References

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References

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Figure: Silica at a potential density of 45.88 referenced to 4000 dbar. This is the density in kg which seawater has when moved adiabatically to 4000 dbar, minus 1000 kg m. This isopycnal lies at about 4500 meters depth. Northward extension of low silica from the southern hemisphere is seen in the western North Pacific. A stronger gradient in silica is seen along a nearly zonal line extending westward from the Hawaiian ridge. Low silica extends northward into the northern North Pacific along the axis of the deep trenches. Two large clockwise swirls of silica, seen in the tendency for silica to increase in a clockwise direction around the gyre, are apparent north and south of the strong gradient. These might suggest anticyclonic flow [ Talley and Joyce, 1992].

Figure 2: Adjusted steric height (10 m s) at 4000 dbar [from Reid, 1986]. Steric height is the anomaly in height of one isobaric surface relative to another. The horizontal gradient of Reid's values is the geostrophic flow with reference velocities adjusted so that flow matches the patterns of properties at all depths and conserves mass. Apparent are cyclonic circulation in the south-easternmost basin (Bellingshausen Basin), and anticyclonic flow in the central South Pacific. Reprinted with kind permission from Elsevier Sciences.

Figure: Potential temperature at a potential density of 36.96 referenced to 2000 dbar. This isopycnal lies at about 2500 meters depth. Two westward extending tongues of relatively warm water are seen on either side of the equator, with an eastward-extending tongue of cooler water just off the equator. The warmth of the westward plumes is probably due to the hydrothermal source at the East Pacific Rise [ Lupton and Craig, 1981]. Similarly zonal property signatures are seen in the Atlantic at similar latitudes, suggesting a common dynamical origin for deep flows in both oceans [ Talley and Johnson, 1994].

Figure 4: Abyssal transports determined from an inverse model. These show a net convergence of water into the westernmost boxes, indicating relatively larger upwelling near the western boundary than elsewhere. [ Roemmich and McCallister, 1989]. Reprinted with kind permission from Elsevier Sciences.

Figure 5: Average currents measured across the equator at 159W over a period of 18 months. The upper ocean current structure is the familiar pattern shown by Wyrtki and Kilonsky [1984]. Apparent are the set of stacked jets at the equator and a suggestion of westward flow off the equator on both sides, with greater vigor south of the equator Firing, 1987, 1989].

Figure 6: Difference in winter time sea-surface temperature (SST) for the periods 1977-1982 minus 1970-1976. This demonstrates the dominant mode of variability in SST in the northern North Pacific, associated with changes in the Aleutian Low pattern. The regime change in 1976 was towards colder SST in the central North Pacific and warmer SST in the eastern Alaskan gyre and eastern subtropics [ Miller et al., 1994].

Figure 7: Freshwater transport for the globe, showing the generally northward transport in the Pacific and southward in the Atlantic. The sign is determined entirely by the northward transport of fresh water through Bering Strait [ Wijffels et al., 1992].

Figure 8: Schematic of the global pathway of deep water renewal, based on direct transport estimates for the major layers at subtropical latitudes in each ocean basin. Latitudes of the estimates are listed at the top. Starting at the left side and moving to the right, one traces the intermediate water flowing northward, overturning into the deep water and flowing back southward (Atlantic), then northward into the Pacific near the bottom, upwelling in the North Pacific to a shallower deep layer and returning southward, then entering the Indian Ocean via the southern ocean and upwelling to the thermocline. [ Roemmich and McCallister, 1989]. Reprinted with kind permission from Elsevier Sciences.

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