Kational Bureau of Standards

Library, N.W. Bldg

OCT 2 61952

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\ SYNOPTIC RADIO METEOROLOGY

B. R. BEAN, J. D. HORN,

AND L P. RIGGS

! U. S. DEPARTMENT OF COMMERCE

NATIONAL BUREAU OF STANDARDS

;'
[E NATIONAL BUREAU OF STANDARDS

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NATIONAL BUREAU OF STANDARDS

technical ^v2cte

98

OCTOBER 1962

SYNOPTIC RADIO METEOROLOGY

B. R. Bean, J. D. Horn, and L P. Riggs

NBS Boulder Laboratories

Boulder, Colorado

NBS Technical Notes are designed to supplement the Bureau's regular publications program. They provide a means for making available scientific data that are of transient or limited interest. Technical Notes may be

listed or referred to in the open literature.

For sale by the Superintendent of Documents, U.S. Government Printing Office Washington 25, D.C. - Price 50 cents

Contents

Page

ABSTRACT iv

1. Introduction ,,,, ......••*.. 1

2. Background 1

3. Refractive Index Parameters 11

4. A Synoptic Illustration 16

5. Surface Analysis in Terms of N . # . . 18

6. Constant Pressure Chart Analysis ,,.... . 21

7. Vertical Distribution of the Refractive Index Using A Units , . 22

8. Summ.ar'9^ . 25

References 27

111
ABSTRACT

A survey of some of the advances in the field of synoptic radio

meteorology is presented. The developnrient of representative refractive index profiles for major air mass types is reviewed. Included is a description of several refractive index parameters currently in use

by radio meteorologists. Two reduced-to-sea-level index forms

developed at the National Bureau of Standards are used to illustrate

the three-dimensional structure of a broad-scale storm system traversing the North American continent.

IV
SYNOPTIC RADIO METEOROLOGY

B. R. Bean, J. D. Horn, and L. P. Riggs

1

.

Introduction

The variation of refractive index structure in the troposphere

may be related to synoptic tropospheric disturbances. Within the

scope of the synoptic field are time-wise and space-wise variations in

the atmosphere from microscale fluctuations to broad-scale systems

of continental dimensions.

The microscale fluctuations of the refractive index are those

that one would expect to observe at a particular point along a radio

path. They reflect detailed terrain and weather conditions in the immediate vicinity of the transmitter or receiver site.

Mesoscale variations, by way of contrast, are those which cover

tens of kilometers and thus encompass a substantial portion of a radio

path. Examples of this type of variation are land-sea breeze effects

and convection cells of thunderstorm activity.

Large-scale weather systems, affecting vast areas, perhaps even

on a continental scale, fall under the classification of macroscale variation. Examples of this type of activity in the atmosphere are sweeping

air mass changes and frontal systems traversing thousands of kilometers

on the earth's surface. A detailed analysis of such a system is given as

an illustration later in this technical note.

2. Background

The radio refractive index, n, may be defined in terms of its

scaled-up value, N = (n-l)lO , from the Smith -Weintraub relation [ 1953]:
-2-

where P is the observed pressure in raillibars (mb),

T is the observed temperature in K, and

e is the partial pressure of water vapor in mb. The SmithWeintraub constants yield an overall accuracy of ± 0.5 percent in N for

the frequency range 30 Mc - 30 kMc For practical work in radio

meteorological studies, (1) may be simplified to a two-term expression

N = D + W, (2)

where D, the "dry term", is given by

D = 77.6 |- (3)

and W, the "wet term", by

W = 3.73 X 10^ -^ . (4)

The problem of determining the vertical and horizontal distribution

of the radio refractive index has engaged the attention of radio meteorologists for the better part of two decades [Sheppard, 1946; Gerson, 1948;

Perlat, 1948; Randall, 1954; Misme, 1957; Hay, 1958].

