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phase and points in the directionof ~ropagation.(upper map, Fig. 4)~there is virtually .no flow ofenergy in the Southern Ocean, notwithstanding thepropagation of phase (upper map, Fig. 3). Thatanomaly is what made me aware of the problemdiscussed in this note. An interpretation of the foregoing comparisons issuggested by the fact that the elevation is aboutthe same in the two solutions (Fig. 3), and the fact FIG. 4. South polar stereographic projection of energy-fluxstreamfunction (unit and
phase and points in the directionof ~ropagation.(upper map, Fig. 4)~there is virtually .no flow ofenergy in the Southern Ocean, notwithstanding thepropagation of phase (upper map, Fig. 3). Thatanomaly is what made me aware of the problemdiscussed in this note. An interpretation of the foregoing comparisons issuggested by the fact that the elevation is aboutthe same in the two solutions (Fig. 3), and the fact FIG. 4. South polar stereographic projection of energy-fluxstreamfunction (unit and
) eigenvector analysis of sealevelpressure for January and July indicates major shiftsin circulation patterns in the early 1920's and againin the early 1950's. Dzerdzeevskii (1966), using acirculation-type catalog, identified three circulationepochs during the first half of this century which aresimilar to the epochs defined by Kutzbach. Girs(1966) found breaks in the frequency of daily hemispheric circulation types in the 1920's, 1930's and1940's. Comparison of these times of change (Table1) shows that
) eigenvector analysis of sealevelpressure for January and July indicates major shiftsin circulation patterns in the early 1920's and againin the early 1950's. Dzerdzeevskii (1966), using acirculation-type catalog, identified three circulationepochs during the first half of this century which aresimilar to the epochs defined by Kutzbach. Girs(1966) found breaks in the frequency of daily hemispheric circulation types in the 1920's, 1930's and1940's. Comparison of these times of change (Table1) shows that
: (1) to afford a look a t the 5-daymean centered 2 days in advance so that comparison withearlier observed mean maps and with the trend map maypermit further inferences regarding evolution, and (2) toobtain estimates of 5-day mean temperature anomdiesas described below.DECEMBEB 1958 MONTHLY WEATHER REVIEW 469FI(JUIZE 2.-(A) 500-mb. contours for the period April 24-28, 1958 objectively predicted by the summation method (see text). Contoursdrawn for every 400 feet and labeled in tens of feet
: (1) to afford a look a t the 5-daymean centered 2 days in advance so that comparison withearlier observed mean maps and with the trend map maypermit further inferences regarding evolution, and (2) toobtain estimates of 5-day mean temperature anomdiesas described below.DECEMBEB 1958 MONTHLY WEATHER REVIEW 469FI(JUIZE 2.-(A) 500-mb. contours for the period April 24-28, 1958 objectively predicted by the summation method (see text). Contoursdrawn for every 400 feet and labeled in tens of feet
. Oceanographers have constructed to include inhomogeneities and anisotropies associated with the presence of topography, and to reflect in a way the adaptation of the ocean fields to the topography. Utilization of ocean topography may change the weighting operation, in (1) , into a mathematical operator, , that maps the innovation (at the observational points) directly onto the grid points, where could be different in (1) and (5) when vertical interpolation is involved. The difference, Δ c = c
. Oceanographers have constructed to include inhomogeneities and anisotropies associated with the presence of topography, and to reflect in a way the adaptation of the ocean fields to the topography. Utilization of ocean topography may change the weighting operation, in (1) , into a mathematical operator, , that maps the innovation (at the observational points) directly onto the grid points, where could be different in (1) and (5) when vertical interpolation is involved. The difference, Δ c = c
prelimina~ one. This restriction isnot as harmful as it first appears since, at the expenseof noise in the analyzed field (and thus the derived468 MONTHLY WEATHER REVIEW VOLUM- 107 TABLE 1. Statistical error analysis comparison between Gaussian interpolation and variational adjustment of a preliminarywind analysis.Variationalwind adjustment Gaussianrms Algebraic rms Algebraicu
prelimina~ one. This restriction isnot as harmful as it first appears since, at the expenseof noise in the analyzed field (and thus the derived468 MONTHLY WEATHER REVIEW VOLUM- 107 TABLE 1. Statistical error analysis comparison between Gaussian interpolation and variational adjustment of a preliminarywind analysis.Variationalwind adjustment Gaussianrms Algebraic rms Algebraicu
