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Residual Flows in Cook Strait, a Large Tidally Dominated Strait

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Residual Flows in Cook Strait, a Large Tidally Dominated Strait 1654 JOURNAL OF PHYSICAL OCEANOGRAPHY VOLUME 44 Residual Flows in Cook Strait, a Large Tidally Dominated Strait CRAIG STEVENS Marine Physics Group, National Institute for Water and Atmospheric Research, Wellington, and Department Physics, University of Auckland, Auckland, New Zealand (Manuscript received 20 February 2013, in final form 19 February 2014) ABSTRACT Flows at subtidal frequencies are resolved from 20 months of current observations at multiple sites across 2 the narrows of Cook Strait, New Zealand. The substantial tidal flows (spring tides .3ms 1) are challenging to 2 measure with moored ADCPs. Along-strait residual flows are on the order of 0.05–0.1 m s 1, but there were differences across the strait and also through the annual cycle. The calculated net residual transport is 20.25 2 Sverdrups (Sv; 1 Sv [ 106 m3 s 1) (i.e., negative sign implies to the south, from Tasman Sea to Pacific Ocean). This is smaller (by a factor of 2–3) than that estimated from previous sparse current measurements. Crucially, however, these new data also suggest that, over the austral summer–autumn period, there is persistent re- sidual flow northward on the western side of the strait so that the summer–autumn net 20.15-Sv flow can be separated into 10.065-Sv westside and 20. 22-Sv eastside flow. This western northward flow had a seasonal bias, appearing only in the summer–autumn period. The observations also show persistent temperature stratification on the order of 28C over the full depth of the water column in this late summer–autumn period. An implication is that there is vertical shear influencing the residual flow estimates. A range of exchange flow scenarios are considered with the most extreme indicating that the flow on the western side of the strait in the January–June period might be as much as 10.08 Sv northward. This has substantial implications for regional circulation as well as for the nutrient supply for the nearby Marlborough Sounds. 1. Introduction the eastward transport around the north [9 Sverdrups 2 (Sv; 1 Sv [ 106 m3 s 1)] and south (8 Sv) bounds of the Subtidal flows dominate the transport of materials main islands of New Zealand have been estimated that influence large-scale processes like ecosystem pro- (Roemmich and Sutton 1998; Sutton 2003), there is duction and climate variability. The challenge is to re- a third pathway for exchange. Cook Strait, the channel solve these modest residual flow speeds from often much separating New Zealand’s North and South Islands, larger tidal flows. This can be especially difficult when connects the eastern Tasman Sea (TS) to the western coastal topography introduces variability in flow struc- Pacific at 428S. At its narrowest point it is 22 km across, ture that can be asymmetric, causing rectification of tidal with 210- and 350-m average and maximum depths, re- transport (Loder 1980). In addition, wind forcing pro- spectively (Fig. 1). Its fast-flowing tidal currents have vides an episodic, and likely seasonal, driver of exchange been the focus of a number of studies, amongst which (Knutsen et al. 2005; Rossby et al. 2005). Finally, baro- the most notable conclusion was that the dominating clinicity and rotation can lead to complex and variable semidiurnal tide is around 1408 out of phase at the op- exchange flows (e.g., Umlauf and Arneborg 2009; Ott posite ends (north vs south) of the strait (Heath 1978; and Garrett 1998). Vennell 1994; Stanton et al. 2001). This phase difference New Zealand bisects the subtropical convergence 2 drives substantial flows, reaching as high as 3.4 m s 1 zone with warm waters arriving from the north via the during spring tides (Vennell and Collins 1991; Stevens East Australia Current and cooler water from the south et al. 2012). separating from the Antarctic Circumpolar Current. While The strait is nominally around 40 km ‘‘long’’ (Vennell 1998) so that even at the maximum flow speed described above, a parcel of fluid travels around 44 km in half Corresponding author address: Craig Stevens, Marine Physics Group, National Institute for Water and Atmospheric Research, a semidiurnal tidal cycle and so is only just exported Greta Point, 301 Evans Bay, Kilbirnie, Wellington 6021, New Zealand. through the strait in a single tidal period. Despite this, E-mail: [email protected] there has been little focus on residual currents and net DOI: 10.1175/JPO-D-13-041.1 Ó 2014 American Meteorological Society Unauthenticated | Downloaded 09/27/21 02:11 AM UTC JUNE 2014 S T E V E N S 1655 FIG. 1. (a) New Zealand and the TS and Southern Ocean (SO) and regional circulation including the East Auckland Current (EAucC) , DC, SC, as