By analysis of current synoptic conditions from standard weather

charts, one may ascertain the characteristics of an air mass appearing

over a given region and, likewise, may predict with reasonable accuracy

the air mass type and consequent changes in atmospheric structure expecte

over a particular locale in, say, 24 hours. Then, from a knowledge of

air mass profile characteristics [Bean, Horn, and Riggs, 1959] one may

estimate the departures of refractive index (and radio ray bending) from

normal for a certain region. The bending predictions permit an estimate

of refraction errors and the introduction of appropriate corrections for

radio range and elevation angle errors in radio navigational equipment.
-3-

VHF-UHF radio field strengths beyond the normal radio horizon

will also differ from air mass to air mass. It has been known for many

years that the seasonal cycle of VHF radio field strengths received far

beyond the normal radio horizon was correlated with the refractive

index [ Pickard and Stetson, 1950a; b; Bean, 1956; Onoe, 1958] and that

significant changes in field strength level are observed from air mass to

air mass [Hull, 1935; 1937; England, Crawford, and Mumford, 1938].

Speaking about signal level on a 60 Mc/ s beyond-the-horizon radio path

near Boston, Massachusetts, Hull [ 1935] states that during the winter

low signal levels prevail during the presence over the path of fresh polar

air. Periods of high signal level occur when a cold, dry polar air mass is

overrun by warm, moist air of tropical maritime origin. Hull's analysis

represents early recognition of refraction and reflection phenomena on

a synoptic scale. Later work on seasonal changes of fields and N

represents, in a way, a summary of synoptic conditions over a period

of time. Gerson [ 1948] was one of the first to consider the variation of

the radio refractive index, n, in terms of seasonal and air mass changes.

Gerson divided n into two parts, one density-sensitive and the other moisture-sensitive. This division is equivalent to the wet- and dry-term

separation of N = (D + W) in equation (2). Gerson was able to measure

seasonal thermal changes by variation in the dry term and seasonal

moisture changes by observed variation in the wet term. His graphs

show a sinusoidal variation of the dry term with a warm season trough

and a cool season crest, indicating density changes in inverse proportion

to the temperature. The wet term component of n, on the other hand, was

observed to attain its maximum during the warm season when the dry term

was at its minimum. In arctic and antarctic locales the surface variation

of the wet term was found to be quite small, while in temperate and

tropical climates there was a sizable annual variation of the moisture
component. Yerg in 1950 showQ'd that even during the long cold

arctic night vertical variations in moisture made significant contributions to the N profile. Apparent ducting gradients, obtained by neglecting

the wet term at low temperatures, may in actuality be only slightly more

refractive than standard.

Continuing his investigation, Gerson next turned to the analysis

of refractive index changes within various air masses. Using air mass

data available in the meteorological literature of the day, he charted

mean refractive index profiles for different air mass types. The largest

initial values and also the largest vertical gradients of n occurred with

tropical maritime air. The air mass with the weakest gradients and,

therefore, the poorest refraction properties was found to be the polar

continental type. Common to all of Gerson's air mass refractive index

graphs is an approximately exponential decrease of n with respect to

height. In 1933 Schelleng, Burrows, and Ferrell attempted to remove

this systematic n-decrease with height by utilizing a correction factor

of linear form. However, this method of correction leads to serious

over-estinaation of refraction effects that becomes steadily more pronounced within increasing altitude (in the more modern problem of sattellite telecommunications). [Bean, 1962]

The work of Hay [ 1958] confirmed and extended the observations

Gerson had made concerning air mass profiles. Measuring air mass

characteristics at Maniwaki, Quebec, Hay concluded that each large-scale

air mass type in central Canada had a distinctive refractive index profile.

Hay determined the height distribution of N for four basic air masses by

fitting a second degree polynomial to each of the four sets of air mass

data, indicating that an average N profile cannot be approximated effectively by a linear curve except over small height increments. Hay

obtained further discrimination by constructing a "dry-term" curve for
-5-

each air mass. The dry-term curves display a smaller standard

deviation than the total N curves for all air masses except the continental

arctic, which is normally very dry. The largest variations in total N

are due to fluctuations in the wet term. The saturation vapor pressure

is approximately an exponential function of the temperature, so that

during the warm season norraal temperature changes cause the saturation

vapor pressure, and therefore the wet term, to vary sharply.

Hay's discussion [ 1958] of the use of N profiles to estimate correction for radio ray refraction includes a table of mean effective earth's

radius factors calculated within 95 percent probability limits for each of

four air masses.

