Further studies of temporal coherence in North Pacific Sea surface temperatures

Namias, Jerome; Born, Robert M.

doi:10.1029/jc079i006p00797

Cited by 81 publications

(56 citation statements)

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“…Overall, the SSTA shows continuous decreases (increases) in the positive (negative) non-WWR years without WWR (Figure 2c and 2d). Thus, the differences between 1951, 1956, 1965, 1966, 1968, 1971, 1974Negative 1959, 1960, 1977, 1978, 1983, 1985, 1986, 1994, 1996, 1998, 1999Non-WWR Positive 1950, 1952, 1953, 1954, 1955, 1957, 1962, 1963, 1967, 1969, 1972, 1976, 1982, 1989, 1990, 1991, 1993, 2000, 2002Negative 1958, 1961, 1964, 1970, 1973, 1975, 1979, 1980, 1981, 1984, 1987, 1988, 1992, 1995, 2001…”

Section: Methodsmentioning

confidence: 99%

Winter‐to‐winter recurrence and non‐winter‐to‐winter recurrence of SST anomalies in the central North Pacific

Zhao¹,

Li²

2012

J. Geophys. Res.

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[1] All previous studies of the winter-to-winter recurrence (WWR) of sea surface temperature anomalies (SSTA) have focused on mean climatic characteristics. Here, interannual variability of the SSTA WWR in the central North Pacific (CNP) is studied. The SSTA WWR displays a strong interannual variability in the CNP. The relative roles of atmospheric forcing and the oceanic reemergence mechanism are investigated by comparing SSTA WWR years and non-WWR years. Oceanic reemergence mechanism operates every year, the SSTA in the following winter, however, depends not only on the oceanic entrainment but also the atmospheric forcing, which exhibits substantial interannual variability. During SSTA WWR years, atmospheric circulation anomalies also exhibit the WWR phenomenon. Atmospheric forcing as well as the oceanic reemergence mechanism can act synergistically to create SSTA in the following winter with the same sign. During SSTA non-WWR years, winter atmospheric circulation anomalies do not recur in the following winter, and the following winter has opposing atmospheric forcing on SSTA. Although the reemergence mechanism is likely still operating, the anomalous heating supplied by the oceanic reemergence mechanism is smaller than that coming through the atmospheric forcing. Overall, the WWR in the CNP is an evolutional characteristic of the whole air-sea system with the seasons, and the WWR of atmospheric circulation anomalies and its forcing play an important role in the SSTA WWR.Citation: Zhao, X., and J. Li (2012), Winter-to-winter recurrence and non-winter-to-winter recurrence of SST anomalies in the central North Pacific,

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Section: Methodsmentioning

confidence: 99%

Winter‐to‐winter recurrence and non‐winter‐to‐winter recurrence of SST anomalies in the central North Pacific

Zhao¹,

Li²

2012

J. Geophys. Res.

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“…5;Namias andBorn 1970, 1974). This process, referred to as the ''reemergence mechanism'' (Alexander and Deser 1995), occurs when temperature anomalies that form at the surface and spread throughout the deep winter ML remain beneath the ML when it shoals in spring.…”

Section: E Reemergence Mechanismmentioning

confidence: 99%

Role of the Gulf Stream and Kuroshio–Oyashio Systems in Large-Scale Atmosphere–Ocean Interaction: A Review

Alexander²,

et al. 2010

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Ocean-atmosphere interaction over the Northern Hemisphere western boundary current (WBC) regions (i.e., the Gulf Stream, Kuroshio, Oyashio, and their extensions) is reviewed with an emphasis on their role in basin-scale climate variability. SST anomalies exhibit considerable variance on interannual to decadal time scales in these regions. Low-frequency SST variability is primarily driven by basin-scale wind stress curl variability via the oceanic Rossby wave adjustment of the gyre-scale circulation that modulates the latitude and strength of the WBC-related oceanic fronts. Rectification of the variability by mesoscale eddies, reemergence of the anomalies from the preceding winter, and tropical remote forcing also play important roles in driving and maintaining the low-frequency variability in these regions. In the Gulf Stream region, interaction with the deep western boundary current also likely influences the low-frequency variability. Surface heat fluxes damp the low-frequency SST anomalies over the WBC regions; thus, heat fluxes originate with heat anomalies in the ocean and have the potential to drive the overlying atmospheric circulation. While recent observational studies demonstrate a local atmospheric boundary layer response to WBC changes, the latter's influence on the large-scale atmospheric circulation is still unclear. Nevertheless, heat and moisture fluxes from the WBCs into the atmosphere influence the mean state of the atmospheric circulation, including anchoring the latitude of the storm tracks to the WBCs. Furthermore, many climate models suggest that the large-scale atmospheric response to SST anomalies driven by ocean dynamics in WBC regions can be important in generating decadal climate variability. As a step toward bridging climate model results and observations, the degree of realism of the WBC in current climate model simulations is assessed. Finally, outstanding issues concerning oceanatmosphere interaction in WBC regions and its impact on climate variability are discussed.

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“…These changes in mixing are clearly associated with prolonged changes in the flux of atmospheric momentum to the ocean (stronger wind mixing after the shift). But they are also due to changes in the temperature of the fluid underlying the mixed layer, because the pool of cool water beneath the mixed layer can provide a thermal memory of previous winters (Namias and Born, 1974).…”

Section: The Mid-pacific Shiftmentioning

confidence: 99%