The Large, Westward-Propagating Haida Eddies of the Pacific Eastern

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Deep-Sea Research II 52 (2005) 845–851 www.elsevier.com/locate/dsr2 Editorial The large, westward-propagating Haida Eddies of the Paciﬁc easternboundary

1. The Haida Eddies et al., 2002). Di Lorenzo et al. (2005) show that they are likely a result of buoyant plumes flowing The easternNorth Pacific eddies that we now out of Hecate Strait around Cape St. James at the call Haida Eddies were first identified in the mid- southerntip of the islands. These small plumes 1970s by Kirwanet al. (1978) who noted antic- first create small anticyclonic eddies that then yclonic loops in drogued drifter tracks. Several of merge to form the Haida Eddies. the features that Tabata (1982) described in The resulting large anticyclonic eddies (see cover historical hydrographic data from the Northeast of this volume) are 150 to 300 km indiameter, with Pacific, as well as other eddies occasionally sea-surface height anomalies up to 40 cm, and identified in drifter observations (Thomsonet al., generally track westward into the North Pacific (a 1990; PaduanandNiiler, 1993 ) and satellite data direction opposing the local surface currents) at (ThomsonandGower, 1998 ), were most likely speeds up to 2 cm/s (Crawford and Whitney, 1999; Haida Eddies but were not identified as such. The Crawford et al., 2002; Whitney and Robert, 2002; possible importance of these eddies was not Crawford et al., 2005). Rotational speeds of more recognized until 1998, when a correlation was first than30 cm/s have beenobserved withinthese drawnbetweensatellite observationsof these eddies, based ondrogued drifters andADCP mesoscale features and anomalous ship-board measurements (Yelland and Crawford, 2005). measurements (see Section 3, below). Dramatic Eddy core waters with distinctly coastal tempera- deviations from what is considered ‘normal’ ture, salinity, and biogeochemical signals (which hydrography, biology, and chemistry for the are also identified with spreading between iso- open-ocean waters of the eastern North Pacific pycnals, Fig. 2) generally extend only between have been encountered occasionally throughout 150 m (the maximum depth of winter mixing) and the history of the time series maintained in 600 m (Whitney and Robert, 2002), although associationwith OceanStationP (50 1N, 1451W; isopycnals beneath the eddies are depressed at e.g. Tabata, 1965; Wong et al., 1999), but these least to 2000 m (Crawford, 2005). Throughout this anomalous observations defied explanation and special issue, we reserve the term ‘core’ to describe were rarely published. Inretrospect, we cannow the subsurface waters that remaindistinctfrom the see that many of those strange data could have surrounding waters, while using the term ‘center’ been from serendipitous sampling of Haida Eddies whendiscussingthe surface waters withinaneddy, (Whitney and Robert, 2002). which are more subject to horizontal exchange and The Haida Eddies form off Haida Gwaii (the relatively rapidly acquire the characteristics of the QueenCharlotte Islands)alongthe coast of British surrounding waters (Chierici et al., 2005; Johnson Columbia during late winter (Fig. 1; Crawford et al., 2005; Mackas et al., 2005; Petersonet al.,

846 Editorial / Deep-Sea Research II 52 (2005) 845–851

58 (Whitney and Robert, 2002), oftencrossingthe 1451W meridian(e.g. Onishi et al., 2000). 56

Haida Gwali 54 Hecate Strait 2. Prevalence of anticyclonic eastern boundary Bowie Seamount eddies

Latitude, N Latitude, 52 British Columbia At least one Haida Eddy forms each year, and