Misme [ 195 7] has studied synoptic radio meteorology in connection

with telecommunications networks in France and North Africa. His discussions include considerations of vertical gradients of the refractive

index and atmospheric reflection of radio waves.

A reasonable question at this point is to what extent are model

exponential atmospheres applicable to various climatic zones around the

earth. While it is readily apparent that individual profiles vary widely

from any sort of exponential norm, there is an increasing amount of

experimental evidence [Misme, Bean, and Thayer, I960] which shows

that long-term averages of synoptic refractive index variations do tend

toward an exponential form with respect to height. Indeed, the five-year

mean N profiles of figures 1 and 2, representing arctic and tropical

climates respectively, bear out this contention by showing close agreement

with models developed from mid-latitude data. The examples verify the

results obtained by Gerson [ 1948] for various air masses.

In 1954 Randall investigated the relationship of surface meteorological data to surface N (N ) and to field strength in the FM frequency band.

The results described were drawn from a very limited data sample that
-6-

i covered less than a month during the summer of 1947. Within the

framework of this specialized study, however, Randall found that polar

continental air masses were associated with low field strengths and low

N , while tropical maritime air masses were associated with high field

strengths and high N , as shown in figure 3. Randall advanced the

hypothesis that the observed field strength changes were due to the existence of characteristic N profiles typical of each air mass type. Randall

was curious also as to the behavior of N and radio fields during the passage

of fronts and squall lines. Figure 4 shows the results of his investigation

and indicates that definite field strength changes may occur during frontal

and squall line passage. Caution should again follow in the interpretation

of these results since they represent but a single example of frontal and

squall line passage.

Gray [ 1957] made studies of the correlation of N and the gradient

of N with path losses at UHF frequencies for observing points representativ

of various climatic areas around the world and concluded that changes in

trans -horizon telecomnnunications were strongly dependent on atmospheric

changes

.

Recently Gray [ 196 l] considered radio propagation and related

meteorological conditions over the Caribbean Sea. Utilizing the effective

earth's radius factor as a representative index, he developed an empirical

curve of annual median scatter loss versus effective propagation distance

for both Caribbean and temperate regions. Effective distance as defined

by Gray is the angular distance in radians multiplied by the radius of

the earth modified for normal refraction. Gray reports that the refractive

gradient in the first 100 meters is in general the determining factor in

median scatter loss for transhorizon telecommunications, as one would

expect from earlier refraction studies [Bean and Thayer, 1959a] .
-7-

Other studies on refraction problems during the past decade

have led to systematic computation of refraction effects, and to significant

applications such as the evaluation of radar elevation angle errors in

differing air masses and climates [Schulkin, 1952; Fannin and Jehn, 195 7] . Schulkin advanced a practical and very fundamental method for numerical

calculation of atmospheric refraction (radio ray bending) from radiosonde

data. Figure 5, after Schulkin, gives mean angular bendings for radio

rays passing completely through the earth's atmosphere for two extremes

of air mass type. Fannin and Jehn concluded that a particular refractive

index profile depends on air mass type and the climatic controls of season

and latitude. Their conclusion was substantiated by mean N profiles for

thirty -four weather observing sites located in or near four distinct air

mass source regions about the world. These data show that a definite

difference does exist in the profiles of various air masses. Refraction

effects were found to be largest in tropical maritime air masses, intermediate in polar continental and polar maritime, and least in tropical continental air masses. Fannin and Jehn also published graphs showing dayto-day variations in profiles (representing the effects of air mass changes

over a given observing station) and graphs of diurnal profile variations.

Bean, Horn, and Riggs [ I960] demonstrated that radio ray refraction within the lower layers of an air mass is mirrored by the difference between the observed refractive index structure and that of a standard

atmosphere. Figure 6 shows a graph of bending, t, plotted with a modified

refractive index profile representative of summertime tropical maritime

air. It is apparent that near the ground bending departures reflect refractive index profile departures from standard. Figure 7 presents a series of

graphs of departures of refractive index and bending from normal for each

air mass and emphasizes the close relation between the two. This affords

the synoptic radio meteorologist a set of standard reference profiles for
-8-

the study of a given air mass or the confluence of contrasting air

masses at a frontal zone.

