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Jeffrey J. Early and Adam M. Sykulski

set at hourly resolution . J. Geophys. Res. Oceans , 121 , 2937 – 2966 , . 10.1002/2016JC011716 Green , P. J. , and B. W. Silverman , 1993 : Nonparametric Regression and Generalized Linear Models: A Roughness Penalty Approach . Chapman and Hall , 184 pp. 10.1201/b15710 Handcock , M. S. , K. Meier , and D. Nychka , 1994 : Kriging and splines: An empirical comparison of their predictive performance in some applications: Comment . J. Amer

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Andrey Y. Shcherbina, Miles A. Sundermeyer, Eric Kunze, Eric D’Asaro, Gualtiero Badin, Daniel Birch, Anne-Marie E. G. Brunner-Suzuki, Jörn Callies, Brandy T. Kuebel Cervantes, Mariona Claret, Brian Concannon, Jeffrey Early, Raffaele Ferrari, Louis Goodman, Ramsey R. Harcourt, Jody M. Klymak, Craig M. Lee, M.-Pascale Lelong, Murray D. Levine, Ren-Chieh Lien, Amala Mahadevan, James C. McWilliams, M. Jeroen Molemaker, Sonaljit Mukherjee, Jonathan D. Nash, Tamay Özgökmen, Stephen D. Pierce, Sanjiv Ramachandran, Roger M. Samelson, Thomas B. Sanford, R. Kipp Shearman, Eric D. Skyllingstad, K. Shafer Smith, Amit Tandon, John R. Taylor, Eugene A. Terray, Leif N. Thomas, and James R. Ledwell

-front direction, as expected under the confluences. To evaluate the contributions of the vertical shear and lateral strain to the observed changes of the patch geometry, a simple semianalytical advection–diffusion model was used. The evolution of the length, width, and tilts of the dye patches was simulated using velocities measured by shipboard ADCPs, a Lagrangian float, and the nine drifters. Velocity gradients in the model were assumed to be constant across the dye patch but were allowed to vary in time

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Leif N. Thomas, John R. Taylor, Eric A. D’Asaro, Craig M. Lee, Jody M. Klymak, and Andrey Shcherbina

). (c) The section-averaged stratification in the boundary layer (stars) and the oscillatory variations in stratification (black line) caused by inertial shear at a front , as predicted by (2) . The phase in the model was chosen so that a maximum in aligned with the maximum in the observed downstream component of the vertical shear at about yearday 65.3. Before yearday 65.2 the winds were weak and the section-averaged shear nearly equaled the geostrophic shear. As the storm moved through

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Daniel B. Whitt, Leif N. Thomas, Jody M. Klymak, Craig M. Lee, and Eric A. D’Asaro

.2 f has the highest amplitude (see Fig. 7 ). This frequency bin represents the frequency range ; the width of the bin is set by the duration of the drift, which sets the spectral resolution 2 π / T ≈ Δ ω ≈ 0.4 f (see section 3 ). Differences between the two estimates of the frequency could also be attributable to spatial variability since the frequency spectra were calculated within 350 m of the float track, while the evaluation of the dispersion relation was made across entire cross

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