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# Atlantic coast cyclogenesis

Harvey W. Halbert

values represent the algebraic averageof a large number of individual values, some positiveand some negative.Professor Beers fails to distinguish between neglecting a term as small in comparison with larger termsand neglecting it in comparison with other terms of thesame order of magnitude. Consider equation (3) frommy paper:idp awdt az-_ 4- - = - div V.The approximate magnitude of the three terms islo+, and sec-', respectively. Therefore,(l/p)dp/dt may be neglected without doing violenceto the

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JAMES E. MILLER

values represent the algebraic averageof a large number of individual values, some positiveand some negative.Professor Beers fails to distinguish between neglecting a term as small in comparison with larger termsand neglecting it in comparison with other terms of thesame order of magnitude. Consider equation (3) frommy paper:idp awdt az-_ 4- - = - div V.The approximate magnitude of the three terms islo+, and sec-', respectively. Therefore,(l/p)dp/dt may be neglected without doing violenceto the

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Robert G. Fleagle

values represent the algebraic averageof a large number of individual values, some positiveand some negative.Professor Beers fails to distinguish between neglecting a term as small in comparison with larger termsand neglecting it in comparison with other terms of thesame order of magnitude. Consider equation (3) frommy paper:idp awdt az-_ 4- - = - div V.The approximate magnitude of the three terms islo+, and sec-', respectively. Therefore,(l/p)dp/dt may be neglected without doing violenceto the

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# Magnitude of horizontal divergence

Norman R. Beers

values represent the algebraic averageof a large number of individual values, some positiveand some negative.Professor Beers fails to distinguish between neglecting a term as small in comparison with larger termsand neglecting it in comparison with other terms of thesame order of magnitude. Consider equation (3) frommy paper:idp awdt az-_ 4- - = - div V.The approximate magnitude of the three terms islo+, and sec-', respectively. Therefore,(l/p)dp/dt may be neglected without doing violenceto the

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# COMPUTATION OF STREAMLINES FROM THE PRESSURE FIELD

Robert C. Bundgaard

with I.At least 63 (75) per cent of the time, term I is 10 (4)times larger than term 11, or more. These statisticswere based upon 236 comparisons of terms I and 11.These comparisons were made from ten consecutive1500 GCT 500-mb maps beginning with 13 February1953. From each map, these comparisons were madefrom a geographical grid of 48 points equally spacedover the United States. In these comparisons, thefields of wind and pressure were analyzed independently; their functions I and I1 in (5) were

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# FORECASTING THE SPEED OF MOVEMENT OF SELECTED CYCLONES ALONG UPPER-AIR STEERING CHANNELS

Ernest M. Rampey

. Sea-level weather map; 1830 GCT 25 December 1950.JUNE 1953ERNEST M. RAMPEYFIG. 3. 850-mb chart; 1500 GCT 25 December 1950.culation at sea level, 850 and 700 mb, but not at500 mb. 500 mb.chosen for type I is 700 mb, while that for type I1 isThus, lows which appear on the sea-level map, butwhich are not closed at 850 mb, are not included.5. Type I : Evaluation of temperature advectionSimilarly, lows which are closed at 500 mb and higherhave been excluded from this investigation.As will be shown

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# The Near-Real-Time, Global, Four-Dimensional Analysis Experiment During the GATE Period, Part I

K. Miyakoda
,
L. Umscheid
,
D. H. Lee
,
J. Sirutis
,
R. Lusen
, and
F. Pratte

NMC level. III data werein general available twice a day at 0000 and 1200 GMT,and were used for comparison together with the level IIIdata (map) of ANMRC (Australian Numerical Meteorology Research Centre) in Melbourne.564 JOURNAl. OF THE ATMOSPHERIC SCIENCES VO~.UME339 SEP 197400 GMTSURFACEFro. lc. FIo. 1. Examples of data maps for 00 GMT=t=3 h, 9 September 1'974. (a) 200 mb map includes the data in the layer

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# Dynamics of 2-Day Equatorial Waves

Patrick T. Haertel
and

for stratiform instability and convectively coupled waves. J. Atmos. Sci , 58 , 1567 â€“ 1584 . Majda , A. J. , B. Khouider , G. N. Kiladis , K. H. Straub , and M. G. Shefter , 2004 : A model for convectively coupled tropical waves: Nonlinearity, rotation, and comparison with observations. J. Atmos. Sci , 61 , 2188 â€“ 2205 . Mapes , B. E. , 1998 : The large-scale part of tropical mesoscale convective system circulations: A linear vertical spectral band model. J. Meteor

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# A THREE-DIMENSIONAL STUDY OF THE HORIZONTAL VELOCITY DIVERGENCE

Holbrook Landers

thelines on a transparent overlay, shown in fig. 2, wasplaced on a point where the smoothed value was tobe computed. The line b-d was always oriented northsouth. The smoothed value obtained was equal to(a+l.+c+d+e)/S, and the distance (f) was equal to25 deg lat. A comparison of a smoothed map with anunsmoothed map showed about what would be ex= 1 Xsec-I, 8 X 23 Xsurface of non-divergence might be located from thetwelve cross sections. It resulted that a surface of leastdivergence could be located at

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# THE RELATIVE IMPORTANCE OF DIFFERENT HEAT-EXCHANGE PROCESSES IN THE LOWER STRATOSPHERE

Wan-cheng Chiu
and
Richard S. Greenfield

change ofabout 0.1C in 12 hr at these latitudes. As may be seen later, thisis smaller than R2At. For the purpose of this study, equation (12)is sufficient.2 74 JOURNAL OF METEOROLOGY VoLixI?: 16FIG. 1. Positions of an air particle and of an isobaric surface at two different times.a finite interval of timei.e., AAt, may be evaluatedfrom data on isobaric maps.In fig. 1, surfaces p(tl) and P(t2) represent thehypothetical positions of an isobaric surface at timestl and t2, respectively. B(x2, y

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