Arvola [ 1957] discussed the changes in refractive index profiles

caused by migratory weather systems. He examined a series of synoptic

situations that gave rise to greater -than-normal refraction in the midwestern portion of the United States during November, 1951. Ridges

and accompanying subsidence effects generally gave rise to strong N

gradients and enhanced signal strength over a 200 km link broadcasting

at 71.75 Mc. Refractive gradients were stronger in the warmer air

masses and at the times when moist air was present below the inversion

created by the subsidence mechanism. Strong gradients which appeared

behind a squall line later weakened with the approach of a cold front. After

the passage of this front, stratification in the cold air again increased the

gradient.

Subsequent investigations of polar continental air across central

North America have made use of reduced-to-sea-level forms of the radio

refractive index as synoptic parameters. The reduced forms are sensitive

indicators of synoptic changes and afford a clearer picture of storm structure than that obtained using analyses in terms of unreduced N or B units

(defined by equation 6).

Jehn [ 1960a] at the University of Texas used a form of the potential refractive modulus, <j), (see equation 11) developed by Lukes [ 1944]

and Katz [ 1951] to account for the height dependence feature of the refractive

index. (When referenced to the 1000 mb level, cj) is termed K by Jehn. ) Articles by Jehn on synoptic climatology in I960 [b] and 1961 use composite

analysis techniques to study the synoptic properties of the Texas-Gulf cyclon«

and the Central-United-States type of cold outbreak.

In another application of the potential refractive modulus, Flavell

and Lane [ 1962] utilized Katz's K unit to study tropospheric wave propagatioi
-9-

Field strength measurements on VHF-UHF transhorizon radio links over

the British Isles were analyzed with cross sections in terms of K and

regional charts of AK (the difference between K at the surface and at the

850 mb level). These charts show features similar to those obtained by

the use of N or A, as defined by equations 5 and 7 respectively.

Flavell and Lane recorded a series of measurements on a 500 km

path at 877 Mc on which the received signal was ordinarily below the noise

level. The singular occasions on which the received signal could be measured at the normal times of radiosonde ascent all exhibited a symmetric

variation of AK over the transmission path. These results lend credence

to the hypothesis that synoptic disturbances play an important role in

transhorizon telecommunications

.

Moler and Arvola [ 1956] advanced the hypothesis that the vertical

gradient of the refractive index is affected by broad-scale vertical motion

in the troposphere and suggested that moisture and temperature stratification is modified principally by changes in vertical velocity. This latter

work was extended [Moler and Holden, I960] by a study of mesoscale

centers of horizontal air mass convergence and divergence in the troposphere. Horizontal convergence takes place in a low pressure area,

where the winds around the low have a predominant component toward a

local vortex at the center. Upward vertical motion results from the pileup of air in the vortex region. In a high pressure area winds have a predominant component away from the center of the high (divergence) and subsiding air descending from higher levels takes the place of air transported

outward from the center. Local convergence implies upward vertical

motion in the lower levels of the troposphere, while local divergence

implies downward vertical motion in the lower levels . It follows that local

convergence centers (small-scale low pressure cells) produce updrafts in

the atmosphere that result in considerable m.ixing and the destruction
-10-

o£ atmospheric layers. Centers of divergence (small-scale high pressure

cells) create strong temperature and humidity inversions by the motion

of subsiding air. Such inversions produce large vertical refractive index

gradients that partially reflect microwaves traveling through this meteorological environment [Gossard and Anderson, 1956] . In a well-mixed

atmosphere, on the other hand, the primary propagation mechanism is

believed to be scattering by turbulent fluctuations of the refractive index

[Megaw, 1950; Booker and Gordon, 1950].

Sea level measurements studied by Moler and Holden [ I960] showed

N to be essentially invariant during the period of observation, yet signal

levels varied by more than 60 db. Since scattering theory would account

for a rise in signal level of only about 13 db, Moler and Holden concluded

that refractive layering and thermal stability over the oceans, principally

functions of vertical wind velocities, contribute significantly to the high

signal levels. These conclusions are similar to the findings of Saxton

[ 1951] and Flavell and Lane [ 1962] that high signal levels from a distant

transmitter may well be the consequence of refractive layering and subsequent reflection of radio energy by turbulent eddies and the effects of

superrefraction of radio waves produced by departures from normal of

the height variation of the tropospheric refractive index.

