Search Results

You are looking at 101 - 110 of 6,116 items for :

  • Waves, oceanic x
  • Journal of Physical Oceanography x
  • Refine by Access: Content accessible to me x
Clear All
W. Perrie and B. Toulany

total energy E ∗ c o can be parameterized by a fetch-law relation in terms of inverse wave age U ∗ c / C p , E ∗ c o = ϵ ( U ∗ c / C p ) γ , (4) where γ and ϵ are appropriate constants. Equation (4) is important because it relates total energy E ∗ c o and inverse wave age U ∗ c / C p . These are open ocean variables specifying spectral maturity. Fetch relations such as Eq. (4) obtained correlation coefficients as high as 0.99 with respect to the CASP data ( Perrie and Toulany 1990

Full access
Julien Jouanno, Frédéric Marin, Yves du Penhoat, and Jean-Marc Molines

associated with the tropical instability waves (TIWs), which are triggered by the instabilities of the tropical oceanic currents (e.g., von Schuckmann et al. 2008 ; Perez et al. 2012 ). Besides the observational evidence that the 15-day variability of the meridional surface velocities is forced by the wind, the dynamical response of the upper ocean to 15-day wind fluctuations is still not fully understood. As mentioned by Picaut (1984) , there is a discrepancy between the zonal wavelengths of the

Full access
Lars Czeschel, Carsten Eden, and Richard J. Greatbatch

-driven stratified ocean is initially strongly modified by variable topography, and it is only when most baroclinic Rossby waves emitted from the wind forcing have reached the western boundary that flat-bottom Sverdrup balance tends to be reached ( Anderson and Killworth 1977 ). Anderson and Corry (1985a) show that transport variation can be related to barotropic Rossby waves generated by wind stress and wind stress curls acting over variable bottom topography. In addition, baroclinic Kelvin waves from the

Full access
Christopher J. Zappa, Michael L. Banner, Russel P. Morison, and Sophia E. Brumer

central role of surface and breaking waves in upper ocean dynamics and air–sea fluxes, wave and breaking measurements are paramount. The dissipation of wave energy in the energetic part of the spectrum has attracted considerable recent interest. Presently, parametric versions of S ds based on satellite data are used in the context of active whitecap fraction ( Anguelova and Hwang 2016 ), of ocean swell dissipation ( Ardhuin et al. 2009 ), and of the TKE dissipation rate due to breaking ( Hwang and

Full access
Jamie MacMahan

swell) that occur in the 3456–12 096-cpd frequency band (7–25-s periods) that radiate away from the coast and travel around the ocean basins ( Herbers et al. 1994 , 1995 ; among others). Based on these studies, it is plausible that small-amplitude, free IG waves in the seiche frequency bands are a component of oceanic white noise, and they are what is forcing the seiche in Monterey Bay and likely elsewhere. Though there is agreement on the idea that free IG waves are a component of oceanic white

Full access
Christopher C. Chapman, Andrew McC. Hogg, Andrew E. Kiss, and Stephen R. Rintoul

baroclinicity. Energy is passed from one eddy to another in the downstream development process. Danielson et al. (2006) presented an example of this effect in an analysis of cyclone development over the North Pacific using atmospheric reanalysis data. A single wave packet emanating from the Asian mainland caused two cyclones to develop as it propagated across the ocean. Taken together, Simmons and Hoskins (1979) and Chang and Orlanski (1993) provide a compelling physical mechanism for the formation

Full access
Gengxin Chen, Weiqing Han, Yuanlong Li, Michael J. McPhaden, Ju Chen, Weiqiang Wang, and Dongxiao Wang

-pass filtered forcing inside the box. Fig . 2. Mooring-observed daily (a) zonal current u and (b) meridional current υ (m s −1 ) of the upper 400 m at 5°N, 90.5°E from 2 Apr 2013 through 15 Apr 2014. The black line marks the zero velocity contour. The ISV of the equatorial winds over the Indian Ocean has been shown to significantly affect the adjacent areas. Intraseasonal equatorial Kelvin waves driven by winds associated with the MJO can propagate to the eastern Indian Ocean (EIO) boundary and the

Full access
Luigi Cavaleri

about our hopeful idea that, adding the single descriptions of the various processes at work, this would be enough to create a proper hindcasting–forecasting machine. As discussed in the previous section, clearly the experience indicates this is not the case. To start with, the sea on which we propagate our waves is not uniform and undisturbed. Rather, the oceans are characterized by currents that interact with the wave field. Most of the currents we find in the sea are not strong enough to affect

Full access
J. R. Carpenter, A. Guha, and E. Heifetz

(1957) . Recent observational evidence of the presence of a critical layer in the airflow above ocean waves has also been found by Hristov et al. (2003) and Grare et al. (2013) . In addition, controlled laboratory experiments by Buckley and Veron (2016) demonstrate the presence of a critical layer, despite the presence of a highly turbulent airflow, in agreement with the predictions of Miles’ theory. In all of these observations, the critical layer only emerges once significant phase averaging

Full access
Gengxin Chen, Weiqing Han, Xiaolin Zhang, Linlin Liang, Huijie Xue, Ke Huang, Yunkai He, Jian Li, and Dongxiao Wang

> 107.5°E, 7.5°S < y < 7.5°N, and it relaxes the zonal-velocity and pressure fields of each mode to zero there ( Han et al. 1999 ). The damper efficiently absorbs the energy of incoming equatorial Kelvin waves, and thus no Rossby waves are reflected back into the ocean interior from the eastern boundary. While LOM_DAMP primarily measures the effects of directly forced Kelvin and Rossby waves, the solution difference LOM_Reflect (LOM_MR − LOM_DAMP) isolates the reflected Rossby wave effects ( Chen

Restricted access