DOCSLIB.ORG

Deep Circulation in the Eastern South Pacific Ocean Vincent Faure

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Deep Circulation in the Eastern South Pacific Ocean Vincent Faure Florida State University Libraries Electronic Theses, Treatises and Dissertations The Graduate School 2009 Deep Circulation in the Eastern South Pacific Ocean Vincent Faure Follow this and additional works at the FSU Digital Library. For more information, please contact [email protected] FLORIDA STATE UNIVERSITY COLLEGE OF ARTS AND SCIENCES DEEP CIRCULATION IN THE EASTERN SOUTH PACIFIC OCEAN By VINCENT FAURE A Dissertation submitted to the Department of Oceanography in partial fulfillment of the requirements for the degree of Doctor of Philosophy Degree Awarded: Summer Semester, 2009 The members of the committee approve the dissertation of Vincent Faure defended on April 25, 2008. Kevin Speer Professor Directing Dissertation Carol Anne Clayson Outside Committee Member Doron Nof Committee Member Georges Weatherly Committee Member William Landing Committee Member Philip Froelich Committee Member Approved: William Dewar, Chair, Department of Oceanography Joseph Travis, Dean, College of Arts and Sciences The Graduate School has verified and approved the above-named committee members. ii TABLE OF CONTENTS List of Tables ...................................... v List of Figures ..................................... vi Abstract ........................................ ix 1. INTRODUCTION ................................. 1 1.1 Objective of the study ............................ 1 1.2 Study Area and Water Masses ........................ 2 1.3 Deep eastern boundary flow ......................... 4 1.4 Zonal flow and mantle Helium ........................ 5 1.5 Circulation study from Davis ........................ 6 2. DATA ........................................ 9 2.1 Hydrography ................................. 9 2.2 Floats ..................................... 10 3. MODEL ....................................... 11 3.1 Inverting a tracer field ............................ 11 3.2 Statistical method .............................. 12 3.3 Physical model ................................ 13 3.4 Solving the system .............................. 15 3.5 Model settings ................................ 16 3.6 Initial Model State .............................. 16 4. RESULTS ...................................... 18 4.1 Preferred solution: choice of the oxygen consumption rate λ . 18 4.2 Diffusivity coefficients ............................ 19 4.3 Upper layer circulation: Comparison with float subsurface displacement data ...................................... 20 4.4 Isopycnal circulation: upper, middle and lower layers . 22 4.5 Deep flow in the East Pacific Rise region . 23 4.6 The deep eastern boundary flow ....................... 25 4.7 PV balance regimes ............................. 26 5. DISCUSSION .................................... 30 iii 5.1 Summary ................................... 31 APPENDICES ..................................... 62 A. MODEL GRID ................................... 62 B. MCMC MOVES .................................. 64 C. USING A STREAMFUNCTION TO IMPOSE GEOSTROPHY . 65 D. DIAPYCNAL VELOCITIES ........................... 67 E. AN ATLAS ..................................... 72 E.1 Isopycnal maps of δ3He ........................... 73 E.2 Isopycnal maps of Oxygen concentration . 83 E.3 Isopycnal maps of Silica concentration ................... 88 REFERENCES ..................................... 92 BIOGRAPHICAL SKETCH ............................. 97 iv LIST OF TABLES 2.1 Summary of all hydrographic data.WHP: World Ocean Circulation Ex- periment - Hydrographic Program; NODC: National Oceanographic Data Center. ...................................... 9 5.1 Number of float velocity measurements data per box. 33 5.2 Posterior mean diffusivities for various oxygen consumption rates. The diffusivities are spatially constant. Those were produced with runs where the diapycnal diffusivity is held constant. The Peclet number Pe is averaged over the model domain. .............................. 33 v LIST OF FIGURES 1.1 δ3He (expressed in %, see text for a definition of δ3He ) along the WOCE Hydrographic Program meridional section P19 (88◦W). The white lines show the 9 neutral surfaces used to define the inverse model’s layers. The neutral density values range from 28 to 27.4. ...................... 6 1.2 δ3He (expressed in %, see text for a definition of δ3He ) along the WOCE Hydrographic Program meridional section P06 (32◦S). ............. 