50 Juan de the amount of coastal water a single eddy carries Fuca Strait 3 Station P offshore is anywhere from 3000 to 6000 km (Whitney and Robert, 2002), the volumes of Lakes 48 150 145 140 135 130 125 120 Victoria and Michigan, respectively. Years with Longitude, W very strong El Nin˜ o events, which generate Fig. 1. The easternNorth Pacific regionwhere Haida Eddies exceptionally high winter sea levels along the coast occur. Contour lines are at 200, 500 m, and then every 1000 m of British Columbia, appear to produce more thereafter, downto 4000 m. eddies (Melsom et al., 1999; Crawford, 2002), which are also larger and persist longer than those formed at other times. Haida-1998 is the best- studied example of such an‘El Nin˜ o eddy’ to date (Crawford and Whitney, 1999; Crawford et al., 2002; Whitney and Robert, 2002). The association between strong, persistent Haida Eddies and El Nin˜ o could provide some interesting climate change feedbacks, if increasing frequency of los Nin˜ os were to increase the mixing rates between coastal and open ocean waters (Crawford, 2005; Petersonet al., 2005 ; Tsurumi et al., 2005; Whitney et al., 2005). While the Haida Eddies are the only eastern boundary anticyclonic eddies in which the ecology and biogeochemistry have been examined over an extended period, similar anticyclonic features have beenobserved at the easternboundaries of all the oceans, implying that the mixing and transport processes associated with the Haida Eddies could have a global significance. Just within the eastern North Pacific, the Sitka Eddies (Tabata, 1982) are similar to the Haida Eddies but form farther north (off the Alaska Panhandle), apparently by a Fig. 2. Hydrographic sectionthrough the Haida-2000 eddy, different mechanism. Okkonen et al. (2003) also along 136.21W inSeptember, 2000. Contoursare st at intervals have identified eddies that form in the extreme of 0.2, and dotted lines show cast locations and depths. Black northern Gulf of Alaska, near Yakutat, and drift triangle at 53.51N represents Hodgkins seamount. mainly in the Alaskan Stream. This proximity to the continental shelf allows the Yakutat Eddies to exchange deep-sea and coastal waters even more 2005; Tsurumi et al., 2005). Using satellite efficiently than Haida or Sitka eddies. In addition, altimetry, Haida Eddies have beentracked un- a number of detailed short-term studies of large, ambiguously out as far as 1000 km from the coast anticyclonic eddies have been conducted in the ARTICLE IN PRESS

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North Atlantic, and incidental sampling in the Eddies, indicating that they may also have South Atlantic, Indian, and South Pacific Oceans extended, subsurface life. has identified similar features (note that these Although not a westward propagating eddy southern-hemisphere eddies have counter-clock- originating at the eastern margin, the PRIME wise, not clockwise, circulation). In particular, eddy (Martinet al., 1998 ; Savidge and Williams, Hamon(1972) saw geostrophic highs resembling 2001) was another important example of an anticyclonic eddies in the Indian Ocean off the intensively studied anticyclonic eddy. Located at westerncoast of Australia as early as 1965, andthe about 601N inthe North Atlantic (south of presence of anticyclonic eddies in these waters was Iceland) in 1996, the PRIME eddy was chosen as confirmed by drogued drifters in 1976 (Cresswell, the site of a June ecosystem study, because it was 1977). assumed that its internal water mass was effec- The first systematic study of aneddy, the tively isolated from mixing with the surrounding Tourbillon experiment in the Mediterranean out- waters. As a part of the study, the eddy was flow region of the North Atlantic during the injected with an SF6 tracer inorder to confirmthe autumnof 1979, occupied aneddy that was about integrity of its core waters, leading to some of the 50 km in diameter and moving northwestward at more valuable analyses of mixing in and around almost 10 cm/s (Le Groupe Tourbillon, 1983). The anticyclonic eddies available (Law et al., 2001; study employed anarray of moored current Martinet al., 2001 ; MartinandRichards, 2001 ). meters, as well as repeated CTD transects, and Similarly, the Gas-Ex eddy at about 461N, 21.51W produced a very detailed understanding of how the was the site of an investigation into air-sea gas Tourbilloneddy effectively mixed Mediterranean exchange processes that was not specifically and Atlantic waters, including estimates of diffu- designed to study eddy dynamics but provided a sion coefficients on both the horizontal and number of insights into the biogeochemistry of vertical scales (ArhanandColinde Verdie ` re, anticyclonic eddies, nonetheless (Hood et al., 2001; 1985; Colinde Verdiere et al., 1986 ). Zhang et al., 2001). Other westward-propagating, anticyclonic eddies observed inthe North Atlanticincludethe Meddies (McDowell and Rossby, 1978), which are 3. The Haida Eddy project deep (generally centered at about 1000 m) lenses of warm, saline Mediterranean water observed off During routine time series cruises in 1995 and the Bahamas, and a Swesty (Pingree, 1996), a 1998, scientists on board the CCGS John P. Tully shallow eddy that originated off the coast of North observed anomalous temperatures and salinities Africa and moved southwestward across the along a transect from the mouth of Juan de Fuca Atlantic during 1993–94 (we wish to note that Strait to OceanStationPapa (50 1N, 1451W, when Crawford and Whitney (1999) named the Fig. 1). Both times, the ship was able to return Haida Eddies, they refrained from using the term to the site of the anomalous observations and Heddies). Both the Meddies and the Swesties are conduct more detailed sampling before returning subsurface eddies, and the Meddies, which contain to port. Later, TOPEX and ERS-2 altimetry very dense water, likely originate from subsurface images provided by the Colorado Center for waters. Onthe other hand,the Swesty Eddy Astrodynamics Research (CCAR; Global Near contained water characteristic of surface waters Real-Time Sea Surface Anomly Data Viewer) in the eastern Atlantic near the Azores and still identified those anomalies as anticyclones of the had a faint temperature signal at the surface. type that are now called Haida Eddies (Whitney Similarly, while the Haida Eddies disappear from and Robert, 2002; Yelland and Crawford, 2005). altimetry maps after a couple of years, the routine Haida-1998 is still the largest Haida Eddy ob- time series cruises to StationP occasionally served to date. identify subsurface water masses that are consis- Based onthe data obtained from those oppor- tent with what we have seen in surface Haida tunistic samplings of Haida-1995 and Haida-1998, ARTICLE IN PRESS