well as the WE. (b) Cook Strait narrows is bounded by Cape Terawhiti (CT) to the east and the headlands of the (shaded) MS to the west. The 200- and 400-m depth contours are marked, as well as the shoal at FR. Meteorological data come from the BI and MI. The locations of the four moorings (E, W, FR, and C) are marked. The dashed line is the power cable exclusion zone (CEZ). (c) The depth profile across the narrows with measurement locations marked and the proportional cross-sectional area as a function of depth shown as an inset. The cross section is divided into areas as discussed in the text. transport in the strait, an exception being the study of Sea is relatively quiescent in terms of circulation currents Heath (1986) using rotor-based current meters. (Sutton et al. 2005) that form the oceanic boundary for Transport through Cook Strait plays a role in influ- the shelf seas of the west coast of the South Island. By encing upper water column ocean circulation in the most accounts (Heath 1971; Chiswell and Stevens 2010), central New Zealand region. The eastern central Tasman a northward coastal flow along the west coast of the Unauthenticated | Downloaded 09/27/21 02:11 AM UTC 1656 JOURNAL OF PHYSICAL OCEANOGRAPHY VOLUME 44 TABLE 1. Residual speed and volume transport estimates from previous work where negative implies southward transport. The volumetric transport estimates were made here and not by the original authors (except where noted by an asterisk). 2 Study Speed (m s 1) Flow (Sv ) Notes Heath (1971) From 20.12 to 20.25 From 20.6 to 21.2 Speed identified using geostrophic balance Bowman et al. (1980) 20.3 21.2 Residual from numerical tidal model Heath (1986) From 20.01 to 20.03 From 20.04 to 20.14 60-day rotor-based current-meter deployment Vennell (1994) From 20.25 (west) to ;0 (east) 20.6 12-h ADCP survey Chiswell (2000) 20.14 20.8* Inferred from conservation of mass Walters et al. (2010) n/a 20.61* Baroclinic numerical model northern half of the South Island (Stanton and Moore effects. Crucially, from the present paper’s perspective, 1992) forms the upstream supply for Cook Strait. This Heath (1986) noted an east–west difference in direction, flow evolves into the d’Urville Current (DC) that moves whereby he found the water in the western zone of the 2 northeast around Farewell Spit and then across to the narrows moving southward (3 cm s 1), but the current west coast of the southern tip of the North Island where it on the eastern side of the strait was found to be moving 2 turns southward (Bowman et al. 1983a; Chiswell and northward (5–15 cm s 1)—as will be seen, this is the Stevens 2010). On the central east coast of New Zealand, opposite to that found in the present work. transport is mainly associated with Wairarapa Eddy Vennell and Collins (1991) deployed month-long (WE) currents containing mainly subtropical water, plus acoustic Doppler current profiler (ADCP) moorings, some sporadic influence from the Southland Current (SC; concentrated to the east of the strait, but their analysis Chiswell 2000). Exchange between the three systems high-pass filtered the currents to focus on tides. Sub- (west coast, east coast–south, and east coast–north, where sequently, Vennell (1994) used vessel-based ADCP data 2 north and south refer to a dividing line at the strait latitude) to estimate residual flows ranging up to 25 cm s 1 to the affects a number of ecosystems and industries including the south and with an east–west bias (larger southward flow economically important Marlborough Sounds (MS; aqua- on the western side of the strait). Chiswell (2000) used culture, forestry, and tourism) and the Kaikoura canyon a mass balance approach to suggest the net residual 2 region (fisheries and tourism). flow (to the south) through the strait is 14 cm s 1 Olsson (1955) and Gilmour (1960) presented esti- (20.8 Sv). This latter value is comparable to the south- mates of flow in the strait using a combination of ap- ward 20.61 Sv estimated for zero wind conditions by proaches including cross-strait cable electrical potential, Walters et al. (2010) in a modeling study that included aerial tracking of surface dye, ship measurements, and Tasman–Pacific sea level differences and regional baro- bottom-mounted current meters. Unfortunately, the clinic gradients. 5-month monitoring of cable electrical potential differ- The wide range of conclusions based on often dis- ence indicated that the technique, while able to capture parate short-duration observations motivated a ;2-yr the tides, was not sensitive enough to measure flow re- ADCP deployment, providing the longest (by a factor of sidual. ;4) flow record in the strait. The objective here is to Previous estimates of residual flow in the strait are examine residual flows through the strait using this re- summarized in Table 1.
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