A Modelling Study of Coastal Upwelling Driven By

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I Journal of Coastal Research | 20 | 3 | 662-671 | West Palm Beach, Florida I Summer 2004 |

A Modelling Study of Coastal Upwelling Driven byWind and Meanders of the Brazil CurrentRenato M. Castelaoa,*, Edmo J. D. Cainposa and Jerry L. Millerb +aInstituto OceanograficoUniversity of Sao PauloPraca do Oceanogrifico, 191Cid. Universitdria05508-900 Sao Paulo, SPBrazil

bOceanography DivisionNaval Research LaboratoryStennis Space Center, MS,

U.S.A.

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CASTELAO, R.M.; CAMPOS, E.J.D., and MILLER, J.L., 2004. A modelling study of coastal upwelling driven by windand meanders of the Brazil Current. Journalof CoastalResearch, 20(3), 662-671. West Palm Beach (Florida), ISSN0749-0208.A numerical model is used to investigate coastal upwelling in the South Brazil Bight. Th e wind in the area is pre-dominantly from the northeast, especially in summer, which is upwelling favorable. Reversals of the wind directionare frequent and intense during the winter, due to the passage of frontal systems. The offshore circulation is dominatedby the Brazil Current, which flows southward meandering around the 200 m isobath. Significant shelf-break u pwellinghas being associated with Brazil Current cyclonic meanders. To assess the relative importance of the two processesin the pumping of South Atlantic Central Water (SACW) onto the continental shelf, three cases are analyzed: (1)wind-driven upwelling; (2) upwelling induced by Brazil Current meanders and (3)both effects acting together. Theresults show that in the coastal area upwelling/downwelling is mainly caused by the wind, whereas the cyclonicmeanders of the Brazil Current are the dominant mechanism in the generation of vertical velocities over the shelfbreak and slope. This meander-induced upward motion brings the SACW to shallower depths, where it is influencedby the wind. In this situation, when both effects act together, the SACW penetrates all the way to the coast.ADDMTIONAL INDEX WORDS: Coastal oceanography, coastal upwelling, wind-driven circulation, shelfdynamics,Brazil Current,cyclonic meander, Brazil, South BrazilBight.

INTRODUCTIONThe Study Area

The area of interest of this study is usually referred in theliterature as the South Brazil Bight (SBB), with Cabo Frioas its northern limit, and Cabo de Santa Marta as its south-ern limit (Figure 1). CASTRO and MIRANDA (1998), in theirreview of coastal oceanography off Brazil, consider that thewater on the upper slope and shelf of the SBB are the resultof mixing of three water masses: Tropical Water-TW(T>20C, S>36.40), South Atlantic Central Water-SACW(T


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Modelling Study of Coastal Upwelling 663

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-51 -50 -49 -48 -470 -460 -450 -440 -430 -42 -41 -40 -390 -38 -370 -36 -350Figure 1. Study area with bottom topography. The light shaded area shows the model domain. The dotted thick line shows the location of Line A, andthe dotted thin lines mark the area shown in plots of model results. Topographic contours are (in meters) 50, 100, 200, 500, 1000, 1500, 2000, and 2500In the lower right hand corner, an inserted satellite-derived image illustrates the meandering of the Brazil Current in the region.

the leading portion of the meander flows southward, up-welled water is advected toward the continental shelf. Suchmeanders and eddies appear to be a ubiquitous feature ofwestern boundary current systems (MILLER and LEE, 1995a).The meanders, occurring in the area between the shelf andthe deep ocean, provide an important communication be-tween these two regions, since most of the nutrients that sup-port the high biological productivity of continental shelvescome from the deeper adjacent ocean. LEMING (1981) ob-served large amounts of cold water pumped onto the conti-nental shelf close to Cape Canaveral, associated with a shelf

break meander of the Gulf Stream. Gulf Stream cold coresand warm filaments transport heat, salt, and other substanc-es between the continental shelf and the adjacent deep oceanto such an extent that the hydrography (ATKINSON et al.1983) and primary productivity (LEE et al., 1991) of the shelfcan be substantially altered by meander behavior (MILLERand LEE, 1995b).Significant shelf break upwelling has been associated withBrazil Current cyclonic meanders. BRANDINI (1990) statesthat, at some places along the SBB shelf break, productivitycan be higher than in the coastal zone, especially during sum-

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664 Castelao, Campos and Miller

0-100 -

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-400 --50Dn-- I I I I , I I I0 100 200 300 400 500 600 700 800

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Figure 2. Initial (a) temperature and (b) salinity cross section. Thethicker line represents the interface between Tropical Water and SouthAtlantic Central Water (T =20'C, S = 36.4). Contour interval is 20C(temperature) and 0.2 (salinity).