A knowledge of the vertical motion of the atmosphere becomes

at this point central to the problem of refractive layering. The relative

magnitude and direction of the vertical component of the wind velocity may

be estimated by a method outlined by Moler and Holden [ I960] .

In the same article Moler and Holden give a description of the

large signal enhancement and deep fading that occurs as the propagation

mechanism varies between partial reflection and scattering on a trans

horizon radio path along the California coastline. Reflection occurs when

strong refracting layers are present within a kilometer of the surface.
-11-

typifying meteorological conditions generally associated with the subsidence inversion frequently found along the California coast.

Figure 8 shows the sea level pressure chart and a series of

streamline analyses by Moler and Holden depicting mesoscale centers

of convergence and divergence for a day in March along the southern

California coast. Figure 9 shows the X-band signal level received at

Point Loma, San Diego (SD) from Santa Barbara (SB) during the same

day. As the centers of convergence along the radio path weaken, refractive layers are formed and the signal level rises sharply during the middle

of the day. Later the signal level lowers again with the regeneration of

convergence centers and the destruction of stratified layers during the

afternoon hours.

3. Refractive Index Parameters

Later in this Technical Note the analysis of a synoptic disturbance

in the troposphere will be described in detail. Certain reduced forms of

the refractive index that w^ill be useful in the ensuing discussion will be

developed here.

Figure 10 shows contours of the mean value of N at the surface,

N , determined from eight years of data for August, 0200 local time.

Miniature circles indicate the sixty-two observing stations from which

N data were available. It is evident that coastal areas display high values

of N as compared with inland locations. Low values of N are apparent

along the Appalachian mountain chain and in the great mountain systems

and intermountain plateaus of the western United States. There is a marked

similarity between the N contours on figure 10 and the elevation contours

of figure 11. N , as a sensitive indicator of changes in atmospheric density, displays a strong elevation dependence. To remove this effect a reduced-to-sea-level expression, Nq, is introduced:

N = N exp -^ , (5) o s "^ H*
-12-

where z is height in km and H*= 7. km is the scaled height. Scale height is

the height at which the mean value of N has decreased to a fraction, l/ e,

of its initial value where

e = 1 + -V + TT + • • • = 2.71828- ••

A scale height of 7. km is in close agreement with H* - 7. 01 km for

the NACA standard atmosphere with 80 percent relative humidity and

H* = 6. 95 km obtained from climatic studies utilizing over two million

observations of the variation in N over the first km above the surface of

the earth [Bean and Thayer, 1959a] . The N contours of figure 12 utilize

the same data as figure 10. The use of Nq produces a simpler map with

a smaller range of variation. Additionally, N may easily be estimated

from the smooth and slowly-varying contours of N if the station elevation

is known. Numerous tests have shown that N may be more accurately

estimated from charts of N than from charts of N itself, by a factor of

four or five to one [Bean, Horn, and Ozanich, I960] . The attempt to find a workable method to compensate for the

decrease of N with increasing height has brought about the development of

various model atmospheres. [Bean and Thayer, 1959a; Bean, 1962.]

Specifically, CRPL model refractive index atmospheres were developed by

Bean and Thayer in 1959 [a] . The steps in this development that are

relevant to synoptic studies are outlined briefly.

Vertical refractive index cross sections are standard working

charts for synoptic studies. Such charts constructed from observed values

of N suffer from a serious shortcoming in that the natural decrease of N

with respect to height effectively masks contrasts between air masses in

the lower troposphere. An idealized synoptic example depicting the confluence of contrasting air masses is presented in figures 13 and 14.
-13-

When these idealized systems are analyzed in terms of N as in figures

15 and 16, the most prominent feature is the laminar structure of the

N field.

