid of multiple characteristics.I [Third part (B). Extension of the theory of envelopes---study of some ordered solutions of (E).] Annls hydrogr., (5)15(762):5-24. (In French, English abstract.) Ecole Polytech. Fed., CH-1007 Lausanne, Swit- zerland.
89:3176 Demchenko, P.F. and Ye.Yu. Polezhayeva, 1987.
The role of thermal expansion in raising the global sea level. Izv. Atmos. Ocean Phys. (a translation of Fiz. Atmos. Okeana), 23(9):700- 706.
Simple one-dimensional models of the thermal behavior of the oceans are used to determine the change in sea level resulting from thermal expansion. Estimates of the change in sea level for a specified
linear surface temperature trend are presented. Use of a diffusive model to calculate the change in sea level produces satisfactory agrement with obser- vations, but the results obtained with allowance for large-scale upwelling are considerably below the observed values. Correction for possible changes in the speed of large-scale upwelling (reconciled with the warming of intermediate waters) brings the predicted sea level considerably closer to the empir- ical figures. Inst. of Atmos. Phys., Acad. of Sci., USSR.
89:3177 Lanfredi, N.W., E.E. D'Onofrio and C.A. Mazio,
1988. Variations of the mean sea level in the southwest Atlantic Ocean. Continent. Shelf Res., 8(1 l): 1211-1220.
An analysis of 64 years of hourly tide heights at the most reliable Argentine oceanic station has been made, using a symmetric low-pass filter based on the Kaiser-Bessel window, which permits elimination of periodic components (of 8.8 and 19 years). Con- voluting the data with a synthesized filter, the spectrum has been obtained using the Fast Fourier Transform. The long-term trend has been calculated at 16.09 cm/100 years, compatible with calculations made recently for variations on a global scale. Com. de Invest. Cient. de la Prov. de Buenos Aires, Fac. de Cienc. Nat., U.N.L.P. Casilla de Correo 45, 1900 La Plata, Argentina.
89:3178 Lee, S.H. and Kuh Kim, 1988. Variations of the
diurnal tides around Jeju-Do [Korea]. J. oceanol. Soc. Korea, 23(2):62-69. Dept. of Oceanogr., Seoul Natl. Univ., Seoui 151-742, Korea.
AI60. Waves, oscillations
89:3179 Bontozoglou, V. and T.J. Hanratty, 1988. Effects of
finite depth and current velocity on large ampli- tude Kelvin-Helmholtz waves. J. Fluid Mech., 196:187-204.
Saffman and Yuen (1982) did work on finite- amplitude interfacial waves between two fluids in relative motion that resulted in identifying a 'geo- metrical limit" reached as the wave height increased to a critical value, and a 'dynamical limit' reached when the relative current velocity increased to a critical value. That work is extended to consider the effects of finite fluid depth and current velocity together on wave behavior. A numerical method was developed to handle fluids of arbitrary uniform
482 A. Physical Oceanography OLR (1989) 36 (6)
depth and any density ratio, and the geometrical and dynamical limits of the more varied system are examined with interesting results. Dept. of Chem. Engng, Univ. of Illinois, Urbana, IL 61801, USA. (fcs)
89:3180 Brueckner, K.A. and B.J. West, 1988. Vindication of
mode-coupled descriptions of multiple-scale water wave fields. J. Fluid Mech., 196:585-592.
The modal description of deep-water waves on the sea surface (Watson & West, 1975) is independent of any reference surface around which expansions of the velocity potential and the surface velocity are done. We demonstrate by direct construction that the interaction between long and short waves does not lead to divergent terms in the equations of motion when this formalism is used. Dept. of Phys., Univ. of Calif., La Jolla, CA 92093, USA.
89:3181 Eriksen, C.C. and J.G. Richman, 1988. An estimate
of equatorial wave energy flux at 9- to 90-day periods in the central Pacific [144°-148°W]. J. geophys. Res., 93(C12): 15,455-15,466.