0--100 -

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-400 --500 I I I I I I I0 100 200 300 400 500 600 700 800

Distance (kmn)

-100 -

E-200-8 -300 -

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Distance (kn)Figure 3. Temperature and salinity cross-section at Line A at day 16 forthe simulation forced by the northeasterly wind (Exp. 1). Contour inter-vals as in Figure 2.

mertime. CAMpos et al. (1995) suggest that the combinationof near-shore wind-driven upwelling and deeper shelf breakupwelling may be responsible for the transport of the nutri-ent-rich SACW from regions deeper than 200 m to the shal-lower parts of the continental shelf near the coast.Objective and Structure of this Article

The present study was based on numerical simulationswith the objective of investigating the importance of the twoprocesses in pumping SACW onto the continental shelf.Section 2 presents the model configuration and the initialand boundary conditions used. The wind driven upwelling,the upwelling induced by cyclonic meanders of the BrazilCurrent and the interactions of the two processes are dis-

cussed in section 3. Section 4 presents the summary and con-clusions.METHIODOLOGY

Model Configuration and Initial ConditionsThe model used is the Princeton Ocean Model (POM)

(BLUMBERG and MELLOR, 1987). It is a finite difference,three-dimensional model, containing a second-order turbu-lence closure submodel providing the vertical mixing coeffi-cients (MELLOR and YAMADA, 1982). The domain used (Fig-ure 1)extends about 1380 km alongshore from Cabo de SantaMarta to Cabo Frio, and about 850 km offshore from Santos,covering the entire South Brazil Bight. The horizontal gridspacing was 10 km in the alongshore direction, and 5 km inthe offshore direction. The first baroclinic Rossby radius at

Table 1. Summary of numericalexperiments.Exper- Imposed Begin Wind Duration (days)iment Forcing Mechanism Velocities Forcing (day) of ExperimentExp. 1 NE wind zero zero 16Exp. 2 SW wind zero zero 16Exp. 3 BC meanders geostr. vel. - 60Exp. 4 BC meanders + NE wind geostr. vel. 30 60Exp. 5 BC meanders + SW wind geostr. vel. 30 60

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Figure 7. Temperature and salinity cross-section at day 46 for the Brazil Current simulation (Exp. 3) (a,b) 10 km and (c,d) 70 km northward of Line A.Contour intervals as in Figure 2.

welling the SACW onto the shelf, a set of numerical experi-ments were pursued, which are summarized in Table 1. InExperiments 1 and 2, a spatially uniform time-independentwind stress of 0.1 Pa wa s considered as forcing. The windwas oriented 50 relative to true north (Exp. 1-NE, Exp. 2-SW). No initial velocities were imposed. The model was runfor 16 days, so there was not enough time for the westernboundary current to develop and become unstable, andchanges in the mass field are mostly wind driven. Although16 days of constant wind is unrealistic, a relatively long sim-ulation is needed to represent an integrated effect of the pre-dominance in the wind direction in each season (northeast-erly during summer, southwesterly during winter). In Exper-iment 3, both the density field and the associated velocityfield were used as initial conditions. No wind forcing wa s ap-plied, so the upwelling induced by cyclonic meanders of theBrazil Current could be isolated.Experiments 4 and 5 are similar to Experiment 3, exceptthat the wind wa s turned on after 30 days (with the samecharacteristics as in Experiments 1 and 2) in order to simu-late the combined effect of the wind and the meanders. Themass field computed in Experiments 1and 2 after 16 days ofwind forcing is then compared with the mass field computedin Experiments 3-5 after 46 days at Line A. This representsthe moment of maximum meander induced upwelling at LineA (Exp. 3) and, for Experiments 4 and 5, 16 days of windforcing (from day 30 to 46).