7 4.1 Contours of potential vorticity on γ = 28. .................... 28 4.2 Contours of potential vorticity on γ = 27.4. ................... 29 5.1 Bathymetry of the south eastern Pacific Ocean and its main features. 34 5.2 Position of all hydrographic profiles along the neutral surface γ = 27.4: WOCE and pre-WOCE (dots) ARGO profiling floats (diamonds). 35 5.3 Same as figure 5.2 for γ = 28. .......................... 36 5.4 Dissolved oxygen (µ mol kg−1) along (32◦S). World Ocean Circulation ex- periment (WOCE) section P06, May-August 1992. The depths of 9 neutral density surfaces used to define the model layers are shown in white: 28, 27.98, 27.95, 27.8, 27.7, 27.6, 27.5 and 27.4. ...................... 37 5.5 Salinity along P06 (32◦S). ............................ 38 5.6 Oxygen concentration along the neutral density layer γ = 27.7. 39 5.7 Oxygen concentration, WOCE section P19 along 88◦W. 40 5.8 Oxygen concentration from the WOCE section P17E along 54◦S. 41 5.9 Oxygen concentration from the WOCE section P17 along 135◦W. 42 5.10 Helium concentration (%, see text) along WOCE section P18 (103◦W) . 43 5.11 Posterior mean of the cost function defined by (3.2) as a function of the oxygen consumption term. ................................ 44 vi 5.12 Oxygen Utilization Rate (OUR) as a function of depth. The thick blue curve is the preferred values. The two thin blue curves define a confidence interval where λ is optimal (corresponds to a minimum of the model costfunction). The vertical red and black lines show the estimates of Feely et al. (2004) and Craig (1971) respectively (no confidence intervals provided). These studies assume a constant value of OUR in the depth range 1000-4000dbar. 45 5.13 Posterior mean of diffusivities Kx (blue) and Ky (red) as a function of the oxygen consumption rate λ. Uncertainties are shown with a gray shading. 46 5.14 Distribution of velocities measured by floats (Argo and WOCE). Each dot corresponds to the mid-position of the subsurface displacement. 47 5.15 Box averaged velocities from subsurface floats displacements (data from Argo and WOCE experiments). The boxes dimensions are 4◦in latitude and are delimited by three meridians (140◦W, 120◦W, 100◦W) and the coast line. A different scale is used for velocities larger than 1cm/s. 48 5.16 Zonal components of box average velocities from the inverse model’s upper layer (γn = 27.4, blue line) and from the float data adjusted to the same layer depth as a function of latitude for three longitues: (a) 130◦W, (b) 110◦W and (c) 80◦W. The region of the ACC is excluded. Positive values are eastward. The grey shadings represent uncertainties. ................... 49 5.17 Oxygen distribution along the neutral density surface γn = 27.98 . 50 5.18 Silica distribution along the neutral density surface γn = 27.98 . 51 5.19 Upper panel: meridional transport across 32◦S, the upper part of the EPR is also shown. Lower panel: cumulative meridional transport, from east to west, in the depth range of the model (between the neutral layer γ = 28 and γ = 27.4). ..................................... 52 5.20 Posterior mean velocities on isopycnal γ = 27.98. Two scales are used (black and gray) and the arrows on the right indicate 1cm/s. 53 5.21 Posterior mean velocities on isopycnal γ = 27.8. Two scales are used (black and gray) and the arrows on the right indicate 1cm/s. 54 5.22 Posterior mean velocities on isopycnal γ = 27.5. Two scales are used (black and gray) and the arrows on the right indicate 1cm/s. 55 5.23 Map of δ3He (posterior mean) overlaid with the posterior mean velocity field along the layer γ = 27.98. ............................ 56 vii 5.24 Base-10 logarithm of Peclet number computed from the zonal and meridional components of the posterior mean velocities and diffusivities for the neutral layer γ = 27.98. The 2700db isobath is shown in 3.2 to locate the EPR and Sala y Gomez ridge. The Subantartic Front (dash line), Polar Front (continous line) and Southern ACC Front (dash) are also shown. 57 5.25 Same as figure 5.24 for the neutral layer γ = 27.8. 58 5.26 Same as figure 5.24 for the neutral layer γ = 27.5. 59 5.27 Dependence of the ratio: diapycnal stretching over isopycnal diffusion of PV (y-axis) against the ’PV’ Peclet number (x-axis) shown on Fig. 5.24 representing the balance of eq. 4.1. Area where Pe 6 1 and ratio > 1 denotes possible Stommel-Arons regime. ......................... 