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Table 1 Cruise dates and general sampling information for the Haida-2000 and Haida-2001 eddies

Dates No. of Stations Types of samples collected

Winter 2000 February 14–16 10 CTD, nutrients, chlorophyll, zooplankton, neustona, inorganic carbon Spring 2000 June 18–22 15 CTD, nutrients, chlorophyll, primary production, zooplankton, neustona, inorganic carbon, organic carbon, trace metals Fall 2000 September 26–29 12 CTD, nutrients, chlorophyll, primary production, zooplankton, neustona, inorganic carbon, organic carbon, trace metals

Winter 2001 February 16–20 9 CTD, nutrients, chlorophyll, zooplankton, neustona, inorganic carbon, organic carbon, trace metals

Spring 2001 June 2–13 39 CTD, nutrients, chlorophyll, primary production, zooplankton, neustona, inorganic carbon, organic carbon, trace metals Fall 2001 September 22–October 1 13 CTD, nutrients, chlorophyll, primary production, zooplankton, neustona, inorganic carbon, organic carbon, trace metals

aNeuston tows primarily targeted larval fish, meroplanktonic larvae, and micronekton. a comprehensive project was designed to study the offshore towards the northwest after forming but physical, biogeochemical, and ecological evolution thenstalled at Bowie Seamountinthe summer of of a Haida Eddy over two years, from formation 2000, remaining at almost the same location for at the coast through transport into the central nearly five months, until late 2000. Haida-2000 oligotrophic gyre of the North Pacific. Inantici- finally entered the High Nitrate-Low Chlorophyll pationof this project, a proto-eddy off Cape St. (HNLC) waters of the Gulf of Alaska sometime James was sampled inFebruary 2000. Eventually during the 2000/01 winter. In spring of 2001, a designated Haida-2000a (also called Haida-2000, small, new eddy (Haida-2001a), which had re- for simplicity), this eddy was resampled during five cently formed off northern Haida Gwaii, merged subsequent cruises, through September 2001 with Haida-2000 (Crawford et al., 2005), and the (Table 1). In2001, each cruise also sampled a biogeochemistry observed inHaida-2000 during new eddy (Haida-2001b), which was therefore 2001 was consistent with such an influx of fresh visited three times. Inadditionto CTD profiles, coastal water (Chierici et al., 2005; Johnson et al., dissolved oxygen, and macronutrients, the project 2005; Petersonet al., 2005 ). included detailed sampling of the zooplankton and After a more ambiguous beginning, the rela- phytoplankton communities (including primary tively small Haida-2001 migrated towards the productionmeasurements),dissolved organicmat- southwest, thereby avoiding the seamounts and ter and pigments, the inorganic carbon system, many of the complications observed in Haida-2000 and trace metals. The details of our cruises, (Crawford et al., 2005). Unfortunately, we mana- including sampling dates, locations, and activities, ged to sample Haida-2001 only three times, are at www-sci.pac.dfo-mpo.gc.ca/dsr2/. including February 2001, when we occupied a Crawford et al. (2005, Fig. 2) show how Haida- station that may or may not have been the nascent 2000 and Haida-2001 developed throughout the Haida-2001 but was quite likely at least represen- study. Haida-2000, which was of a size typical for tative of the waters from which the eddy eventually Haida Eddies (Crawford, 2005), moved rapidly formed. ARTICLE IN PRESS