Deep fluctuations in current along the equator in the central Pacific are dominated by coherent structures which correspond closely to narrow-band (in wave number) propagating equatorial waves. Observations indicate that energy flux is westward and downward in long first meridional mode Rossby waves at periods 45 days and longer and eastward and downward in short first meridional mode Rossby waves and Rossby-gravity waves at periods 30 days and shorter. A local minimum in energy flux occurs at periods corresponding to a maximum in upper ocean meridional current energy contributed by tropical instability waves. Total vertical flux across the 9- to 90-day period range is 2.5 kW/m. Sch. of Oceanogr., Univ. of Washington, Seattle, WA 98195, USA.
89:3182 Heaps, N.S. et al., 1988. Modelling of storm-driven
shelf waves north of Scotland. I. Idealized models. Continent. Shelf Res., 8(11): 1187-1210.
Storm-driven currents observed over the Scottish continental shelf were described in 1987 as conti- nental shelf-wave responses. This suggestion is investigated here using semi-analytic and numerical models of a straight continental shelf. Grid reso- lution, boundary conditions, truncations and dif- ferences of depth profile are considered; dispersion curves and wave forms are derived. These forms are closely matched by the fully numerical model forced
by specified elevations at one end. Localized forcing of short duration gives currents of the type observed, being rotary (clockwise) with roughly 22 h period. More extensive alongshelf forcing gives predomi- nantly alongshelf currents with a strength tending to follow the forcing, the second form of observed response. Frictional effects are considered. Proud- man Oceanogr. Lab., Bidston Observ., Birkenhead, Wirral, Merseyside L43 7RA, UK.
89:3183 Iguchi, Toshio et al., 1988. Ocean wave spectra
derived from Shuttle Imaging Radar-B imagery and surface measurements. J. geophys. Res., 93(C12): 15,367-15,373.
Wave spectra derived from SIR-B imagery off the coast of Japan were compared with simultaneous wave buoy observations. Waves at the time of flight were nearly perpendicular to the SAR flight direc- tion and were composed of two major systems: a swell of about 200-m wavelength and wind waves with 70-m wavelength. Both the swell and wind wave peaks were identifiable in the SAR image spectrum after stationary response correction. Peak frequen- cies derived from SIR-B images and from the wave gauge agreed satisfactorily; however, the relative magnitudes of the peaks are not in accordance with the surface measurements. Possible reasons for the disagreement are discussed. Okinawa Radio Wave Observ., Commun. Res. Lab., Min. of Posts and Telecommun., 829-3 Daigusukubaru, Kuba, Naka- gusukuson, Okinawa, 901-24, Japan.
89:3184 Irvine, D.E. and D.G. Titley, 1988. Ocean wave
directional spectra and wave-current interaction in the Agulhas from the Shuttle lma~ng Radar-B synthetic aperture radar. J. geophys. Res., 93(C12): 15,389-15,401.
SIR-B synthetic aperture radar ocean-wave spectra for a 200-km pass crossing the Agulhas Current off the coast of Africa are analyzed. A significant enhancement of one spectral peak along the north- ern edge of the current is attributed both to amplification of the waves by refraction-dominated wave-current interaction and to transient specular backscatter contributions spatially correlated to the waves. St. Johns Coll., College Ave., Annapolis, MD 21404, USA.
89:3155 Linde, Bogumil, Stanislaw Pogorzelski and Antoni
Sliwifiski, 1986. The effect of thickness of crude oil layers on the attenuation of the surface capillary wave. Oceanologia, Warsz., 24:41-46.
OLR (I 989) 36 (6) A. Physical Oceanography 483
The absorption of a capillary wave with a frequency of 30 Hz propagated on a water surface covered with crude oil derivatives was investigated. The rela- tionship of the absorption coefficient value and oil layer thickness was studied; experimentally-deter- mined a values are greater than those predicted by Stokes' theory. Applicability of the Stokes' equation was considered on the basis of physical properties characterizing the investigated petroleum deriva- tives. Inst. of Exp. Phys., Univ. of Gdansk, Poland.
