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B. L. Blackford

for four different values of v are shown.664 JOURNAL OF PHYSICAL OCEANOGRAPHY VOLUME8used to carry out a linear regression (from t = 0to t = 60 h) between the sinusoidal wind stresspulse and the resulting current amplitude, assuming only .one wind stress pulse in a 60 h interval.The analysis was done for each value of v and theresulting linear relationships were

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Paul A. Hwang and Edward J. Walsh

10°, the range of the linear regression slope is between 0.7 and 1.1, the rms difference is between 16 and 42°, and the correlation coefficient is better than 0.7 in 8 of the 9 datasets. The model performance may deteriorate considerably for hurricane data with close proximity to land (B26) and rapid change of hurricane translation direction or speed (H24). The analysis results show that waves in the front-right quarter propagate into the advancing wind field, and they can grow higher and longer

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Lonneke Goddijn-Murphy, David K. Woolf, and Adrian H. Callaghan

speeds and the detection of an apparent dependence on wind history, among other features. However, sea state was not measured and whitecap coverage was parameterized solely in terms of ship-board wind speed. The data can be divided into two overlapping groups: all W data points measured at wind speeds below 11.25 m s −1 and all W data points above 9.25 m s −1 . Applying a simple regression of W 1/3 versus wind speed, it was determined that the regression slope for the lower wind speeds is

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Georgia D. Kalantzi, Christine Gommenginger, and Meric Srokosz

opportunities for investigating the model’s behavior under different wind and wave conditions, the model has, unfortunately, yet to be officially released, and no results with the new version are therefore included in this analysis. Section 5 is dedicated to the methodology, including the descriptions of the north Indian Ocean study area and the local monsoon cycle, the model and altimeter datasets used, the collocation technique, and the manner with which the datasets were analyzed and compared. Section

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Warren B. White and Jeffrey L. Annis

meridional components of geostrophic flow at the sea surface. We utilize mean geostrophic flow computed from the surface geopotential anomaly (0/2000 m) based on the historical hydrographic dataset compiled at the National Oceanographic Data Center (NODC) by Levitus et al. (1994) and Levitus and Boyer (1994) . Prior to analysis, we interpolated the SST and atmospheric data onto the 1° latitude by 1° longitude grid of the SLH data, centered at the middle of each month. Next, we computed long

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Stuart D. Smith

715 Rotation 0 about a vertical yaw axis would causespurious horizontal crosswind fluctuations us' = Usin0, while u~'= U(1- cos0) is very small forreasonable values of 0 = 10-15-. The effect onmeasured fluxes should therefore be minimal. Pond(1968) has shown that pitching of an anemometersupport by a few degrees also causes negligible fluxerrors. However, if pitch and yaw motions of theplatform are coupled, then much larger flux errorscan result. Our data analysis procedure correctsu~ua for

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Odin Gramstad, Elzbieta Bitner-Gregersen, Karsten Trulsen, and José Carlos Nieto Borge

waves, he showed that such a system is unstable for crossing angles 0° < θ < 70.5° and 136.1° < θ ≤ 180°. Based on this result it was suggested by Onorato et al. (2006) that more rogue waves may be expected in crossing sea states with crossing angles smaller than about 70°. Similar analysis was presented also in Onorato et al. (2010) , who, based on the growth rate and amplification factor of an Akhmediev breather solution, suggested that a maximum amount of rogue waves could be expected for

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Alejandra Sanchez-Franks, Sultan Hameed, and Robert E. Wilson

plankton distributions. The analysis presented in this paper is based on the GSNW index of Taylor and Stephens (1980 , 1998 ). This index has been used in studies of plankton abundance in the eastern North Atlantic, the North Sea ( Taylor 1995 ; Planque and Taylor 1998 ), Narragansett Bay ( Borkman and Smayda 2009 ), and lakes in Ireland ( Jennings and Allott 2006 ). From current measurements in the slope sea, Bane et al. (1988) found the southwestward shelfbreak current is stronger when the Gulf

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Gregory C. Johnson, Eric Kunze, Kristene E. McTaggart, and Dennis W. Moore

scientific parties of the many scientific programs involved in collecting deep CTD data in the equatorial Pacific. Conversations with Eric D'Asaro, William Kessler, LuAnne Thompson (as usual), and Mike Wallace were useful. Comments from Eric Firing and two anonymous reviewers improved the manuscript. REFERENCES Cleveland , W. S. , and S. J. Devlin , 1988 : Locally weighted regression: An approach to regression analysis by local fitting. J. Amer. Stat. Assoc. , 83 , 596 – 610 . Dengler , M

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Michael M. Whitney and Richard W. Garvine

demand tidal information along all open boundaries, as in the shelf tidal modeling efforts of Han (2000) . The inverse tidal model does not provide reliable results along the across-shelf boundaries because TOPEX/Poseidon altimetry does not perform well over shallow waters. To create tidal information for the across-shelf open boundary conditions, a tidal simulation over a much longer domain (with lower resolution and no estuary) was executed prior to the standard runs. Harmonic analysis of these

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