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VOLUME 19 JOURNAL OF PHYSICAL OCEANOGRAPHY NOVEMBER 1989A Quasi-geostrophic Circulation Model of the Northeast Pacific.Part II: Effects of Topography and Seasonal Forcing PATRICK F. CUMMINS*Institute of Ocean Sciences, Sidney, British Columbia, Canada(Manuscript received l0 November 1988, in final form 23 March 1989)ABSTRACT A quasi-geostrophic regional model of the northeast Pacific is used to investigate the
VOLUME 19 JOURNAL OF PHYSICAL OCEANOGRAPHY NOVEMBER 1989A Quasi-geostrophic Circulation Model of the Northeast Pacific.Part II: Effects of Topography and Seasonal Forcing PATRICK F. CUMMINS*Institute of Ocean Sciences, Sidney, British Columbia, Canada(Manuscript received l0 November 1988, in final form 23 March 1989)ABSTRACT A quasi-geostrophic regional model of the northeast Pacific is used to investigate the
Greenland low-pressure atmospheric cells between summer and winter ( Bakun and Nelson 1991 ). Similarly, Pingree et al. (1999) were able to partially relate observed flow reversals in the vicinity of Goban Spur to seasonal changes in the mean wind stress as well as in the large-scale oceanic density structure. This study aims at evaluating the relative effects of local wind stress and seasonal changes in the large-scale density structure of the northeastern Atlantic Ocean on the variability of the
Greenland low-pressure atmospheric cells between summer and winter ( Bakun and Nelson 1991 ). Similarly, Pingree et al. (1999) were able to partially relate observed flow reversals in the vicinity of Goban Spur to seasonal changes in the mean wind stress as well as in the large-scale oceanic density structure. This study aims at evaluating the relative effects of local wind stress and seasonal changes in the large-scale density structure of the northeastern Atlantic Ocean on the variability of the
primary objective of this paper is to illustrate the seasonal variation in the ocean’s response to upwelling-favorable wind stress. To establish the context for this analysis and define the “seasons,” the 3-yr time series of wind speed, 10-m current, and temperature at several depths are provided ( Fig. 3 ). Spring was defined as the time from the spring transition to when the upwelling jet separated from the coast. The time of the spring transitions was established primarily from the surface wind
primary objective of this paper is to illustrate the seasonal variation in the ocean’s response to upwelling-favorable wind stress. To establish the context for this analysis and define the “seasons,” the 3-yr time series of wind speed, 10-m current, and temperature at several depths are provided ( Fig. 3 ). Spring was defined as the time from the spring transition to when the upwelling jet separated from the coast. The time of the spring transitions was established primarily from the surface wind
this interaction contributes to the flow of various length scales. An example of this limited understanding is well illustrated in the Subtropical Countercurrent (STCC) bands of the South and North Pacific Oceans. In these bands of the wind-driven subtropical gyres, elevated eddy kinetic energy (EKE) level has been observed to modulate seasonally with an EKE peak appearing in the local spring season: April–May in the North Pacific STCC band and November–December in the South Pacific STCC band (see
this interaction contributes to the flow of various length scales. An example of this limited understanding is well illustrated in the Subtropical Countercurrent (STCC) bands of the South and North Pacific Oceans. In these bands of the wind-driven subtropical gyres, elevated eddy kinetic energy (EKE) level has been observed to modulate seasonally with an EKE peak appearing in the local spring season: April–May in the North Pacific STCC band and November–December in the South Pacific STCC band (see
the anomaly to denser regions through diapycnal fluxes. While previous studies have revealed a number of interesting features of SPESTMW, as described above, a full picture of SPESTMW that integrates all these features, including the seasonal evolution of its spatial extent and properties, has not yet been presented. This is because the data available to previous studies were spatially and temporally limited. For example, the vigorous vertical diffusion of the temperature–salinity anomaly
the anomaly to denser regions through diapycnal fluxes. While previous studies have revealed a number of interesting features of SPESTMW, as described above, a full picture of SPESTMW that integrates all these features, including the seasonal evolution of its spatial extent and properties, has not yet been presented. This is because the data available to previous studies were spatially and temporally limited. For example, the vigorous vertical diffusion of the temperature–salinity anomaly