Wind Forcing ExperimentsThe ocean response to northeasterly winds (Exp. 1)is sim-

ilar to the classical upwelling picture described by ALLEN(1980). The wind stress drives an offshore transport in a sur-face Ekman layer that generates a depression of the sea sur-face. A geostrophic jet is established, flowing southward. Th ecoastal jet is stronger where the shelf is narrow (close to CaboFrio). While the surface velocities are deflected offshore (rel-ative to the geostrophic flow), an onshore flow develops be-low. The onshore flow offsets the offshore surface Ekman lay-er flow, allowing the sea surface slope to remain in a quasi-steady state while feeding an upwelling circulation (LI andWEISBERG, 1999). Near the coast, then, the ocean responsecomprises a superposition of geostrophic and Ekman circu-lation. Offshore of this region, surface velocities are deflectednearly 45 to the left of the wind direction, while the bottomvelocities are zero or very small. The temperature and salin-ity sections along Line A after 16 days are shown in Figure3. The wind effect can be clearly seen, especially close to thecoast, where the most intense vertical velocities are found.The northeasterly wind advects surface water offshore (eg.26C isotherm, 36.4 isohaline) and upwells water from thebottom (Figure 3 a,b). After 4 days (not shown), the 20C iso-therm reaches the surface. After 16 days, it is possible toobserve some upwelling at the shelf break (seen as a slightelevation of the isotherms and isohalines), but the upwelling

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0 100 200 300 400 500 600 700 800 0 100 200 300 400 500 600 700 800Distance (kln) Distance (kmn)Figure 8. Temperature and salinity cross-section at Line A at day 46 for Figure 9. Temperature and salinity cross section at day 46 for the sim-the simulation forced by the northeasterly wind and the Brazil Current ulation forced by the northeasterly wind and the Brazil Current (Exp. 4)(Exp. 4). Contour intervals as in Figure 2. 120 km northward of Line A. Contour intervals as in Figure 2.

there is not as evident as in the coastal zone. The upwellingcirculation forced by northeasterly wind alone was not -22-enough to connect the SACW core present on the shelf withthe same water mass in the deep ocean. -23-The shelf response to southwesterly wind (Exp. 2) is op -posite to the previous case. The surface Ekman transport is -24-onshore, creating a surface convergence which results in asloping sea surface. Since the alongshore component of flow -25'is essentially in geostrophic balance, a coastal je t is estab- 25lished, flowing northward nearly parallel to isobaths. Thesurface velocities are deflected toward the coast, while below -26-the velocities are deflected in the offshore direction. This off-set of the velocities feeds the downwelling circulation. After -27-16 days, isotherms slope downward toward the coast (Figure4a). The region closer to the coast (inshore of 40-50 m) isessentially vertically homogeneous (Figures 4a,b), a result -28- CSMsimilar to what wa s found by ALLEN and NEWBERGER (1996)for the Oregon coast under downwelling wind conditions. -29- -The computed volume of SACW in a 10 km wide slice over -50- -49 -48 -4 7 -46- -45 -44- -43 -42- -41-the shelf along Line A is given in Table 2. There is a general Figure 10. Minimum depth reached by the SACW at day 46 for the sim-tendency for decreasing the volume of SACW with time. Com- ulation forced by the northeasterly wind and the Brazil Current (Exp. 4).paring Experiments 1and 2, we see that the upwelling winds Contours are (in meters) 70, 80, 90, 100, 120 and 140. The thicker contourtendo retard this process, while the downwelling winds ac- is the 100 m isobath. The across-shore line shows the location of Line A.tend to retard th s process, wile the downwellng wins ac- CF: Cabo Frio, CSM: Cabo de Santa Marta.celerate the decrease of the volume. ______________________________

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to the north of Line A (Figure 9) shows a core of SACW overthe shelf disconnected from the same water mass present onthe slope, suggesting that the increase in the volume ofSACW along Line A is caused by local upwelling in the vicin-ities of that section, and not by southward advection fromfarther north. Indeed, a plot of the minimum depth reachedby the SACW (Figure 10) shows that the upwelling alongLine A is localized. It can also be seen that upwelling is en-hanced in the vicinities of Cabo Frio. Figure 11 shows a con-tour plot of vertical velocity at Line A, day 46. Two local max-imums of vertical velocity are found, one over the mid-shelf(associated with the wind forcing) and another over the slope(caused by the cyclonic meander). Values of computed upwardvelocity over the slope were similar to values found by CAM-Pos et al. (1999). The cyclonic meander brings the SACW toshallower depths, exposing it to northeasterly wind effect.Both effects acting together increase the amount of upwelledwater (Table 2). When the wind is southwesterly (downwell-ing favorable, Exp. 5), the two mechanisms opposed one an-other. There are still some upwelling at the shelf break,which is caused by the cyclonic meander by itself (Figure 12-compare to Figure 6, parts a-d), but it is not enough to con-nect the deep ocean SACW and the shelf core. Close to thecoast, isotherms slope downward, similar to the results usingthe southwesterly wind as the only forcing (Exp. 2, Figure 4),and the volume of SACW over the shelf is greatly decreased(Table 2).

