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al. 1999 ; Iskandar et al. 2005 , 2006 ). 2) Theory and modeling Previous studies suggest that a possible explanation for the peak responses at both the 180- ( Jensen 1993 ; Han et al. 1999 ) and 90-day ( Han et al. 2001 ; Han 2005 ) periods is the establishment of basin resonance in the equatorial IO. Cane and Moore (1981) and Gent (1981) constructed low-frequency equatorial resonance modes in an idealized basin that consist of eastward-propagating Kelvin and westward-propagating, long
al. 1999 ; Iskandar et al. 2005 , 2006 ). 2) Theory and modeling Previous studies suggest that a possible explanation for the peak responses at both the 180- ( Jensen 1993 ; Han et al. 1999 ) and 90-day ( Han et al. 2001 ; Han 2005 ) periods is the establishment of basin resonance in the equatorial IO. Cane and Moore (1981) and Gent (1981) constructed low-frequency equatorial resonance modes in an idealized basin that consist of eastward-propagating Kelvin and westward-propagating, long
planetary waves mathematically is to decompose the midlatitude meridional wind field into its spectral components. Waves are characterized by their amplitude (north–south wind speed) and phase speed (velocity of west–east propagation) ( Rossby 1940 ; Charney and Eliassen 1949 ; Haurwitz 1940a ; Haurwitz 1940b ) and can interact with each other as well as with the background flow ( Frederiksen and Webster 1988 ). They can be subject to reflection, diffraction, dispersion, and resonance ( Hoskins and
planetary waves mathematically is to decompose the midlatitude meridional wind field into its spectral components. Waves are characterized by their amplitude (north–south wind speed) and phase speed (velocity of west–east propagation) ( Rossby 1940 ; Charney and Eliassen 1949 ; Haurwitz 1940a ; Haurwitz 1940b ) and can interact with each other as well as with the background flow ( Frederiksen and Webster 1988 ). They can be subject to reflection, diffraction, dispersion, and resonance ( Hoskins and
the internal wave fields are in phase and the conversion is enhanced when beams emitted from the opposing ridges superpose after one surface reflection during semidiurnal tides. The role of the beams in the resonance suggests that higher vertical modes may be important. Vlasenko et al. (2010) show with analytical 2D and numerical 3D simulations that the resonant interaction between the west and the east ridges enhances the generation of second-mode waves by the west ridge. Fig . 1. (a) Zonal
the internal wave fields are in phase and the conversion is enhanced when beams emitted from the opposing ridges superpose after one surface reflection during semidiurnal tides. The role of the beams in the resonance suggests that higher vertical modes may be important. Vlasenko et al. (2010) show with analytical 2D and numerical 3D simulations that the resonant interaction between the west and the east ridges enhances the generation of second-mode waves by the west ridge. Fig . 1. (a) Zonal
MARCH 1983 JOHN P. BOYD 459Second Harmonic Resonance for Equatorial Waves JOHN P. BOYDDepartment of Atmospheric and Oceanic Science, University of Michigan, Ann Arbor, 48109(Manuscript received 23 December 1981, in final form 17 September 1982)ABSTRACT Simple, exact analytical conditions for second harmonic resonance between equatorial waves are derived.Such resonance can
MARCH 1983 JOHN P. BOYD 459Second Harmonic Resonance for Equatorial Waves JOHN P. BOYDDepartment of Atmospheric and Oceanic Science, University of Michigan, Ann Arbor, 48109(Manuscript received 23 December 1981, in final form 17 September 1982)ABSTRACT Simple, exact analytical conditions for second harmonic resonance between equatorial waves are derived.Such resonance can
VOLUME23 JOURNAL OF PHYSICAL OCEANOGRAPHY SEPTEMBER 1993Inertial Resonance Induced by an Oceanic Jet P. KLEIN AND A. M. TREGUIERLaboratoire de Physique des Oceans, IFREMER, Plouzane, France(Manuscript received 5 August 1992, in final form 19 January 1993)ABSTRACT The dynamics of the mixed layer in the presence of an embedded geostrophic jet has been investigated usinga simple 1 l/2-1ayer model and a two
VOLUME23 JOURNAL OF PHYSICAL OCEANOGRAPHY SEPTEMBER 1993Inertial Resonance Induced by an Oceanic Jet P. KLEIN AND A. M. TREGUIERLaboratoire de Physique des Oceans, IFREMER, Plouzane, France(Manuscript received 5 August 1992, in final form 19 January 1993)ABSTRACT The dynamics of the mixed layer in the presence of an embedded geostrophic jet has been investigated usinga simple 1 l/2-1ayer model and a two