Early attempts to compensate for the decrease of N with increasing

height used the constant gradient of the effective earth's radius theory, l/4a,

where a is the radius of the earth. As an illustration, the strong elevated

layer found during the summer in southern California was studied in terms

of a linearly-corrected expression, B, given by

B = N(z) + (39.2)z, (6)

where N{z) is the value of N at height z in kilometers [Smyth and Trolese,

1947] . Since N tends to be an exponential function of height rather than

the linear function assumed by the effective earth's radius theory, the Bunit approach overcorrects when z is greater than about one km. This

point is illustrated by figures 17 and 18, where the N data of figures 15

and 16 are plotted in terms of B units. Note that the overcorrection produces a cross-section in w^hich N increases with height from a value of

310 at the surface to 360 at 5 kilometers. A function of exponential form

was designed to account for the systematic decay of density with height

that characterizes the terrestrial atmosphere, as given by [Bean, Riggs,

and Horn, 1959]

A - N(z) + 313[1 -{exp (-^-5)}]- (7)

The quantity A enables one to discern departures of N structure from the

model atmosphere

N = 313 exp{- :^ } . (8)

Further, the radio-ray bending,

^2

T i - \ cot dN • 10" , (9)

^1
-14-

where 6 is the local elevation angle of the radio ray to spherically stratified surfaces of constant N, may be approximated by [Bean and Button,

I960]

r cot 6(10- ) dA(z,313) + T(z,313). (10) 1,2 J n

The term t(z, 313) is the bending in the average atmosphere given by

(8), while the integral term represents the departures in bending produced

by various synoptic and air mass effects. The values of bending in the

average atmosphere are tabulated [Bean and Thayer, 1959b] and approximate methods of calculating the integral term in (lO) to within a few

percent have been given [Bean and Button, I960] .

In figures 19 and ZO the frontal cross sections, previously

analyzed in terms of N and B, are plotted in A units. The range of refractivity values on the new charts is reduced from more than 60 to about 25

N units, and a pattern emerges that displays sharp contrasts for air mass

differences associated with the frontal zone. Note that for the warm

front case (figure 20) the A values increase with height until they reach a maximum associated with the upgliding warm moist air overriding the

frontal surface. The region of precipitation in advance of the front is

shown as an area of high surface N. In the cold front case (figure 19) the

push of warm air aloft by the encroaching cold air is evidenced by the

"dome" of high A value just before the front. Stratification in the cold air

due to inversion effects, although inmpossible to detect in the N charts, is

clearly shown on the A unit charts.

"A" units are used in subsequent cross -section analyses presented

in this article in order to throw frontal discontinuities and air mass differences into sharp relief. The Potential Refractivity Chart of figure 21

facilitates the rapid conversion of N to A. This simplification eliminates

the necessity of using exponential tables for each individual calculation
-15-

of A and thus lends considerable ease to the preparation of charts of the

new parameter. The N and A corrections do substantially the same

thing; the primary distinction is that A is a non-linear "add-on" correction

while N is a multiplicative one. The disparity between N and A is

tabulated in table I. Table I Differences Between—N

o- and A at V arious Elevati Dns (N -A)

o

Value of N at z = Elevation

(km) 250 300 313 350 400

1 -10 -2 5 13

2 -21 -5 7 29

3 -49 -22 5 31

4 -48 -29 30 68

These figures were obtained by taking the value of A (for example, 300),

subtracting the "add-on" correction for, say, 3 km (300 - 109 = 191) and

"reducing" this number (N = 191) to zero elevation by the N "reduction",

N^ = N exp (y ).

The N = 313 exponential atmosphere is adopted for a single reference

atmosphere. The large discrepancies of table I may be avoided for

practical applications by choosing a model near the mean value of N for

the site under study.

The A unit has the additional advantage that while it is a convenient

method for height reduction the ray bending is also readily recoverable from

it, requiring only a knowledge of the altitude of the observed refractive

index measurement and the local elevation angle of the radio ray. The

potential refractive modulus of I. Katz [ 1951] ,

^ e p +b -^ ] , (11)

o 6
-16-

where 6 is the potential teraperature and e the potential vapor pressure,

is also in current use. The values of b and c of equation (11) are the

Smith-Weintraub [ 1953] constants, b - 4810 and c = 77.6. The potential

refractive modulus has been employed by Jehn [ I960] to study polar waves

over North America. N cannot accurately be recovered from cj) for bending calculations unless additional information is available: namely,

observed temperature and vapor pressure. The concept of the potential

refractive modulus arose out of the earlier refractive modulus, M, [Kerr,

1951] which is defined by

M n- 1+ ^

a X 10^ = N(z) + I - 1 X 10^, (12)

L ^ J where z = height above the earth's surface and a = earth's radius.