89:3186 Mazova, R.Kh., N.N. Osipenko and Ye.N. Pelinov-
skiy, 1987. Effect of nonlinearity on the runup characteristics of long waves. Izv. Atmos. Ocean Phys. (a translation of Fiz. Atmos. Okeana), 23(9):707-710.
An analog of the Riemann equations is used to calculate runup characteristics of long waves on a planar beach. Time dependence of the flow speed and the climbing height of the wave tongue are found, and the mean submergence level and the wave breaking parameter are determined for an initial disturbance of arbitrary form. As nonlinearity increases, the time required to climb the beach is considerably greater than the downflow time. Inst. of Appl. Phys., Acad. of Sci., USSR.
89:3187 Monaldo, F.M. and D.R. Lyzenga, 1988. Compar-
ison of Shuttle Imaging Radar-B ocean wave image spectra with linear model predictions based on aircraft measurements. J. geophys. Res., 93(C12): 15,374-15,388.
The 2-D wave spectrum was measured by both a radar ocean wave spectrometer and a surface contour radar aboard the aircraft. In this paper we compare SAR image intensity variance spectra with these independent measures of ocean wave spectra to verify previously proposed models of the rela- tionship between such SAR image spectra and ocean wave spectra. Results illustrate both the functional relationship and the limitations imposed on the imaging of short-wavelength, azimuth-traveling waves. APL, Johns Hopkins Univ., Johns Hopkins Rd., Laurel, MD 20707, USA.
89:3188 Nielsen, Peter, 1988. Wave setup: a field study. J.
geophys. Res., 93(C12):15,643-15,652.
A new, efficient method for obtaining field meas- urements of surf zone mean water levels applies manometer tubes rather than the traditional pressure transducers, and hence makes it unnecessary to survey the vertical positions of the 'sensors.' A
substantial data base is obtained which gives clear, general indications of where previous wave setup models need to be amended. It is clear from the data that while traditional setup models work reasonably well seaward of the still water line, the most landward part of the mean water surface (on fairly steep beaches at least) requires radically different models. Coast and Rivers Branch, Public Works Dept., 140 Phillip St., Sydney, 2000 NSW, Australia.
89:3189 Oh, I.S. and Y.R. Lee, 1988. A capacitance wavestaff
for use near the surf zone. J. oceanol. Soc. Korea, 23(2):53-61. (In Korean, English abstract.) Dept. of Oceanogr., Seoul Natl. Univ., Seoul 151-742, Korea.
89:3190 Pogorzelski, Stanislaw, Bogumil Linde and Antoni
Sliwi6ski, 1986. Interrelationship between the process of surface wave generation caused by an air stream and wave attenuation process on water covered with a monolayer of crude oil derivative. Oceanologia, Warsz., 24:29-39.
Acoustically-determined viscoelastic properties of oil monolayers made it possible to define the conditions of loss of surface flow stability of a liquid caused by an air stream. Monolayer surface concentrations for which a stabilization maximum occurs have been determined and approach those at which the max- imum attenuation of a surface capillary layer is observed. The presence of a crude oil derivative surface monolayer results in the increase of the threshold stream velocity capable of wave genera- tion. Inst. of Exp. Phys., Univ. of Gdansk, Poland.
89:3191 Sclavounos, P.D., 1988. Radiation and diffraction of
second-order surface waves by floating bodies. J. Fluid Mech., 196: 65-91.
A theory is developed for the evaluation of the second-order velocity potential and wave forces valid for bodies of arbitrary geometry, which does not involve the evaluation of integrals over the free surface or require an increased accuracy in the solution of the linear problem. The second-order velocity potential is expressed as the sum of a particular and a homogeneous component. The former satisfies the non-homogeneous free-surface condition and is expressed explicitly in terms of the second-order Green functions. The latter is subject to the homogeneous free surface condition and enforces the body boundary condition by the solution of a linear problem. The singular behaviour of the second-order potential near the intersection of the body boundary with the free surface is analyzed.
484 A. Physical Oceanography O LR (1989) 36 (6)
Dept. of Ocean Engng, MIT, Cambridge, MA 02139, USA.