1. Introduction Models and, to some extent, observations show that isolated islands and seamounts can be the site of resonant trapped wave responses at subinertial frequencies (e.g., Longuet-Higgins 1969 ; Hogg 1980 ; Brink 1989 ; Brink 1999 ). The continental shelf literature (e.g., Dale and Sherwin 1996 ) makes it natural to ask whether there might also be resonances, or leaky resonances, at superinertial frequencies [e.g., Chambers (1965) ; Longuet-Higgins (1967) for very idealized
1. Introduction Models and, to some extent, observations show that isolated islands and seamounts can be the site of resonant trapped wave responses at subinertial frequencies (e.g., Longuet-Higgins 1969 ; Hogg 1980 ; Brink 1989 ; Brink 1999 ). The continental shelf literature (e.g., Dale and Sherwin 1996 ) makes it natural to ask whether there might also be resonances, or leaky resonances, at superinertial frequencies [e.g., Chambers (1965) ; Longuet-Higgins (1967) for very idealized
I AuGUSTI985 HERSCHEL L. MITCHELL AND JACQUES DEROME 1653Resonance of Topographically Forced Waves in a Quasi-Geostrophic Model HERSCHEL L. MITCHELL Recherche en Prdvision Num~rique, Atmospheric Environment Service, Dorval, Quebec, H9P 1J3, Canada JACQUES DEROMEDepartment of Meteorology, McGill University, Montrdal, Quebec, H3A 2K6, Canada(Manuscript received 19 June 1984
I AuGUSTI985 HERSCHEL L. MITCHELL AND JACQUES DEROME 1653Resonance of Topographically Forced Waves in a Quasi-Geostrophic Model HERSCHEL L. MITCHELL Recherche en Prdvision Num~rique, Atmospheric Environment Service, Dorval, Quebec, H9P 1J3, Canada JACQUES DEROMEDepartment of Meteorology, McGill University, Montrdal, Quebec, H3A 2K6, Canada(Manuscript received 19 June 1984
84 . The general understanding of the instability of a zonally varying flow without a restriction of ∂/∂ y = 0 on a disturbance has yet to be established. The instability of a parallel flow can be most succinctly interpreted in terms of wave resonance ( Bretherton 1966 ; Baines and Mitsudera 1994 ; and others). By wave resonance we mean that instability results from mutual reinforcement of two constituent wave components with the same zonal wavelength that are stationary relative to one another
84 . The general understanding of the instability of a zonally varying flow without a restriction of ∂/∂ y = 0 on a disturbance has yet to be established. The instability of a parallel flow can be most succinctly interpreted in terms of wave resonance ( Bretherton 1966 ; Baines and Mitsudera 1994 ; and others). By wave resonance we mean that instability results from mutual reinforcement of two constituent wave components with the same zonal wavelength that are stationary relative to one another
2670 JOURNAL OF THE ATMOSPHERIC SCIENCES VOL. 52, NO. I5Acoustic Resonance of the A~raosphere at 3.7 mHz MAKOTO TAHIRADepartment of Earth Sciences, Aichi University of Education, Kariya, Japan(Manuscript received 28 June 1994, in final form 3 February 1995)ABSTRACT Vertical propagation of plane acoustic-gravity waves with horizontal wave fronts is discussed using a layermodel with realistic temperature
2670 JOURNAL OF THE ATMOSPHERIC SCIENCES VOL. 52, NO. I5Acoustic Resonance of the A~raosphere at 3.7 mHz MAKOTO TAHIRADepartment of Earth Sciences, Aichi University of Education, Kariya, Japan(Manuscript received 28 June 1994, in final form 3 February 1995)ABSTRACT Vertical propagation of plane acoustic-gravity waves with horizontal wave fronts is discussed using a layermodel with realistic temperature
excited and the perturbation streamfunction grows linearly in time. The existence of a linear resonance has been found before in analytical studies of the Eady model where the upper rigid lid was removed ( Thorncroft and Hoskins 1990 ; Chang 1992 ; Davies and Bishop 1994 ; Bishop and Heifetz 2000 ) but no serious attempt has been made so far to include the impact of the linear resonance in an analytical approach to the SV. To fill the gap we will concentrate on the role of the CMs in the SV
excited and the perturbation streamfunction grows linearly in time. The existence of a linear resonance has been found before in analytical studies of the Eady model where the upper rigid lid was removed ( Thorncroft and Hoskins 1990 ; Chang 1992 ; Davies and Bishop 1994 ; Bishop and Heifetz 2000 ) but no serious attempt has been made so far to include the impact of the linear resonance in an analytical approach to the SV. To fill the gap we will concentrate on the role of the CMs in the SV