60 5.28 MCMC trace plot of the costfunction defined in Eq. 3.2 and 3.12. All terms associated with each tracer are shown. Each step corresponds to 100 iterations as described in the text. Only the last 20,000 steps of the calculation are plotted. These last steps were used to compute the posterior mean of the model parameters. ................................ 61 C.1 Posterior streamfunction for a run using a streamfunction MCMC move. 66 ∂w −1 D.1 Posterior mean of the diapycnal stretching ∂z in s along the shallowest layer (1000m). ...................................... 68 ∂w −1 D.2 Posterior mean of the diapycnal stretching ∂z in s along the deepest layer (2500m). ...................................... 69 D.3 Posterior mean of the diapycnal velocities in ms−1 along the shallowest
Load more

Recommended publications
  • Rapid Mixing and Exchange of Deep-Ocean Waters in an Abyssal Boundary Current
    Rapid mixing and exchange of deep-ocean waters in an abyssal boundary current Alberto C. Naveira Garabatoa,1, Eleanor E. Frajka-Williamsb, Carl P. Spingysa, Sonya Leggc, Kurt L. Polzind, Alexander Forryana, E. Povl Abrahamsene, Christian E. Buckinghame, Stephen M. Griffiesc, Stephen D. McPhailb, Keith W. Nichollse, Leif N. Thomasf, and Michael P. Meredithe aOcean and Earth Science, National Oceanography Centre, University of Southampton, SO14 3ZH Southampton, United Kingdom; bNational Oceanography Centre, SO14 3ZH Southampton, United Kingdom; cNational Oceanic and Atmospheric Administration Geophysical Fluid Dynamics Laboratory & Atmospheric and Oceanic Sciences Program, Princeton University, Princeton, NJ 08544; dDepartment of Physical Oceanography, Woods Hole Oceanographic Institution, Woods Hole, MA 02543; ePolar Oceans, British Antarctic Survey, CB3 0ET Cambridge, United Kingdom; and fDepartment of Earth System Science, Stanford University, Stanford, CA 94305 Edited by Eric Guilyardi, Laboratoire d’Océanographie et du Climat: Expérimentations et Approches Numériques, Institute Pierre Simon Laplace, Paris, France, and accepted by Editorial Board Member Jean Jouzel May 26, 2019 (received for review March 8, 2019) The overturning circulation of the global ocean is critically shaped UK–US Dynamics of the Orkney Passage Outflow (DynOPO) by deep-ocean mixing, which transforms cold waters sinking at high project (17), and consisted of two core elements: a series of fifteen latitudes into warmer, shallower waters. The effectiveness of mixing 6- to 128-km-long vessel-based sections of profile measurements in driving this transformation is jointly set by two factors: the crossing the boundary current at an unusually high horizontal – – ∼ intensity of turbulence near topography and the rate at which well- resolution (Fig.
    [Show full text]
  • Hydrographic Atlas of the World Ocean Circulation Experiment (WOCE) Volume 2: Pacific Ocean
    Hydrographic Atlas of the World Ocean Circulation Experiment (WOCE) Volume 2: Pacific Ocean Lynne D. Talley Series edited by Michael Sparrow, Piers Chapman and John Gould Hydrographic Atlas of the World Ocean Circulation Experiment (WOCE) Volume 2: Pacific Ocean Lynne D. Talley Scripps Institution of Oceanography, University of San Diego, La Jolla, California, USA. Series edited by Michael Sparrow, Piers Chapman and John Gould. Compilation funded by the US National Science Foundation, Ocean Science division grant OCE-9712209. Publication supported by BP. Cover Picture: The photo on the front cover was kindly supplied by Akihisa Otsuki. It shows squalls in the northernmost area of the Mariana Islands and was taken on June 12, 1993. Cover design: Signature Design in association with the atlas editors, Principal Investigators and BP. Printed by: ATAR Roto Presse SA, Geneva,Switzerland. DVD production: ODS Business Services Limited, Swindon, UK. Published by: National Oceanography Centre, Southampton, UK. Recommended form of citation: 1. For this volume: Talley, L. D., Hydrographic Atlas of the World Ocean Circulation Experiment (WOCE). Volume 2: Pacific Ocean (eds. M. Sparrow, P. Chapman and J. Gould), International WOCE Project Office, Southampton, UK, ISBN 0-904175-54-5. 2007 2. For the whole series: Sparrow, M., P. Chapman, J. Gould (eds.), The World Ocean Circulation Experiment (WOCE) Hydrographic Atlas Series (4 vol- umes), International WOCE Project Office, Southampton, UK, 2005-2007 WOCE is a project of the World Climate Research Programme (WCRP) which is sponsored by the World Meteorological Organization (WMO), the International Council for Science (ICSU) and the Intergovernmental Oceanographic Commission (IOC) of UNESCO.
