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Dynamics of the Cape Farewell Upwelling Plume, New Zealand

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Dynamics of the Cape Farewell Upwelling Plume, New Zealand New Zealand Journal of Marine and Freshwater Research ISSN: 0028-8330 (Print) 1175-8805 (Online) Journal homepage: http://www.tandfonline.com/loi/tnzm20 Dynamics of the Cape Farewell upwelling plume, New Zealand T. G. L. Shlrtcliffe , M. I. Moore , A. G. Cole , A. B. Viner , R. Baldwin & B. Chapman To cite this article: T. G. L. Shlrtcliffe , M. I. Moore , A. G. Cole , A. B. Viner , R. Baldwin & B. Chapman (1990) Dynamics of the Cape Farewell upwelling plume, New Zealand, New Zealand Journal of Marine and Freshwater Research, 24:4, 555-568, DOI: 10.1080/00288330.1990.9516446 To link to this article: http://dx.doi.org/10.1080/00288330.1990.9516446 Published online: 30 Mar 2010. Submit your article to this journal Article views: 108 View related articles Citing articles: 15 View citing articles Full Terms & Conditions of access and use can be found at http://www.tandfonline.com/action/journalInformation?journalCode=tnzm20 Download by: [203.118.161.175] Date: 14 February 2017, At: 22:09 New Zealand Journal of Marine and Freshwater Research, 1990, Vol. 24: 555-568 555 0028-8330/2404-0555 $2.50/0 © Crown copyright 1990 Dynamics of the Cape Farewell upwelling plume, New Zealand T. G. L. SfflRTCLIFFE Keywords Cape Farewell; Farewell Spit; M. I. MOORE* Kahurangi; upwelling; Research School of Earth Sciences Victoria University of Wellington INTRODUCTION P.O. Box 600, Wellington, New Zealand Cape Farewell forms the north-west comer of the *Present address: New Zealand Occanographic South Island of New Zealand (Fig. 1). To the north Institute, DSIR Marine and Freshwater, Department lies a large bay which extends c. 110 km north-east to of Scientific and Industrial Research, Private Bag, Cape Egmont and c. 185 km south-east to the Kilbirnie, Wellington, New Zealand Wellington coast of the North Island. Nomenclature is variable, but in this paper the bay thus defined will A. G. COLE be referred to as Taranaki Bight. At its south-east New Zealand Oceanographic Institute comer, Cook Strait separates the North from the South Island and leads to the east coast waters. The A. B. VINER region is windy, with frequent strong winds from the west, and there are strong tidal currents through Cook Taupo Research Laboratory Strait. DSIR Marine and Freshwater The Cape Farewell area is known to include the Department of Scientific and Industrial Research source of an intermittent plume of water which upwells P.O. Box 415, Taupo, New Zealand from a depth of about 100 m; it has been investigated several times. Cruise 1155 of R V Tangaroa visited the R. BALDWIN area in January 1984 with a primary goal of B. CHAPMAN investigating small-scale features and mixing New Zealand Oceanographic Institute associated with this plume. The present paper reviews previous investigations, describes the hydrological observations which were made, and presents a Abstract Hydrological observations made in theoretical description which accommodates the January 1984 in the region near Cape Farewell, New principal features of the observations. The small- Zealand, are described and previously published scale processes are considered elsewhere. Chief observations reviewed. It is shown that upwelling interest in the present analysis lies in clarifying the depends on the existence of the intermittent Westland role of onshore winds in accelerating the longshore Current, and is intensified by an onshore wind. Such flow and intensifying the upwelling inshore of a wind induces a fall in sea level near Cape Farewell, Kahurangi Shoals. and the resulting favourable sea surface slope accelerates deep water over the bathymetric rise Review of previous work inshore of Kahurangi Shoals. The hydraulic response The first published observation that an extensive of the thermocline, coupled with a coastal convergence region of cold water near Cape Farewell resulted of the bottom Ekman flow, produce a strong upwelling from the upwelling of subsurface water was that of source near Kahurangi Point. Garner (1954). The data published in that paper were surface temperature measurements made from commercial ships. Garner (1959) published a M90020 temperature section measured from HMNZS Lachlan Received 26 March 1990; accepted 4 October 1990 in October 1951 which showed a band of cold water 556 New Zealand Journal of Marine and Freshwater Research, 1990, Vol. 24 r-^.- •:••:•••. 39 s •.••• .•••.• NORTH.-• •.•.•••.-.'••.•ISLAND •.