The M unit came into being out of an approach similar to that

J 1 which led to the development of the B unit. The condition -— = - — (a dz a radio duct) implies an effective earth of infinite radius (effective earth's

radius factor, k = °o

) [Schelleng, Burrows, and Ferrell, 1933] . The M

unit is designed so that —;— = when k = °o. M units are employed from

dz

time to time in radio meteorological analysis. The Canterbury Project

[ 1951], for example, used M unit analyses in the study of ranges of overwater radar signals near New Zealand.

4. A Synoptic Illustration

The specialized field of synoptic radio meteorology attempts a description of the variations in atmospheric refraction that arise from

large scale weather changes such as the passage of a polar front or the

movement of an air mass over a particular geographic region. The term

air mass is used to describe a portion of the troposphere that has at the

surface generally homogeneous properties. Although no air mass is in

fact homogeneous, the advantages of the air mass concept as a convenient fiction are evident in the cataloguing of meteorological observations
-17-

for climatic or synoptic purposes.

The region of interaction between the cold air of the poles and

the warm air of the tropics is referred to as the polar front and is generally located between 30° and 60°N or S. From time to time a section

of the polar front is displaced poleward by a flow of warm tropical air

while an adjacent section is simultaneously displaced toward the equator

by a flow of polar air. The interaction of the flow of polar and tropical

air results in the formation of a "wave" that moves along the polar front,

often for thousands of kilometers. An example of a fully developed polar

front wave is shown in figure 22(a), as it might appear on a weather map.

Across the Great Plains and eastern seaboard of the United States the

polar front wave normally moves along the line AB in figure 22(a), An

idealized space cross section along the line AB is shown in figure 22(b).

The warm tropical air that flows into the warm sector of the wave overrides the cool air before the wave to form the transition zone denoted as

a warm front. The cold front represents the transition between the generally humid air of the warm sector that has been forced upward and the

advancing cold polar air. Squall lines are drawn to represent belts of

vigorous vertical convection, intense thunder showers, and sharp wind

shifts that frequently precede fast-moving cold fronts. The fronts shown

on a daily weather map represent the ground intersection of the transition

zones between various air masses. * As a representative example of the application of refractive index

parameters to a synoptic situation, a large-scale outbreak of continental

polar air which occurred over the U. S. during February, 1952, was

* A critical appraisal of recent meteorological thinking on fronts, air

masses, squall lines, etc., is given in Dynamic Meteorology and Weather

Forecasting, by Godske, Bergeron, Bjerknes, and Bundgaard, American

Meteorological Society and Carnegie Institute of Washington, D. C, 1957.
-18-

analyzed in terms of N and A [Bean and Riggs, 1959; Bean, Riggs, and

Horn, 1959]

For this synoptic illustration the reduced expression, N , was

used in preparing constant level charts of the storm at the same levels and

times as those used in the daily weather map series of the U. S. Weather

Bureau. The A unit, on the other hand, was employed to construct vertical

cross sections through the frontal system to give a three-dimensional picture of the synoptic changes taking place.

5. Surface Analysis in Terms of N

A pronounced cold front developed and moved rapidly across the

central and eastern United States during the period 18 to 21 February 1952.

Prior to February 18, a polar maritime air mass had been

moving slowly eastward across the Great Basin and Rocky Mountain

regions. This system included a slow-moving cold front extending from

northern Utah southward into Arizona, and a quasi -stationary front

extending northeastward into Wyoming. With the outbreak of polar continental air east of the Rocky Mountains, the maritime front became more

active and, as it moved ahead of the fast-moving polar continental front

sweeping across the Great Plains, was reported as a squall line by the

time it crossed the Mississippi River early on the morning of the 20th

of February. During the later stages of the storm system, the polar

maritime cold front-squall line was located in the developing warm sector of the polar front wave. The entire ensemble of cold front, polar

front wave and squall line then moved rapidly to the east coast by the

morning of the 21st, thus completing the sequence.