    [Show full text]
  • Spiciness Theory Revisited, with New Views on Neutral Density, Orthogonality, and Passiveness
    Ocean Sci., 17, 203–219, 2021 https://doi.org/10.5194/os-17-203-2021 © Author(s) 2021. This work is distributed under the Creative Commons Attribution 4.0 License. Spiciness theory revisited, with new views on neutral density, orthogonality, and passiveness Rémi Tailleux Dept. of Meteorology, University of Reading, Earley Gate, RG6 6ET Reading, United Kingdom Correspondence: Rémi Tailleux ([email protected]) Received: 26 April 2020 – Discussion started: 20 May 2020 Revised: 8 December 2020 – Accepted: 9 December 2020 – Published: 28 January 2021 Abstract. This paper clarifies the theoretical basis for con- 1 Introduction structing spiciness variables optimal for characterising ocean water masses. Three essential ingredients are identified: (1) a As is well known, three independent variables are needed to material density variable γ that is as neutral as feasible, (2) a fully characterise the thermodynamic state of a fluid parcel in material state function ξ independent of γ but otherwise ar- the standard approximation of seawater as a binary fluid. The bitrary, and (3) an empirically determined reference function standard description usually relies on the use of a tempera- ξr(γ / of γ representing the imagined behaviour of ξ in a ture variable (such as potential temperature θ, in situ temper- notional spiceless ocean. Ingredient (1) is required because ature T , or Conservative Temperature 2), a salinity variable contrary to what is often assumed, it is not the properties im- (such as reference composition salinity S or Absolute Salin- posed on ξ (such as orthogonality) that determine its dynam- ity SA), and pressure p.
    [Show full text]
  • Is the Neutral Surface Really Neutral? a Close Examination of Energetics of Along Isopycnal Mixing
    Is the neutral surface really neutral? A close examination of energetics of along isopycnal mixing Rui Xin Huang Department of Physical Oceanography Woods Hole Oceanographic Institution Woods Hole, MA 02543, USA April 19, 2010 Abstract The concept of along-isopycnal (along-neutral-surface) mixing has been one of the foundations of the classical large-scale oceanic circulation framework. Neutral surface has been defined a surface that a water parcel move a small distance along such a surface does not require work against buoyancy. A close examination reveals two important issues. First, due to mass continuity it is meaningless to discuss the consequence of moving a single water parcel. Instead, we have to deal with at least two parcels in discussing the movement of water masses and energy change of the system. Second, movement along the so-called neutral surface or isopycnal surface in most cases is associated with changes in the total gravitational potential energy of the ocean. In light of this discovery, neutral surface may be treated as a preferred surface for the lateral mixing in the ocean. However, there is no neutral surface even at the infinitesimal sense. Thus, although approximate neutral surfaces can be defined for the global oceans and used in analysis of global thermohaline circulation, they are not the surface along which water parcels actually travel. In this sense, thus, any approximate neutral surface can be used, and their function is virtually the same. Since the structure of the global thermohaline circulation change with time, the most suitable option of quasi-neutral surface is the one which is most flexible and easy to be implemented in numerical models.
    [Show full text]
  • An Assessment of Orthobaric Density in the Global Ocean
    2054 JOURNAL OF PHYSICAL OCEANOGRAPHY VOLUME 35 An Assessment of Orthobaric Density in the Global Ocean TREVOR J. MCDOUGALL AND DAVID R. JACKETT CSIRO Marine Research, Hobart, Australia (Manuscript received 20 May 2004, in final form 18 April 2005) ABSTRACT Orthobaric density has recently been advanced as a new density variable for displaying ocean data and as a coordinate for ocean modeling. Here the extent to which orthobaric density surfaces are neutral is quantified and it is found that orthobaric density surfaces are less neutral in the World Ocean than are potential density surfaces referenced to 2000 dbar. Another property that is important for a vertical coordinate of a layered model is the quasi-material nature of the coordinate and it is shown that orthobaric density surfaces are significantly non-quasi-material. These limitations of orthobaric density arise because of its inability to accurately accommodate differences between water masses at fixed values of pressure and in situ density such as occur between the Northern and Southern Hemisphere portions of the World Ocean. It is shown that special forms of orthobaric density can be quite accurate if they are formed for an individual ocean basin and used only in that basin. While orthobaric density can be made to be approximately neutral in a single ocean basin, this is not possible in both the Northern and Southern Hemisphere portions of the Atlantic Ocean. While the helical nature of neutral trajectories (equivalently, the ill-defined nature of neutral surfaces) limits the neutrality of all types of density surface, the inability of orthobaric density surfaces to accurately accommodate more than one ocean basin is a much greater limitation.