89:3192 Veerayya, M. and T. Pankajakshan, 1988. Variability
in wave refraction and resultant nearshore current patterns: exposed versus sheltered beaches along north Karnataka, west coast of India. Indian J. mar. Sci., 17(2): 102-110. Natl . Inst. of Oceanogr., Dona Paula, Panaji 403 004, India.
89:3193 Yoshikawa, Ikuo et al., 1988. Turbulent structure in
water under laboratory wind waves. J. oceanogr. Soc. Japan, 44(3): 143-156.
Laboratory experiments of the turbulent boundary layer underneath wind generated waves are de- scribed. While there is no question that the turbu- lence develops under close coupling to the char- acteristics of the wind-wave system, the structure underneath also shows downward bursting in a pattern similar to the familiar turbulent boundary layer that develops over a rough solid wall. Kobe Mar. Observ., Kobe, 650 Japan. (fcs)
AI70. Wind-wave interactions
89:3194 Mitsuyasu, Hisashi and Tadao Kusaba, 1988. On the
relation between the growth rate of water waves and wind speed. J. oceanogr. Soc. Japan, 44(3): 136-142.
Various wind velocities (friction velocity plus wind speeds at half-wavelength, wavelength, and 10 m above the surface) are correlated to the measured growth rate of water waves. It is shown that within a range of the dimensionless wind speed (wind friction velocity ~0.1/water wave phase velocity ~0.6), there are no appreciable differences in correlations. The growth rate for waves under rough surface conditions is greater than that for waves under smooth surface conditions. Results here are 1.7- to 1.8-foid larger than values obtained using Al'Zanaidi and Hui's (1984) relation. Res. Inst. for Appl. Mechanics, Kyushu Univ., Kasuga, 816 Japan.
AIS0. Internal waves and tides
1D:3195 Broutman, D. and R. Grimshaw, 1988. The ener-
getks of the interaction between short small- amplitude internal waves and inertial waves. J. Fluid Mech., 196:93-106.
The interaction between a wave packet of small- amplitude short internal waves and a finite-ampli- tude inertial wave field is described to second order in the short-wave amplitude. As the short internal waves propagate through the inertial wave field they generate a wave-induced train of trailing inertial waves, whose contribution to the total energy balance is described. Results obtained here com- plement previous findings that the short internal waves undergo a net change in energy after their encounter with the inertial wave field. Sch. of Math., Univ. of New South Wales, P.O. Box 1, Kensington, NSW 2033, Australia.
89:3196 La Violette, P.E. and R.A. Arnone, 1988. A tide-
generated internal waveform in the western approaches to the Strait of Gibraltar. J. geophys. Res., 93(C12): 15,653-15,667.
An internal waveform (depending on flow condi- tions, either an internal hydraulic jump or a lee wave) is a semipermanent feature over the Camarinal Sill in the western approaches to the Strait of Gibraltar. Comparison of data indicates that the waveform, generated at the interface between the Atlantic and Mediterranean waters, undergoes periodic changes wrought by interaction of the tidal current and the flow of the Atlantic and Mediterranean waters. We believe that the waveform is a major mixing mechanism between the two water masses. NORDA, Stennis Space Center, MS 39529, USA.
A210. Ice
89:3197 Craig, H., Y. Horibe and T. Sowers, 1988. Gravi-
tational separation of gases and isotopes in polar ice caps. Science, 242(4886): 1675-1678.
Atmospheric gases trapped in polar ice at the firn to ice transition layer are enriched in heavy isotopes and heavy gases relative to the free atmosphere. Maximum enrichments observed follow patterns predicted for gravitational equilibrium at the base of the firn layer. Gas ratios exhibit both positive and negative enrichments relative to air: negative en- richments of heavy gases are consistent with ob- served artifacts of vacuum stripping of gases from fractured ice and with the relative values of molec- ular diameters that govern capillary transport. These two models provide a basis for understanding initial enrichments of carbon-13 and oxygen-18 in trapped CO2, CH4, and 02 in ice cores, which must be known in order to decipher ancient atmospheric isotopic
tion patterns in sea ice. J. Glaciol., 34(118):301- 308. Geophys. Inst., Univ. of Oslo, Blindern, N-0315 Oslo 3, Norway.
