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ω L , (iv) upward energy propagation as inferred both from clockwise-rotating-with-depth shear and downward phase propagation, and (v) narrowband vertical wavelengths ~ O (100) m ~ O ( U/N ) [although Sheen et al. (2013) reported no well-defined spectral peak in shear or strain]. Features iii–v are consistent with expectations for lee-wave generation in the continuum band f ≪ | kU | ≪ N radiating aloft (e.g., Nikurashin and Ferrari 2010a ). Trossman et al. (2015) revisited this
ω L , (iv) upward energy propagation as inferred both from clockwise-rotating-with-depth shear and downward phase propagation, and (v) narrowband vertical wavelengths ~ O (100) m ~ O ( U/N ) [although Sheen et al. (2013) reported no well-defined spectral peak in shear or strain]. Features iii–v are consistent with expectations for lee-wave generation in the continuum band f ≪ | kU | ≪ N radiating aloft (e.g., Nikurashin and Ferrari 2010a ). Trossman et al. (2015) revisited this
1. Introduction Slowly varying stratified flow over topography occurs throughout the ocean either due to mean flows or eddies. Energy can be lost from the mean flow by bottom friction (usually small), by the creation of internal waves that radiate and eventually break ( Nikurashin and Ferrari 2010 ), or by other nonlinear processes. By creating internal waves that have to break in the water column, mean flow over rough topography is one of the possible pathways by which the interior of the
1. Introduction Slowly varying stratified flow over topography occurs throughout the ocean either due to mean flows or eddies. Energy can be lost from the mean flow by bottom friction (usually small), by the creation of internal waves that radiate and eventually break ( Nikurashin and Ferrari 2010 ), or by other nonlinear processes. By creating internal waves that have to break in the water column, mean flow over rough topography is one of the possible pathways by which the interior of the