    [Show full text]
  • Orthobaric Density: a Thermodynamic Variable for Ocean Circulation Studies
    2830 JOURNAL OF PHYSICAL OCEANOGRAPHY VOLUME 30 Orthobaric Density: A Thermodynamic Variable for Ocean Circulation Studies ROLAND A. DE SZOEKE,SCOTT R. SPRINGER, AND DAVID M. OXILIA College of Oceanic and Atmospheric Sciences, Oregon State University, Corvallis, Oregon (Manuscript received 21 October 1998, in ®nal form 30 December 1999) ABSTRACT A new density variable, empirically corrected for pressure, is constructed. This is done by ®rst ®tting com- pressibility (or sound speed) computed from global ocean datasets to an empirical function of pressure and in situ density (or speci®c volume). Then, by replacing true compressibility by this best-®t virtual compressibility in the thermodynamic density equation, an exact integral of a Pfaf®an differential form can be found; this is called orthobaric density. The compressibility anomaly (true minus best-®t) is not neglected, but used to develop a gain factor c on the irreversible processes that contribute to the density equation and drive diapycnal motion. The complement of the gain factor, c 2 1, multiplies the reversible motion of orthobaric density surfaces to make a second contribution to diapycnal motion. The gain factor is a diagnostic of the materiality of orthobaric density: gain factors of 1 would indicate that orthobaric density surfaces are as material as potential density surfaces. Calculations of the gain factor for extensive north±south ocean sections in the Atlantic and Paci®c show that it generally lies between 0.8 and 1.2. Orthobaric density in the ocean possesses advantages over potential density that commend its use as a vertical coordinate for both descriptive and modeling purposes.
    [Show full text]
  • MIMOC: a Global Monthly Isopycnal Upperocean Climatology with Mixed
    JOURNAL OF GEOPHYSICAL RESEARCH: OCEANS, VOL. 118, 1658–1672, doi:10.1002/jgrc.20122, 2013 MIMOC: A global monthly isopycnal upper-ocean climatology with mixed layers Sunke Schmidtko,1,2 Gregory C. Johnson,1 and John M. Lyman1,3 Received 23 November 2012; revised 7 February 2013; accepted 8 February 2013; published 3 April 2013. [1] A monthly, isopycnal/mixed-layer ocean climatology (MIMOC), global from 0 to 1950 dbar, is compared with other monthly ocean climatologies. All available quality- controlled profiles of temperature (T) and salinity (S) versus pressure (P) collected by conductivity-temperature-depth (CTD) instruments from the Argo Program, Ice-Tethered Profilers, and archived in the World Ocean Database are used. MIMOC provides maps of mixed layer properties (conservative temperature, Y, absolute salinity, SA, and maximum P) as well as maps of interior ocean properties (Y, SA, and P) to 1950 dbar on isopycnal surfaces. A third product merges the two onto a pressure grid spanning the upper 1950 dbar, adding more familiar potential temperature (θ) and practical salinity (S) maps. All maps are at monthly 0.5 Â 0.5 resolution, spanning from 80Sto90N. Objective mapping routines used and described here incorporate an isobath-following component using a “Fast Marching” algorithm, as well as front-sharpening components in both the mixed layer and on interior isopycnals. Recent data are emphasized in the mapping. The goal is to compute a climatology that looks as much as possible like synoptic surveys sampled circa 2007–2011 during all phases of the seasonal cycle, minimizing transient eddy and wave signatures.