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The zooplanktonic communities of the eddies water to the central gyre. Although we originally remained quite distinct from the surrounding saw these eddies as simply curious possible waters through much of the study (Mackas and explanations of some of the more dramatic short Galbraith, 2002; BattenandCrawford, 2005 ; time-scale variations observed in this area, we have Mackas et al., 2005; Tsurumi et al., 2005), now come to understand that they may be major strengthening the hypothesis that Haida Eddies contributors to the biological production of the are an important mechanism for transporting central North Pacific. organisms. On the other hand, Putland et al. (2004) found no difference between coccolitho- phore distributions or characteristics inside and outside the eddies, although that may have been Acknowledgments because their samples were only collected from the surface 10 m; Chierici et al. (2005); Johnson et al. First and foremost, we thank the Colorado (2005); Mackas et al. (2005); Petersonet al. (2005) Center for Astrodynamics Research; without their found that in many ways, the surface waters website of near real-time altimetry data, we could (mixed layer) of the eddies came to resemble not have done this project. We also thank the surrounding waters within a year. The subsurface captains and crews of the CCGS J.P. Tully, who core waters, however, remained geochemically were remarkably enthusiastic about our eddy- distinct and maintained their coastal water signals chasing and Joe Linguanti for his assistance in throughout the two years of our study. Thus, archiving the data and preparing the website, and through vertical mixing and diffusion, a Haida we acknowledge the support of the Fisheries and Eddy provides a continuous supply of nutrients Oceans Strategic Science Fund for our work on the and iron to the surface waters of the oligotrophic Haida-2000 and -2001 Eddies. LAM and WRC ocean( Johnson et al., 2005; Petersonet al., 2005 ), thank Dave Mackas for editorial handling of the Batten and Crawford manuscript. We also thank contributing to atmospheric CO2 drawdown (Chierici et al., 2005) for at least two years and all the reviewers who helped us evaluate and possibly for longer. improve the papers in this volume, often turning Inadditionto the data presented inthe papers their reviews around remarkably quickly. Finally, inthis volume andonthe associated website we thank John Milliman and Elsevier for support, (www.sci.pac.dfo-mpo.gc.ca/dsr2/), most of the encouragement, and patience. data from this project are archived at the Institute of Ocean Sciences (Fisheries and Oceans Canada, Sidney, BC) and can be obtained by contacting the References institute’s database manager. Arhan, M., Colin de Verdie` re, A., 1985. Dynamics of eddy motions in the eastern North Atlantic. Journal of Physical Oceanography 15, 153–170. 4. Epilogue Batten, S.D., Crawford, W.R., 2005. The influence of coastal origin eddies on oceanic plankton distributions in the Haida-2000 disappeared from the TOPEX/ easternGulf of Alaska. Deep-Sea Research II, this issue ERS-2 sea-surface height anomaly images by [doi:10.1016/j.dsr2.2005.02.009]. Chierici, M., Miller, L.A., Whitney, F.A., Johnson, W.K., November, 2002, somewhere inthe vicinityof Wong, C.S., 2005. Biogeochemical evolution of the carbon 551N, 1451W, while Haida-2001 remained identifi- dioxide system inthe waters of long-livedmesoscale eddies able until December, 2003, having last been in the northeast Pacific Ocean. Deep-Sea Research II, this observed at 521N, 1431W. Since we stopped issue [doi:10.1016/j.dsr2.2005.01.001]. visiting these two eddies, however, at least five Colin de Verdiere, A., Harvey, J.G., Arhan, M., 1986. Stirring and mixing of thermohaline anomalies. Journal of Marine more have beenspawnedfrom the British Colum- Research 44, 99–118. bian coast to journey into the open ocean, directly Crawford, W.R., 2002. Physical characteristics of Haida 3 contributing as much as 25,000 km of coastal Eddies. Journal of Oceanography 58, 703–713. ARTICLE IN PRESS

