Search Results
all FCC-positioned transosondeflights which traversed t'his area a t 300 and 250 mb.Since it was only legitimate to make the comparisonsat synoptic map time, only about 200 geostrophic velocitydifferences went into figure 3 wit'h the averctge numberof comparisons varying from about three per 5' liititdc-longitude area in the belt' of rnaxirnum flight frequencybetween40' and 45' IT., to twa comparisons per unitarea between 50' and 55' N., :wd one comparison perunit area between 15' and 20' N. The
all FCC-positioned transosondeflights which traversed t'his area a t 300 and 250 mb.Since it was only legitimate to make the comparisonsat synoptic map time, only about 200 geostrophic velocitydifferences went into figure 3 wit'h the averctge numberof comparisons varying from about three per 5' liititdc-longitude area in the belt' of rnaxirnum flight frequencybetween40' and 45' IT., to twa comparisons per unitarea between 50' and 55' N., :wd one comparison perunit area between 15' and 20' N. The
efficiency, and(iii) simplicity of implementation. Its implementation is demonstrated on a set of pressure datg collectedby CLASS.1. Introduction The National Center for Atmospheric Research hasdeveloped a radiosonde system named Cross-ChainLORAN Atmospheric Sounding System (CLASS). Itis planned to employ this new system in operationalfield projects where the data will be distributed to theresearch community in real time for comparison andpooling with other systems to perform real-time analyses and
efficiency, and(iii) simplicity of implementation. Its implementation is demonstrated on a set of pressure datg collectedby CLASS.1. Introduction The National Center for Atmospheric Research hasdeveloped a radiosonde system named Cross-ChainLORAN Atmospheric Sounding System (CLASS). Itis planned to employ this new system in operationalfield projects where the data will be distributed to theresearch community in real time for comparison andpooling with other systems to perform real-time analyses and
–Weiss parameter. The comparison of trajectories obtained with these two methods showed that both sets of trajectories presented similar patterns (not shown). Last, the complete set of the 213 maps of the Okubo–Weiss parameter for the whole basin, with vortices labeled automatically as described before, has been visually inspected, showing that there were few errors in the trajectories obtained with the automatic method. 5. Discussion The application of the Okubo–Weiss criterion has shown a basin full of
–Weiss parameter. The comparison of trajectories obtained with these two methods showed that both sets of trajectories presented similar patterns (not shown). Last, the complete set of the 213 maps of the Okubo–Weiss parameter for the whole basin, with vortices labeled automatically as described before, has been visually inspected, showing that there were few errors in the trajectories obtained with the automatic method. 5. Discussion The application of the Okubo–Weiss criterion has shown a basin full of
role in the computation of the principal mass and energy fluxes. In the literature these parameters are usually defined using soil texture maps ( Rawls and Brakensiek 1985 ), but problems of representativeness arise owing to pixel heterogeneity. Satellite images of land surface temperature can help in the calibration of these parameters in each pixel of the analyzed domain, overcoming the traditional calibration based on a single multiplicative value retrieved from the comparison between observed
role in the computation of the principal mass and energy fluxes. In the literature these parameters are usually defined using soil texture maps ( Rawls and Brakensiek 1985 ), but problems of representativeness arise owing to pixel heterogeneity. Satellite images of land surface temperature can help in the calibration of these parameters in each pixel of the analyzed domain, overcoming the traditional calibration based on a single multiplicative value retrieved from the comparison between observed
Bemmelen's Table 1 in Met. Zeit., May 1924 p. 134. Arrows fly with the wlnd. Velocities in m. p. s., each feather equaling 1 m. p. s. At 10-Inn. altitude and below, tenths of D m. p. s. m approximatelp &&nted by the frnctional lengths of a fe8the.rS ~M B E R , 1924 MONTHLY WEATHER REVIEW 448melen's table into graphic form (fig. 1) that the great seasonal shifts of theairstreams over western Java may be more clearly visualized and a comparison made easywith his map showing conditions at the
Bemmelen's Table 1 in Met. Zeit., May 1924 p. 134. Arrows fly with the wlnd. Velocities in m. p. s., each feather equaling 1 m. p. s. At 10-Inn. altitude and below, tenths of D m. p. s. m approximatelp &&nted by the frnctional lengths of a fe8the.rS ~M B E R , 1924 MONTHLY WEATHER REVIEW 448melen's table into graphic form (fig. 1) that the great seasonal shifts of theairstreams over western Java may be more clearly visualized and a comparison made easywith his map showing conditions at the