    [Show full text]
  • Spiciness Theory Revisited, with New Views on Neutral Density
    Spiciness theory revisited, with new views on neutral density, orthogonality and passiveness Rémi Tailleux1 1Dept of Meteorology, University of Reading, Earley Gate, PO Box 243, RG6 6BB Reading, United Kingdom Correspondence: Rémi Tailleux ([email protected]) Abstract. This paper clarifies the theoretical basis for constructing spiciness variables optimal for characterising ocean water masses. Three essential ingredients are identified: 1) a material density variable γ that is as neutral as feasible; 2) a material state function ξ independent of γ, but otherwise arbitrary; 3) an empirically determined reference function ξr(γ) of γ representing the imagined behaviour of ξ in a notional spiceless ocean. Ingredient 1) is required, because contrary to what is often assumed, 5 it is not the properties imposed on ξ (such as orthogonality) that determine its dynamical inertness but the degree of neutrality of 0 γ. The first key result is that it is the anomaly ξ = ξ −ξr(γ), rather than ξ, that is the variable the most suited for characterising ocean water masses, as originally proposed by McDougall and Giles (1987). The second key result is that oceanic sections of normalised ξ0 appear to be relatively insensitive to the choice of ξ, as first suggested by Jackett and McDougall (1985), based on the comparison of very different choices of ξ. It is also argued that orthogonality of rξ0 to rγ in physical space is more 10 germane to spiciness theory than orthogonality in thermohaline space, although how to use it to constrain the choices of ξ and ξr(γ) remains to be fully elucidated.
    [Show full text]
  • Ertel Potential Vorticity Versus Bernoulli Potential on Approximately Neutral Surfaces in the Antarctic Circumpolar Current
    SEPTEMBER 2020 S T A N L E Y E T A L . 2621 Ertel Potential Vorticity versus Bernoulli Potential on Approximately Neutral Surfaces in the Antarctic Circumpolar Current GEOFFREY J. STANLEY School of Mathematics and Statistics, University of New South Wales, Sydney, New South Wales, Australia TIMOTHY E. DOWLING Department of Physics and Astronomy, University of Louisville, Louisville, Kentucky MARY E. BRADLEY Department of Mathematics, University of Louisville, Louisville, Kentucky DAVID P. MARSHALL Department of Physics, University of Oxford, Oxford, United Kingdom (Manuscript received 20 June 2019, in final form 4 July 2020) ABSTRACT We investigate the relationship between Ertel potential vorticity Q and Bernoulli potential B on orthobaric density surfaces in the Antarctic Circumpolar Current (ACC), using the Southern Ocean State Estimate. Similar to the extratropical atmospheres of Earth and Mars, Q and B correlate in the ACC in a function-like manner with modest scatter. Below the near-surface, the underlying function relating Q and B appears to be nearly linear. Nondimensionalizing its slope yields ‘‘Ma,’’ a ‘‘Mach’’ number for long Rossby waves, the ratio of the local flow speed to the intrinsic long Rossby wave speed. We empirically estimate the latter using established and novel techniques that yield qualitatively consistent results. Previous work related ‘‘Ma’’ to the degree of homogeneity of Q and to Arnol’d’s shear stability criteria. Estimates of ‘‘Ma’’ for the whole ACC are notably positive, implying inhomogeneous Q, on all circumpolar buoyancy surfaces studied. Upper layers generally exhibit ‘‘Ma’’ slightly less than unity, suggesting that shear instability may operate within these layers.
    [Show full text]
  • A New Algorithm to Accurately Calculate Neutral Tracer Gradients and Their
    1 A new algorithm to accurately calculate neutral tracer gradients and their 2 impacts on vertical heat transport and water mass transformation ∗ 3 Sjoerd Groeskamp and Paul M. Barker and Trevor J. McDougall 4 School of Mathematics and Statistics, University of New South Wales, Sydney, New South Wales, 5 Australia 6 Ryan P. Abernathey 7 Columbia University, Lamont-Doherty Earth Observatory, New York City, NY, USA 8 Stephen M. Griffies 9 NOAA Geophysical Fluid Dynamics Laboratory & Princeton University Program in Atmospheric 10 and Oceanic Sciences, Princeton, USA ∗ 11 Corresponding author address: Sjoerd Groeskamp, School of Mathematics and Statistics UNSW 12 Sydney, NSW, 2052, Australia 13 E-mail: [email protected] Generated using v4.3.2 of the AMS LATEX template 1 ABSTRACT 14 Mesoscale eddies stir along the neutral plane, and the resulting neutral diffu- 15 sion is a fundamental aspect of subgrid scale tracer transport in ocean models. 16 Calculating neutral diffusion traditionally involves calculating neutral slopes 17 and three-dimensional tracer gradients. The calculation of the neutral slope 18 usually occurs by computing the ratio of the horizontal to vertical locally ref- 19 erenced potential density derivative. This approach is problematic in regions 20 of weak vertical stratification, prompting the use of a variety of ad hoc reg- 21 ularization methods that can lead to rather nonphysical dependencies for the 22 resulting neutral tracer gradients. We here propose an alternative method that 23 is based on a search algorithm that requires no ad hoc regularization. Com- 24 paring results from this new method to the traditional method reveals large 25 differences in spurious diffusion, heat transport and water mass transforma- 26 tion rates that may all affect the physics of, for example, a numerical ocean 27 model.