SUMMARY AND CONCLUSIONSA primitive equation model has been used to simulate Bra-zil Current meanders and the wind driven circulation of theSouth Brazil Bight. The numerical experiments performedshow that the coastal ocean response to wind forcing in theSBB comprises a superposition of geostrophic and Ekman cir-culation. Alongshore wind generates a surface cross-shelftransport. When the wind is from the northeast, this surfacecross-shelf transport is offshore, causing coastal divergenceand establishing a coastal jet. The flow below the surface isdeflected toward the coast, feeding upwelling circulation.When the wind is from the southwest, the surface cross-shelf

transport is onshore. Northward geostrophic flow is estab-lished. In this situation, the flow is deflected offshore belowthe surface. The offset of the surface and bottom velocitiesmaintains a downwelling circulation.

At the shelf break, the cyclonic meanders of the Brazil Cur-rent represent an efficient mechanism for generation of ver-tical velocities, acting decisively in the upwelling of SACW.Combined with upwelling favorable winds, there is a positiveinteraction: the meander-induced upwelling brings theSACW to shallower depths, exposing it to the northeasterlywind effect. In this situation, the SACW in deep water is con-nected to the core over the shelf which was present in theinitial conditions, reaching all the way to the coast along thecontinental shelf. This is similar to the findings of CAMPoset aL (1999) data results, which show that during the winter,when coastal upwelling is diminished and practically only themeander-induced upwelling occurs, the SACW was confinedto the shelf break.

There is a general tendency for decreasing the volume ofSACW with time (Table 2). A comparison between Experi-ments I and 2 shows that upwelling winds tend to retard thisprocess, while the downwelling wind s accelerate the decreaseof the volume. When no wind forcing is imposed (Exp. 3), thevolume of SACW over the shelf after 30 days is -73% of thevolume present in the initial conditions. After continuing de-creasing (day 38), the cyclonic meander causes an increase inits volume (day 46-Exp. 3). This increase can be greatly am-plified by the northeasterly wind forcing (Exp. 4). Experiment5 is similar to Experiment 2, with the southwesterly windsaccelerating the decrease of the volume of SACW over theshelf. Both the wind and the cyclonic meanders of the BrazilCurrent seem to be important in the upwelling process,pumping the SACW from deep water onto the continentalshelf, which may have important chemical/biological conse-quences. Indeed, BRANDINI (1990) found concentrations ofphosphate and nitrate within the euphotic zone at a cold me-ander of the SBB comparatively higher than in adjacent oce-anic waters. ATKINSON et al. (1996) found that northwardwind stress, together with frontal eddies of the Gulf Stream,causes cold, nutrient rich water to rise to the shelf edge andpenetrate shoreward to the coast.Although the wind-forced onshore transport of nutrient-rich water certainly has a high seasonal variability, beinghigher in summer, the cyclonic meander-induced upwellingcan occur even in winter. DEIBEL (1985), in a study off SouthCarolina (USA), reports high levels of biological activity dur-ing wintertime, implying nutrient input from the GulfStream. This suggests that, at least on the outer continentalshelf of the South Brazil Bight, onshore nutrient transportmay occur during all seasons.

ACKNOWLEDGEMENTSWe gratefully acknowledge support from the Fundagao deAmparo a Pesquisa do Estado de Sao Paulo (FAPESP-grant98/14648-0) and from the Inter American Institute for GlobalChange Research (LAI), through projects SAMC (IAI-ISPI)and SACC (CRN-061). Project COROAS was funded by FA-PESP (grant 91/0542-7) and CNPq (Conselho Nacional de De-senvolvimento Cientifico e Tecnol6gico-grant 40.3007/91.7).

J. Miller was funded by U.S. Grants.LITERATURE CITED

ALLEN, J.S., 1980. Models of wind-driven currents on the continentalshelf. Ann. Rev. Fluid Mech., 12, 389-433.ALLEN, J.S. and NEWBERGER, P.A., 1996. Downwelling circulationon the Oregon continental Shelf. Part I: response to idealized forc-ing. Journalof Physical Oceanography26, 2011-2035.ATKINSON, L.P.; LEE, T.N.; BLANTON, J.O., and CHANDLER, W.S.,1983. Climatology of the southeast U.S. continental shelf waters.Journalof Geophysical Research 88, 4705-4718.ATKINSON, L.P.; MILLER, J.L.; LEE, T.N., and DUNSTAN, W.M.,1996. Nutrients and chlorophyll at the shelf break off the south-eastern United States during the Genesis of Atlantic Lows Exper-iment: winter 1986. Journalof GeophysicalResearch 101, 20565-20578.BLUMBERG, A.F. and KANTHA, L.H., 1985. Open boundary condi-tions for circulation models. Journal of Hydraulic Engineering,ASCE, 111, 237-255.BLUMBERG, A-F. and MELLOR, G.L., 1987. A description of a three-