10 20 30 40 [msq Horizontal windFIG. 4. Comparison of the horizontal wind profileat the crest of the two-dimensional mountain.ordinates. The computational domain was a 4508 kmx 4508 km area in the map coordinates. The horizontalmesh width was 92 km. The vertical depth was 6000 m;zt = 6000 m was assumed. The vertical mesh numberwas 20, and the mesh width varied from 100 m (bpttomlayer) to 500 m (top layer). The input meteorological data were meteorologicalfields
10 20 30 40 [msq Horizontal windFIG. 4. Comparison of the horizontal wind profileat the crest of the two-dimensional mountain.ordinates. The computational domain was a 4508 kmx 4508 km area in the map coordinates. The horizontalmesh width was 92 km. The vertical depth was 6000 m;zt = 6000 m was assumed. The vertical mesh numberwas 20, and the mesh width varied from 100 m (bpttomlayer) to 500 m (top layer). The input meteorological data were meteorologicalfields
-look metrics. 3. Guidelines for metrics Figure 1 presents the diurnal harmonic amplitude and phase from the observations. Since warm seasons have similar dynamics, Fig. 1 combines Northern Hemisphere July and Southern Hemisphere January in both maps. The resulting discontinuity at the equator is small. (Corresponding cold season maps provide little additional information because coherent diurnal variation outside the tropics is small; cf. Figs. S2–S5 in the supplemental material.) The diurnal
-look metrics. 3. Guidelines for metrics Figure 1 presents the diurnal harmonic amplitude and phase from the observations. Since warm seasons have similar dynamics, Fig. 1 combines Northern Hemisphere July and Southern Hemisphere January in both maps. The resulting discontinuity at the equator is small. (Corresponding cold season maps provide little additional information because coherent diurnal variation outside the tropics is small; cf. Figs. S2–S5 in the supplemental material.) The diurnal
measurement sites using acoustic tomography. Together with a conventional data survey one can derive the validity of well-known turbulence theories, which normally require horizontal homogeneity regarding the mean meteorological quantities ( Raabe et al. 2002 ). An open question, which will be investigated in this study, is the comparison of tomographically obtained and conventionally derived point data. The following section describes the acoustic tomography method and its applicability to measurements
measurement sites using acoustic tomography. Together with a conventional data survey one can derive the validity of well-known turbulence theories, which normally require horizontal homogeneity regarding the mean meteorological quantities ( Raabe et al. 2002 ). An open question, which will be investigated in this study, is the comparison of tomographically obtained and conventionally derived point data. The following section describes the acoustic tomography method and its applicability to measurements
selected points is shown in Table 3 , with an illustration for two of them shown in Fig. 7 . Considering these results, one has to keep in mind several peculiarities of the problem. As pointed out above, the HIRLAM fluxes are averaged between the output times (i.e., these are the 3-h mean values). The SILAM values are based on profiles taken at a specific HIRLAM time step and thus practically “instantaneous.” The comparison domain covers several time regions, therefore at every time the map includes
selected points is shown in Table 3 , with an illustration for two of them shown in Fig. 7 . Considering these results, one has to keep in mind several peculiarities of the problem. As pointed out above, the HIRLAM fluxes are averaged between the output times (i.e., these are the 3-h mean values). The SILAM values are based on profiles taken at a specific HIRLAM time step and thus practically “instantaneous.” The comparison domain covers several time regions, therefore at every time the map includes
PDFs are due to coherent vortices in a semienclosed basin such as the Mediterranean basin. The Mediterranean Sea is dominated by the entrance of freshwater incoming from the Atlantic Ocean through the Strait of Gibraltar. The instability of this inflow and local wind action often generate coherent vortices in several parts of the basin that enhance the mixing of these incoming light waters with the saltier resident waters (e.g., Millot 1999 , 2005 ). Analysis of altimetric maps shows that PDFs of
PDFs are due to coherent vortices in a semienclosed basin such as the Mediterranean basin. The Mediterranean Sea is dominated by the entrance of freshwater incoming from the Atlantic Ocean through the Strait of Gibraltar. The instability of this inflow and local wind action often generate coherent vortices in several parts of the basin that enhance the mixing of these incoming light waters with the saltier resident waters (e.g., Millot 1999 , 2005 ). Analysis of altimetric maps shows that PDFs of