simplified and can be solved algebraically. A scale analysis of the full transport equations is offered as partialjustification for the present approach in the case of nearly isotropic turbulence. The problem studied is that of a well-mixed layer bounded above by a region of strong stable stratification. The present model gives a significant improvement in the representation of the large-scale variables as compared with the more conventional eddy viscosity approach. In three experiments
simplified and can be solved algebraically. A scale analysis of the full transport equations is offered as partialjustification for the present approach in the case of nearly isotropic turbulence. The problem studied is that of a well-mixed layer bounded above by a region of strong stable stratification. The present model gives a significant improvement in the representation of the large-scale variables as compared with the more conventional eddy viscosity approach. In three experiments
reviewed current knowledge of the diffusivity of turbulence diffusivities throughout the oceans. Estimates of this parameter come from several sources, including direct measurements, parameterizations of oceanic finestructure, and indirect estimates based on algebraic and statistical inversions of hydrography. While each of these methods require assumptions with potential limitations, results are generally consistent among water mass–based comparisons. Diffusivities in the ventilated waters of the
reviewed current knowledge of the diffusivity of turbulence diffusivities throughout the oceans. Estimates of this parameter come from several sources, including direct measurements, parameterizations of oceanic finestructure, and indirect estimates based on algebraic and statistical inversions of hydrography. While each of these methods require assumptions with potential limitations, results are generally consistent among water mass–based comparisons. Diffusivities in the ventilated waters of the
Basin, Coast Ranges. Antillian Mountain Sys-tem: position; extent; characteristics; subdivisions-Greater Antilles, Lesser Antilles, Bahamas, Trinidad-Tobago group, Mountains of Cen- tral America.LECTURE 11.SUBJECT.-CLIMATOLOGY AND HYDROGRAPHY. vaiues and the afilication of this climhdogical knowledgeto the benefit of mankind. Practical meteorology implies C~vbatolog#.-Definition of climate: precipitation: evaporation; cir-daily weather map and the study and prediction of 6tornls I heat in atmosphere
Basin, Coast Ranges. Antillian Mountain Sys-tem: position; extent; characteristics; subdivisions-Greater Antilles, Lesser Antilles, Bahamas, Trinidad-Tobago group, Mountains of Cen- tral America.LECTURE 11.SUBJECT.-CLIMATOLOGY AND HYDROGRAPHY. vaiues and the afilication of this climhdogical knowledgeto the benefit of mankind. Practical meteorology implies C~vbatolog#.-Definition of climate: precipitation: evaporation; cir-daily weather map and the study and prediction of 6tornls I heat in atmosphere
minus sign (-) if the ships barometer reads higher than tlie standard. Divide the algebraic sum of these differ- mces by the total number of readings and enter the result at the footIf the column, prefixing the proper sign. All readings should be to the nearest hundredth.of an inch and no urther. Promptly forward the completed cards to the main office. Comparisons should be made on several different days; not several )n tlie same day. Readings on at least three (3) different days are nec- mary for a
minus sign (-) if the ships barometer reads higher than tlie standard. Divide the algebraic sum of these differ- mces by the total number of readings and enter the result at the footIf the column, prefixing the proper sign. All readings should be to the nearest hundredth.of an inch and no urther. Promptly forward the completed cards to the main office. Comparisons should be made on several different days; not several )n tlie same day. Readings on at least three (3) different days are nec- mary for a
30- veering in westerly flow. Boundary-layer trajectory estimates made from geostrophic vectors are easily constructed graphicallyon sea level weather charts, and trajectory forecasts can be made by using National Weather Service foreeast maps distributed by facsimile. L~yer-average wind and adjusted surface wind trajectories are moresuited to post analysis by computer since the data are available on magnetic tapes and the wind vector dataare processed objectively.1. Introduction In
30- veering in westerly flow. Boundary-layer trajectory estimates made from geostrophic vectors are easily constructed graphicallyon sea level weather charts, and trajectory forecasts can be made by using National Weather Service foreeast maps distributed by facsimile. L~yer-average wind and adjusted surface wind trajectories are moresuited to post analysis by computer since the data are available on magnetic tapes and the wind vector dataare processed objectively.1. Introduction In