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BRANDINI, F.P., 1990. Hydrography and characteristics of the phy-toplankton in shelf and oceanic waters off southeastern Brazil dur-ing winter (July/August 1982) an d summer (February/March1984). Hydrobiologia196, 111-148.CAMPos, E.J.D.; GONQALVES, J.E., an d IKEDA, Y., 1995. Water MassCharacteristics an d Geostrophic Circulation in the South BrazilBight-summer of 1991. Journalof Geophysical Research 100(9),18537-18550.CAMPOS, E.J.D.; IKEDA, Y.; CAsTRo FO, B.M.; GAETA, SA.; LOR-ENZZETTI, J.A., an d STEVENSON, M.R., 1996. Experiment StudiesCirculation in the Eastern South Atlantic. EOS, Transactions,American Geophysical Union 77 (27) 253,259.

CAMPos, E.J.D.; VELHOTE, D., and DA SILvEIRA, I.C.A., 1999. ShelfBreak Upwelling driven by Brazil Current Cyclonic Meanders.Geophysical Research Letters 26, No 14, 2061-2064.CASTRO, B.M. and MIRANDA, L.B., 1998. Physical Oceanography ofthe Western Atlantic Continental Shelf Located between 4N and340S. In: ROBINSON, A.R. and BRINK, KH. (eds.), The Sea, vol. 11.John Wiley, New York, pp. 209-251.CAsTRo F , B.M.; MIRANDA, L.B., an d MIYAo, S.Y., 1987. Condicoes

hidrograficas na plataforma continental ao largo de Ubatuba: var-iac6es sazonais e em m6dia escala. Boletim do Instituto Oceano-grdfico 35(2), 135-151.DEIBEL, D., 1985. Blooms of the pelagic tunicate, Doliolettagegen-bauri:Are they associated with Gulf Stream frontal eddies? Jour-nal of MarineResearch 43, 211-236.HouRY, S.; DOMBROWSKY, E.; MEY, P., and MINSTER, J.F., 1987.

Brunt-Viiisalai frequency and Rossby Radii in the South Atlantic.Journalof Physical Oceanography 17, 1619-1626.LEE, T.N.; YODER, JA., and ATINSON, L.P., 1991. Gulf Streamfrontal eddy influence on productivity of the southeast U.S. con-tinental shelf. Journalof GeophysicalResearch 96, 22191-22205.LEMING, T.D., 1981. Cold water intrusion an d upwelling near CapeCanaveral, Florida, 2, American Geophysical Union, Washington,D.C., 63-71.Li, Z. an d WEISBERG, R.H., 1999. West Florida Shelf Response toUpwelling Favorable Wind Forcing: Kinematics. Journal of Geo-physicalResearch 104, 13507-13527.MARTINSEN, EA. an d ENGEDAI-IL, H., 1987. Implementation andtesting of a lateral boundary scheme as an open boundary condi-tion in a barotropic ocean model. CoastalEngineering11,603-627.MATSUURA, Y., 1996. A probable cause of recruitment failure of thebrazilian sardine (Sardinella aurita)population during the 1974/75 spawning season. SouthAfrican JournalofMarineSciences17,29-35.MELLOR, G.L. an d YAADA, T., 1982. Development of a turbulenceclosure submodel for geophysical fluid problems. Reviews of Geo-physicsand Space Physics 20, 851-875.MILLER, J.L. and LEE, T.N., 1995a. Gulf Stream meanders in theSouth Atlantic Bight. 1. Scaling and energetics. Journalof Geo-physicalResearch 100, 6687-6704.MILLER, J.L. an d LEE, T.N., 1995b. Gulf Stream meanders in theSouth Atlantic Bight. 2. Momentum balances. JournalofGeophys-ical Research 100, 6705-6723.ORLANSKI, I., 1976. A simple boundary condition for unbounded hy-perbolic flows. Journalof ComputationalPhysics 21, 251-269.OSGOOD, KE.; BANE, J.M., and DEWAR, W.K., 1987. Vertical veloc-ities and dynamical balances in Gulf Stream meanders. Journalof GeophysicalResearch 92, 13029-13040.

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