1. Introduction The fine sediment distribution in estuaries is strongly influenced by the effects of climate change, such as accelerated sea level rise and intensified river discharge (e.g., Scavia et al. 2002 ; Robins et al. 2016 ; Achete et al. 2017 ), and human interventions, such as land reclamation, channel deepening, and channelization (e.g., de Jonge 1983 ; Winterwerp and Wang 2013 ; de Jonge et al. 2014 ; van Maren et al. 2015 ). In turn, the sediment distribution impacts the
1. Introduction The fine sediment distribution in estuaries is strongly influenced by the effects of climate change, such as accelerated sea level rise and intensified river discharge (e.g., Scavia et al. 2002 ; Robins et al. 2016 ; Achete et al. 2017 ), and human interventions, such as land reclamation, channel deepening, and channelization (e.g., de Jonge 1983 ; Winterwerp and Wang 2013 ; de Jonge et al. 2014 ; van Maren et al. 2015 ). In turn, the sediment distribution impacts the
to the equator. Their results agreed well with observations in the upstream region of the island but not in the downstream region. White (1971a) considered both nonlinearity and the rotational effects in his steady barotropic model, in which uniform background zonal flow hits a circular island. He referred to the resulting wake as a Rossby wake to distinguish it from a von Kármán wake ( von Kármán 1911 ). The idea of the Rossby wake is suggestive, but it is unlikely for his theory to be
to the equator. Their results agreed well with observations in the upstream region of the island but not in the downstream region. White (1971a) considered both nonlinearity and the rotational effects in his steady barotropic model, in which uniform background zonal flow hits a circular island. He referred to the resulting wake as a Rossby wake to distinguish it from a von Kármán wake ( von Kármán 1911 ). The idea of the Rossby wake is suggestive, but it is unlikely for his theory to be
that stable antisymmetric inertial subgyres appeared for some wind stress strengths and can be explained by an analytical modon solution. Thus far, most studies of double gyres using middle-range complexity have been conducted under constant (time independent) wind forcing. In the real atmosphere and oceans, seasonal wind forcing with westerly and trade winds generates subtropical and subpolar gyres arising from western boundary currents and internal currents. Recently, Sakamoto (2006) showed
that stable antisymmetric inertial subgyres appeared for some wind stress strengths and can be explained by an analytical modon solution. Thus far, most studies of double gyres using middle-range complexity have been conducted under constant (time independent) wind forcing. In the real atmosphere and oceans, seasonal wind forcing with westerly and trade winds generates subtropical and subpolar gyres arising from western boundary currents and internal currents. Recently, Sakamoto (2006) showed
MAB is supplied from high latitudes throughout the year ( Linder et al. 2004 ), whereas COW is observed only from January to April ( Kono et al. 2004 ; Oguma et al. 2008 ). Although seasonal variations of the COW distribution and CO have been reproduced in a western North Pacific GCM to some extent, mechanisms controlling the variations have not been discussed thoroughly ( Nakamura et al. 2003 ). Our approach to the problems about dynamics of the Coastal Oyashio and its seasonal variation is to
MAB is supplied from high latitudes throughout the year ( Linder et al. 2004 ), whereas COW is observed only from January to April ( Kono et al. 2004 ; Oguma et al. 2008 ). Although seasonal variations of the COW distribution and CO have been reproduced in a western North Pacific GCM to some extent, mechanisms controlling the variations have not been discussed thoroughly ( Nakamura et al. 2003 ). Our approach to the problems about dynamics of the Coastal Oyashio and its seasonal variation is to
JUNE 1985 DAVID L. T. ANDERSON AND ROBERT A. CORRY 773Seasonal Transport Variations in the Florida Straits: A Model StudyDAVID L. T. ANDERSON AND ROBERT A. CORRYDepartment of Atmospheric Physics, Oxford University, England(Manuscript received 16 July 1984, in final form 2 February 1985)ABSTRACT In a previous study Anderson and Corry used a wind-driven two-layer model to study the effects oftopography and islands on
JUNE 1985 DAVID L. T. ANDERSON AND ROBERT A. CORRY 773Seasonal Transport Variations in the Florida Straits: A Model StudyDAVID L. T. ANDERSON AND ROBERT A. CORRYDepartment of Atmospheric Physics, Oxford University, England(Manuscript received 16 July 1984, in final form 2 February 1985)ABSTRACT In a previous study Anderson and Corry used a wind-driven two-layer model to study the effects oftopography and islands on