89:3199 Neralla, V.R., R.G. Jessup and S. Venkatesh, 1988.
The Atmospheric Environment Service regional ice model (RIM) for operational applications. Mar. Geod., 12(2):135-153.
An adaptation of the Cold Regions Research and Engineering Laboratory's sea ice dynamic/ther- modynamic model, the RIM permits short-range, near real-time forecasting of ice conditions for navigational and offshore operations purposes. Internal ice resistance is treated in the model based on Hibler's (1979) depiction of ice as a viscous plastic substance. An example is presented for the Beaufort Sea. Atmos. Environ. Service, Downsview, ON M3H 5T4, Canada. (slr)
89:3200 Overland, J.E. and C.H. Pease, 1988. Modeling ice
dynamics of coastal seas. J. geophys. Res., 93(C12): 15,619-15,637.
A coupled sea ice, barotropic ocean model with a l-km resolution and a seaward domain of 200 km quantifies three coastal processes: coupling of ice motion to wind-driven coastal currents, ice thickness redistribution under compaction at the coast, and formation of coastal shear zones. The model consists of an ice momentum balance, mass concentration and two-parameter ice thickness distribution, and equations for horizontal water motion and conti- nuity using vertical structure functions. Results indicate that (1) ice thickness/motion feedback is important on scales ( 1 0 kin, (2) the observational base to discriminate between mesoscale constitutive laws is not yet available, and (3) the relation of ice velocity to wind stress is variable because the ocean slope current responds only to the alongshore component of the wind. PMEL, NOAA, 7600 Sand Point Way, N.E., Seattle, WA 98115, USA.
89:3201 Palais, J.M. and P.R. Kyle, 1988. Cl~mical compo-
sition of ice contalnin~ tephra layers in the Byrd Station ice core, Antarctica. Quat. Res., 30(3): 315-330.
Ice samples that contain tephra layers have, on average, about two times more sulfate and three to
89:3202 Pritchard, R.S., 1988. Mathematical characteristics of
sea ice dynamics models. J. geophys. Res., 93(C12): 15,609-15,618.
IceCasting, Inc., 11042 Sand Point Way, N.E., Seattle, WA 98125-5846, USA.
A240. Optical properties 89:3203
Prikhach, A.S., 1987. Illumination intensity under a rough sea surface illuminated by a narrow light beam. Izv. Atmos. Ocean Phys. (a translation of Fiz. Atmos. Okeana), 23(9):730-735. Inst. of Phys., Belorussian Acad. of Sci., USSR.
A250. Electromagnetic properties 89:3204
Junge, Andreas, 1988. The telluric field in northern Germany induced by tidal motion in the North Sea. Geophys. J., 95(3):523-533. Inst. fur Geophys., Postfach 2341, D-3400 Gottingen, FRG.
A260. Acoustics 89:3205
Collins, M.D., 1988. The time-domain solution of the wide-angle parabolic equation including the ef- fects of sediment dispersion. J. acoust. Soc. Am., 84(6):2114-2125. NORDA, Stennis Space Cen- ter, MS 39529, USA.
486 A. Physical Oceanographj OLR (1989) 36 (6)
89:3206 d'Agostino, Luca and C.E. Brennen, 1988. Acoustical
absorption and scattering cross sections of spher- ical bubble clouds. J. acoust. Soc. Am., 84(6): 2126-2134. Calif. Inst. of Tech., Pasadena, CA 91125, USA.
89:3207 Godin, O.A., 1988. A wave equation for sound in a
medium with slow currents. Dokl. Earth Sci. Sect. (a translation of Dokl. Akad. Nauk SSSR), 293(1-6):4-7. Shirshov Inst. of Oceanol., Acad. of Sci., Moscow, USSR.