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SF6 tracer study of an anticyclonic eddy in the North anoverview. Deep-Sea Research II 48, 687–704. Atlantic: patch evolution, vertical mixing and nutrient Tabata, S., 1965. Variability of oceanographic conditions supply to the mixed layer. Deep-Sea Research II 48, at OceanStation‘‘P’’ inthe Northeast Pacific 705–724. Ocean. Transactions of the Royal Society of Canada 3, Le Groupe Tourbillon, 1983. The Tourbillon experiment: a 367–418. study of a mesoscale eddy inthe easternNorth Atlantic. Tabata, S., 1982. The anticyclonic, baroclinic eddy off Sitka, Deep-Sea Research 30 (5A), 456–511. Alaska, in the Northeast Pacific Ocean. Journal of Physical Mackas, D.L., Galbraith, M.D., 2002. Zooplankton distribu- Oceanography 12, 1260–1282. tion and dynamics in a North Pacific eddy of coastal origin: Thomson, R.E., Gower, J.F.R., 1998. A basin-scale oceanic 1. Transport and loss of continental margin species. Journal instability event in the Gulf of Alaska. Journal of of Oceanography 58, 725–738. Geophysical Research 103 (C2), 3033–3040. Mackas, D.L., Tsurumi, M., Galbraith, M.D., Yelland, D.R., Thomson, R.E., LeBlond, P.H., Emery, W.J., 1990. Analysis of 2005. Zooplankton distribution and dynamics in a North deep-drogued satellite-tracked drifter measurements in the Pacific eddy of coastal origin: II. Mechanisms of eddy Northeast Pacific. Atmosphere-Ocean28 (4), 409–443. colonization by and retention of offshore species. Deep-Sea Tsurumi, M., Mackas, D.L., Whitney, F.A., DiBacco, C., Research II, this issue [doi:10.1016/j.dsr2.2005.02.008]. Galbraith, M.D., Wong, C.S., 2005. Pteropods, eddies, Martin, A.P., Richards, K.J., 2001. Mechanisms for vertical carbonflux, andclimate variability inthe Alaska nutrient transport within a North Atlantic mesoscale eddy. Gyre. Deep-Sea Research II, this issue [doi:10.1016/ Deep-Sea Research II 48, 757–773. j.dsr2.2005.02.005]. ARTICLE IN PRESS

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Whitney, F., Robert, M., 2002. Structure of Haida Eddies and Zhang, J.-Z., Wanninkhof, R., Lee, K., 2001. Enhanced new their transport of nutrient from coastal margins into the NE production observed from the diurnal cycle of nitrate in an Pacific Ocean. Journal of Oceanography 58, 715–723. oligotrophic anticyclonic eddy. Geophysical Research Let- Whitney, F.A., Crawford, D.W., Yoshimura, T., 2005. The ters 28 (8), 1579–1582. uptake and export of silicon and nitrogen in HNLC waters of the NE Pacific. Deep-Sea Research II, this issue [doi:10.1016/j.dsr2.2005.02.006]. Wong, C.S., Whitney, F.A., Crawford, D.W., Iseki, K., Lisa A. Miller, Marie Robert, Matear, R.J., Johnson, W.K., Page, J.S., Timothy, D., 1999. Seasonal and interannual variability in particle fluxes William R. Crawford of carbon, nitrogen and silicon from time series of sediment Division of Ocean Science and Productivity, traps at OceanStationP, 1982–1993: relationship to Institute of Ocean Sciences, changes in subarctic primary productivity. Deep-Sea Re- Fisheries and Oceans Canada, P.O. Box 6000, search II 46 (11–12), 2735–2760. Sydney BC, Canada V8L 4B2 Yelland, D., Crawford, W.R., 2005. Currents in Haida Eddies. Deep-Sea Research II, this issue [doi:10.1016/ E-mail address: [email protected] j.dsr2.2005.02.010]. (L.A. Miller)