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Jahrul M. Alam and John C. Lin

called the mass-adjusted three-dimensional wind field (MATHEW; Sherman 1978 ). Further examples include such commonly used models as the Stochastic Time Inverted Lagrangian Transport model (STILT; Lin et al. 2003 ), “FLEXPART” ( Stohl et al. 1998 ), the Hybrid Particle and Concentration Transport Model (HYPACT; Uliasz 1996 ), Hybrid Single Particle Lagrangian Integrated Trajectory model (HYSPLIT; Draxler and Hess 1998 ), and Numerical Atmospheric Dispersion Modeling Environment (NAME; Ryall and

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Jenna A. Brown, Jamie H. MacMahan, Ad J. H. M. Reniers, and Ed B. Thornton

.g., Anderson 2009 ; Michel et al. 2013 ). Understanding the transport and retention of hazardous pollutants and biological matter in the nearshore region is important for reasons ranging from human health factors to sustaining ecosystems (e.g., Shahidul Islam and Tanaka 2004 ; Grant et al. 2005 ). Studies of cross-shore circulation over the inner shelf, focusing on wave-driven flows (i.e., during weak wind forcing), demonstrate the importance of the onshore Lagrangian Stokes drift u St ( z ) associated

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Ana M. Mancho, Emilio Hernández-García, Des Small, Stephen Wiggins, and Vicente Fernández

field of the western Mediterranean Sea, obtained from a three-dimensional model simulation under climatological atmospheric forcing. Our aim is, first, to find the location and nature of the Lagrangian structures associated with the so-called Balearic Current that serve to maintain the North Balearic Front. And, second, to show that transport mechanisms, in particular the so-called turnstile mechanism previously identified in abstract dynamical systems ( Channon and Lebowitz 1980 ; Bartlett 1982

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Luke P. Van Roekel, Taka Ito, Patrick T. Haertel, and David A. Randall

hurricane-induced mixing run. We show that the LOM is able to reproduce essential features of large-scale ocean circulation and exploit the advantages of the Lagrangian model to present insightful and unique diagnostics of the oceanic transport of heat and tracers. a. Meridional overturning circulation In each experiment, the model is spun up for 1000 years. The circulation reaches a quasi-steady state after 200 years of integration and does not change significantly afterward. To determine time

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Kazuyuki Miyazaki and Toshiki Iwasaki

affected by vertical advection alone, trace analysis approximates the Lagrangian mean vertical velocity well. However, the zonal mean constituent distribution is not determined solely by the mean meridional circulation; it is also a function of how much meridional and vertical mixing is occurring. These transports can lead to errors in the assumptions of trace analysis. We found some disagreements in the mean vertical velocity around the polar vortex between the dynamical and trace analyses. Dynamical

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Jian Lu, Koichi Sakaguchi, Qing Yang, L. Ruby Leung, Gang Chen, Chun Zhao, Erik Swenson, and Zhangshuan J. Hou

CWV. Since water vapor is concentrated in the lower troposphere, this velocity reflects the circulation near the boundary. It can be further decomposed into rotational and divergent components: with ∇ ⋅ v ψ = 0. Noting that we can rewrite (2) as The additional term R represents the numerical dissipation of CWV in the model, reflecting the diffusive effect of the third-order transport scheme on scalars used in MPAS ( Skamarock and Gassmann 2011 ). Except for the extra E − P term, (3

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Peng Wang, James C. McWilliams, Yusuke Uchiyama, Mickaël D. Chekroun, and Daling Li Yi

across the surf-zone edge into the inner shelf ( Figs. 12e,f ); consequently, the inner-shelf tracer concentration is elevated remarkably ( Figs. 11c,d ). Particularly with wave streaming, the tracers are transported farther offshore by the inner-shelf Lagrangian overturning circulation ( Figs. 11c and 12c ). 4. Discussion a. Sensitivity to bottom roughness Wave streaming is parameterized with a streaming force given by Eqs. (A5) and (A6) , in which the bottom roughness height z o is crucial

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Syed Hyder Ali Muttaqi Shah, François W. Primeau, Eric Deleersnijder, and Arnold W. Heemink

velocity along particle pathways. The diffusive transport due to subgrid-scale processes was neglected. However, in coarse-grained ocean circulation models the redistribution of tracers by parameterized eddy diffusive fluxes is an important part of the transport and its neglect leads to substantial errors ( Hall et al. 2004 ). More recent studies have used high-resolution, eddy-permitting models to compute Lagrangian pathways ( Getzlaff et al. 2006 ; Bower et al. 2009 , 2011 ; Gary et al. 2011

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Gang Chen

1. Introduction The global atmospheric circulation transports momentum, energy, moisture, and chemical constituents both horizontally and vertically, and consequently impacts both global and regional climate. The conventional Eulerian-mean circulation, averaged at constant pressure or height, displays a three-cell pattern in each hemisphere, with a tropical Hadley cell, a midlatitude Ferrel cell, and a polar cell (e.g., Peixoto and Oort 1992 ). By contrast, to the extent that an isentropic

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Sarah N. Giddings, Stephen G. Monismith, Derek A. Fong, and Mark T. Stacey

depth-integrated oceanward Eulerian flow ( Uncles and Jordan 1980 ). While in some estuaries this Stokes drift component may be small, in estuaries that are dynamically shallow and/or have strong tidal forcing, Eulerian and Lagrangian means will be different ( Godin 1995 ), complicating inferences of particle transport from observations made at fixed points in space ( Uncles and Jordan 1980 ; Kuo et al. 1990 ). A potentially useful approach to interpret residual circulation in an estuary with a

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