89:3208 Godin, O.A. and I.V. Prokopyuk, 1987. Reflection of
a spherical wave from an interface between media with similar properties, lzv. Atmos. Ocean Phys. (a translation of Fiz. Atrnos. Okeana), 23(9):692- 699. Inst. of Oceanol., Acad. of Sci., USSR.
89:3209 Knapp, C.H., 1989. Signal detectors for deformable
hydrophone arrays. IEEE Trans. A coust. Speech Signal Process., 37(1): 1-7. Univ. of Connecticut, Storrs, CT 06268, USA.
89:3210 Lauterborn, W. and U. Parlitz, 1988. Methods of
chaos physics and their application to acoustics. J. acoust. Soc. Am., 84(6):1975-1993.
This article gives an introduction to the research area of chaos physics. The new language and basic tools are presented and illustrated by examples from acoustics: a bubble in water driven by a sound field and other nonlinear oscillators. The notions of strange attractors and their basins, bifurcations and bifurcation diagrams, Poincar~ maps, phase dia- grams, fractal dimensions, scaling spectra, recon- struction of attractors from time series, winding numbers, as well as Lyapunov exponents, spectra, and diagrams are addressed. Drittes Phys. Inst., Univ. Gottingen, Burgerstr. 42-44, D-3400 Gottin- gen, FRG.
89:3211 Li, Saimu and C.S. Clay, 1988. Sound transmission
experiments from an impulsive source near rigid wedges. J. acoust. Soc. Am., 84(6):2135-2143. Shandong Coll. of Oceanogr., Qingdao, People's Republic of China.
89:3212 Pillai, S.U. and B.H. Kwon, 1989. Forward/backward
spatial smoothing techniques for coherent signal identification. IEEE Trans. Acoust. Speech Signal Process., 37(1):8-15. Dept. of Elec. Engng and Computer Sci., Polytech. Univ., Brooklyn, NY, USA.
89:3213 Schmidt, Henrik and W.A. Kuperman, 1988. Esti-
mation of surface noise source level from low- frequency seismoacoustic ambient noise meas- urements. J. acoust. Soc. Am., 84(6):2153-2162. MIT, Cambridge, MA 02139, USA.
89:3214 Swingler, D.N. and R.S. Walker, 1989. Line-array
bcanfforming using linear prediction for aperture interpolation and extrapolation. 1EEE Trans. Acoust. Speech Signal Process., 37(1):16-30. Div. of Engng, St. Mary's Univ., Halifax, NS B3H 3C3, Canada.
89:3215 Thorne, P.D. and D.J. Foden, 1988. Generation of
underwater sound by c o m m ~ spber~. J. acoust. Soc. Am., 84(6):2144-2152. Proudman Oceanogr. Lab., Bidston Observ., Birkenhead, Merseyside L43 7RA, UK.
89:3216 Anisimova, Ye.P., S.S. Matkheyev and A.A. Speran-
skaya, 1987. Horizontal turbulent flux of mo- mentum in an intense convective eddy. lzv. A tmos. Ocean Phys. (a translation of Fiz. A tmos. Okeana), 23(9):736-739. Univ. of Moscow, USSR.
89:3217 Denes, T.A. and J.M. Caffrey, 1988. Changes in
seasonal water transport in a Louisiana estuary, Fourleague Bay, Iamislana. Estuaries, 11(3): 184- 191. U.S. Army Corps of Engr., Coastal Engng Res. Center, P.O. Box 631, Vicksburg, MS 39180, USA.
OLR (1989) 36 (6) A. Physical Oceanography 487
89:3218 Druet, Czeslaw and Ryszard Siwecki, 1986. Char-
acteristics of turbulent horizontal heat exchange in subsurface layers of the Southern Ocean. Part H. Indian Ocean and Pacific. Oceanologia, Warsz., 24:3-10.
This paper is part two of a study dealing with the coefficients and scales of turbulent horizontal heat exchange in the subsurface layer of the Southern Ocean. Resultant basic equations, assumptions, and empirical data form the basis of the method chosen to determine the turbulent horizontal heat exchange coefficients and iinear horizontal dimensions of thermal eddy structures occurring in this layer. Characteristics of turbulent heat exchange for the South Atlantic are presented. Inst. of Oceanol., Acad. of Sci., Sopot, Poland.