••••• K- BIGHT Kahurangi Shoals GOLDEHH Kahurangi Pt. BAY \ Steep''Ft. KARAMEA BIGHT Cape Foulwind Fig. 1 Location of the observations. north of Cape Farewell. However, in the same paper, water. He believed that upwelling was general along a contrasting near-coast survey by Lachlan of sea the coast, but locally intensified at certain points. surface temperature round the South Island in Stanton (1976) surveyed the area again in 1974, February/March 1952 w;is presented, and this showed in the course of a study of regional geostrophic flow. a tongue of warm water stretching southwards along Conditions had been calm, and the near-coastal flow the entire West Coast, with no sign of upwelling. was southward at all depths, with no upwelling. A The first detailed study of the area was conducted tongue of warm saline water projected south-west in 1969 by Stanton (1971). Upwelling was present, into the study area north of Cape Farewell. Stanton more marked north of Kahurangi Point than south suggested that the Westland Current, a northwards- of it. Stanton noted a weal; subsurface salinity moving mean flow identified by Brodie (1960), was maximum just outside the shelf edge, and ascribed it a response to the south-westerly winds prevalent to a southward-going compensation current assoc- along the West Coast. Apart from the absence of this iated with the upwelling. He also commented on the current, Stanton's geostrophic flow agreed with the presence of slicks and banding parallel to the coast, earlier drogue and drift-card observations. The associated with internal waves in the highly stratified regional inflow from the west turned south about Shirtcliffe et al.—Cape Farev/ell upwelling plume dynamics 557 42°S, following the bathymetry along the flank of from a depth of about 50 m. Both in this survey and the Challenger Plateau, and an anticyclonic eddy the previous one, numerous isolated patches of cold appeared to occupy the shallowest part of the water were found in Taranaki Bight, and Bowman et Plateau. al. (1983c) discussed the possible origin of these By 1979 it had become clear that the northern "eddies" in terms of a barotropic numerical model. West Coast of the South Island was biologically They concluded that upwelling at Kahurangi Shoals important. Indeed, Bradford & Roberts (1978) had was caused mainly by bottom Ekman pumping, that shown that the Karamea Bight - Taranaki Bight - tidal mixing probably contributed, and that centrifugal Cook Strait area was the most extensive of only four effects were insignificant. They estimated that the New Zealand coastal regions in which zooplankton typical wavelength and phase speed of meanders in biomass exceeded 300 mg m~3. A cruise of RV the plume, 28 km and 0.4 m s"1, respectively, indicated Tangaroa in June 1979 led to several papers (Bradford a period close to the inertial period, suggesting that 1983; Chang 1983; MacKenzie & Gillespie 1984; the eddies were formed by wind-induced fluctuations Chang & Bradford 1985). Three transects were of the intensity of the Westland Current. Pointing out studied, off Cape Foulwind, Greymouth (42°30'S, that the spin-down time of such eddies should be less 171°10'E) and Wanganui Bluff(43°02'S, 170°25'E). than 1 day, they concluded that their lifetime of 10- Some upwelling was evident from a depth of 75 m to 15 days showed that rotation was being maintained the surface at the inshore station off Wanganui Bluff, by the conversion of potential to kinetic energy; but it with down welling below 150 m depth; the other should be noted that in spite of a maximum tangential transects showed neither upwelling nor down wclling. velocity of 0.8 m s"1 being estimated from the The winds were strong from the south-west before isopycnal slopes in one eddy, there has been no the Greymouth section, strong from the north-east demonstration of closed trajectories in these flows. during that section, moderate from the westerly quarter The picture that is presented in these two studies during the Westport section, and increased to strong is of a persistent Westland Current leading to persistent south-westerlies during the Wanganui Bluff section. upwelling at Kahurangi Shoals, with the production Taken with the suggestion of Stanton (1976) of cold-core eddies resulting from modulation of the concerning the importance of the south-westerly wind process by wind. This picture is inconsistent with to the existence of the Westland Current, these results earlier studies which showed that the Westland suggest that the tendency to upwelling in this region Current and the upwelling are both intermittent might also represent a, rather rapid, response to such phenomena, but it seems quite possible that the time winds. This would be consistent with the classical scale of this intermittency is rather long. picture of upwelling resulting from an offshore surface Further information was obtained during a Ekman transport, the Westiand Current being set up succeeding cruise of HMNZS Tui in February 1981 to balance, the surface stress by bottom friction. (Foster & Battaerd 1985). The survey began in light A detailed summer survey was carried out from winds. A plume of upwelled water stretched into RV Tangaroa in January/February 1980 (Bowman et Taranaki Bight, but the lowest surface temperature of al. 1983a, 1983b; Bradford et al. 1986). Upwelling 14°C was found just south of Kahurangi Point. The was observed at Cape Farewell, and ascribed to bottom following day this had gone, and the coldest water friction acting on the Westland Current, reinforced was 15°C over Paturau Bank.
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