    [Show full text]
  • Approximating Isoneutral Ocean Transport Via the Temporal Residual Mean
    fluids Article Approximating Isoneutral Ocean Transport via the Temporal Residual Mean Andrew L. Stewart Department of Atmospheric and Oceanic Sciences, University of California, Los Angeles, CA 90095, USA; [email protected] Received: 28 July 2019; Accepted: 27 September 2019; Published: 2 October 2019 Abstract: Ocean volume and tracer transports are commonly computed on density surfaces because doing so approximates the semi-Lagrangian mean advective transport. The resulting density-averaged transport can be related approximately to Eulerian-averaged quantities via the Temporal Residual Mean (TRM), valid in the limit of small isopycnal height fluctuations. This article builds on a formulation of the TRM for volume fluxes within Neutral Density surfaces, (the “NDTRM”), selected because Neutral Density surfaces are constructed to be as neutral as possible while still forming well-defined surfaces. This article derives a TRM, referred to as the “Neutral TRM” (NTRM), that approximates volume fluxes within surfaces whose vertical fluctuations are defined directly by the neutral relation. The purpose of the NTRM is to more closely approximate the semi-Lagrangian mean transport than the NDTRM, because the latter introduces errors associated with differences between the instantaneous state of the modeled/observed ocean and the reference climatology used to assign the Neutral Density variable. It is shown that the NDTRM collapses to the NTRM in the limiting case of a Neutral Density variable defined with reference to the Eulerian-mean salinity, potential temperature and pressure, rather than an external reference climatology, and therefore that the NTRM approximately advects this density variable. This prediction is verified directly using output from an idealized eddy-resolving numerical model.
    [Show full text]
  • Hydrographic Atlas of the World Ocean Circulation Experiment (WOCE) Volume 3: Atlantic Ocean
    Hydrographic Atlas of the World Ocean Circulation Experiment (WOCE) Volume 3: Atlantic Ocean Klaus Peter Koltermann, Viktor Gouretski and Kai Jancke Bundesamt für Seeschifffahrt und Hydrographie, Hamburg, Germany Series edited by Michael Sparrow, Piers Chapman and John Gould Federal Ministry of Education and Research Hydrographic Atlas of the World Ocean Circulation Experiment (WOCE) Volume 3: Atlantic Ocean Klaus Peter Koltermann (1), Viktor Gouretski (2) and Kai Jancke Bundesamt für Seeschifffahrt und Hydrographie, Hamburg, Germany (1) now Natural Risk Assessment Laboratory, Geography Faculty, Moscow State University, Moscow, Russia (2) now KlimaCampus, Universität Hamburg, Hamburg, Germany Series edited by Michael Sparrow, Piers Chapman and John Gould. Compilation funded by German Bundesministerium für Forschung und Technologie, BMFT. Publication supported by BP. Cover Picture: The photo on the front cover was kindly supplied by Olaf Boebel. It was taken in mid December 1992, during the Meteor 22/4 cruise in the South Atlantic. Cover design: Signature Design in association with the atlas editors, Principal Investigators and BP. Printed by: Nauchnyi Mir Publishers, Moscow, Russia DVD production: Reel Picture, San Deigo, CA Published by: National Oceanography Centre, Southampton, UK. Recommended form of citation: 1. For this volume: Koltermann, K.P., V.V. Gouretski and K. Jancke. Hydrographic Atlas of the World Ocean Circulation Experiment (WOCE). Volume 3: Atlantic Ocean (eds. M. Sparrow, P. Chapman and J. Gould). International WOCE Project Office, Southampton, UK, ISBN 090417557X. 2011 2. For the whole series: Sparrow, M., P. Chapman, J. Gould (eds.), The World Ocean Circulation Experiment (WOCE) Hydrographic Atlas Series (4 vol- umes), International WOCE Project Office, Southampton, UK, 2005-2011.
    [Show full text]