89:3219 Gallagher, J.B. and H.R. Burton, 1988. Seasonal
mixing of Ellis Fjord, Vesffold Hills, East Antarctica. Estuar. coast. Shelf Sci., 27(4):363- 380. Burton: Australian Antarctic Div., Channel Hwy., Kingston, Tas. 7050, Australia.
89:3220 Romanof, Nicolae, 1988. Applications of the random
process theory to the turbulence theory: contri- butions to the stochastic study of turbulent diffusion. Meteorology Hydrol., Bucuresti, 18(1): 3-49.
89:3221 Savenije, H.H.G., 1988. Influence of rain and evap-
oration on salt intrusion in estuaries. J. hydraul. Engng, Am. Soc. cir. Engrs, 114(12):1509-1524.
The influence of local evaporation and rainfall on the salinity of estuary water is generally neglected in salt intrusion models; in the Gambia Estuary, however, it is important. A model is presented to simulate salt intrusion, taking into account the effects of local rain and evaporation. Euroconsult, P.O. Box 441, Arnhem, Netherlands.
89:3222 Williams, R.G., 1988. Modification of ocean eddies
by uir-sca interaction. J. geophys. Res., 93(C12): 15,523-15,533.
A mixed-layer model shows that an eddy is modified by the air-sea interaction for the local environment and the feedback from its SST signal, which alters the surface heat and water fluxes. This buoyancy forcing tends to decrease the eddy temperature anomaly; seasonal changes in mixed-layer depth lead to the surface signal being removed in summer
and reappearing in winter. Buoyancy forcing alters the eddy velocity profile and, over several seasons, may lead to the formation of a subsurface velocity maximum. After the spring decrease in mixed-layer depth, the eddy potential vorticity anomaly is reduced, and lateral mixing may subsequently play a role in further eroding the eddy. Dept. of Phys., Imperial Coll. of Sci. and Tech., Prince Consort Rd., London, SW7 2BZ, UK.
89:3223 Yanagi, Tetsuo and Atsuhiko Isobe, 1987. Density
inversion in the coastal sea. Umi to Sora, 63(2):79-90. (In Japanese, English abstract.) Dept. of Ocean Engng, Ehime Univ., Matsu- yama, Japan.
A300. Fluid mechanics
89:3224 Brevdo, Leonid, 1988. A study of absolute and
convective instabilities with an application to the Eady model. Geophys. astrophys. Fluid Dynam., 40(1-2):1-92. Dept. of Math. and Statistics, Univ. of Alabama, Huntsville, AL 35899, USA.
89:3225 Godin, O.A., 1988. Reciprocity relations for waves in
a compressible liquid. Dokl. Earth Sci. Sect. (a translation of Dokl. Akad. Nauk SSSR), 293(1- 6):14-16. Shirshov Inst. of Oceanol., Acad. of Sci., Moscow, USSR.
89:3226 Monin, A.S., 1988. Negative viscosity in global
circulations. Dokl. Earth Sci. Sect. (a translation of Dokl..4kad. Nauk SSSR), 293(1-6):11-13.
Negative viscosity terms arise in the statistical treatment of momentum transport from domains of low density to those of high density where kinetic energy is transferred from fluctuating motions to averaged ones. Manifestations of negative viscosity are discussed as they arise in circulation models of the Earth's atmosphere and oceans, and of the global circulations of the Sun, Jupiter and Saturn. Shirshov Inst. of Oceanol., Acad. of Sci., Moscow, USSR. (fcs)
89:3227 Vvedenskaya, N.D. and L.R. Volevich, 1987. Motion
of localized vorticity on the surface of a rotating sphere. Izv. Atmos. Ocean Phys. (a translation of Fiz. Atmos. Okeana), 23(9):744-746. Inst. of Problems of Info. Transmission, Acad. of Sci., USSR.