Charts of N were prepared from Weather Bureau surface observations taken at twelve-hour intervals from 0130 EST, February 18th

until 0130 EST, February 21st, 1952, or, in other words, the period of
-19-

time that it took the polar front wave to develop and move across the

country. The synoptic sequence is seen in figures 23 through 29 where

contours of N are derived for various stages of the stornm and compared

to the superimposed Weather Bureau frontal analysis. The same procedure

of comparing derived contours with the existing frontal pattern was followed

throughout the example. Observations from sixty-two weather stations

were used in preparing the surface weather maps. Figure 23 indicates

that the cold front extending from Utah southward displays weak N changes

across the frontal interface. In the early stages of the sequence (figures 23

and 24) this lack of air mass contrast is evidenced in another way by the

slight change of the position of the N = 290 contour encircling west Texas

and New Mexico as the frontal system moves through that area.

By comparison, the cold front sweeping down across the Great

Plains (figures 24 to 26) has a rather marked N gradient across the

front, due in large measure to the northward flow of warm, moist air

that forms a definite warm sector by 1330 EST on the 19th. It is perhaps

significant that the N contours indicate that the various frontal systems

are transition zones rather than the sharply defined discontinuities of

textbook examples, a point that has been enlarged upon by Palmer [ 1957] . Figures 26 to 29 trace the course of this vigorous push of

cold air across the Gulf Coastal Plain and the southeastern states. The

most spectacular gradients on this map series are in the eastern half of

Texas where the marked contrast of cold, dry polar air of low N and

warm moist Gulf air of very high N occurs. A prominent feature of

meteorological significance in -figures 24 to 27 is the northward advection

of tropical maritime air in the warm sector ahead of the cold front. The

advection is evidenced by the northward bulge of high N over the Mississippi Valley on these charts. Figure 29 shows the synoptic situation as the

front moves off the Atlantic Coast and refractivity gradients across
-20-

the continent gradually weaken.

The variation of N due to the passage of the frontal system

can be seen in figures 30 to 34, where the 24-hour changes of Nq are

shown. The 24-hour change, designated AN , is obtained by subtracting

the value of N observed 24 hours ago from the current value. The change

is determined on a 24-hour basis in order to remove effects of the diurnal

cycle ' of N . The AN charts show a general rise of N in the warm sector

o o

° o and a drop in N behind the front, amounting, in the warm sector, to 35 to

40 N units by 1330 EST on the 20th of February (figure 33) accompanied

by a 40 to 50 N unit drop behind the front.

The relative sensitivity of N to humidity changes is emphasized

by the AN charts. The N drop behind the cold front occurs in a region

of increasing pressure and decreasing temperature -- a combination that

increases the dry term and depresses the wet term of the refractive index

(see equation 2). The decrease in the wet term from the rapidly dropping

de>ypoint more than compensates for the increased dry term. As an

example, in the 24-hour period ending 0130 EST on the 19th the station

pressure at Oklahoma City increased 13 millibars. The dry term increased

12 N units while the wet term dropped 42 N units, giving a net change of

minus 30 N units. This N rise in the warm sector and drop behind the

o

^ cold front is consistent throughout the development of this polar front

wave. The present system had about a 35 N unit rise and a 40 N unit drop.

This general pattern might be expected to occur in all fast-moving cold

fronts, with varying intensity depending upon the individual synoptic pattern. In any case, it appears that the N pattern is a sufficiently stable

and conservative property of the atmosphere so that it should be possible

to develop forecasting rules for N but not, of course, without the analysis

of many more N patterns.
-21-

6. Constant Pressure Chart Analysis

The same frontal system (February 18-21, 1952) was analyzed for

selected constant pressure levels. The 850 millibar (mb) charts (about

5, 000 feet above mean sea level) and the 700 mb charts (about 10, 000 feet

above mean sea level) were prepared for the times of radiosonde ascent

(10 A.M. and 10 P.M. EST) throughout the synoptic sequence from the

radiosonde reports of 43 U.S. sounding stations. It is not necessary to

reduce the 850 mb or 700 mb level data since they are referenced by definition

to the indicated constant pressure level. Contours for the charts aloft are

shown in figures 35 to 40 while their respective 24-hour changes, Nqcq

and N_^p., are given in figures 41 to 44.

The NocQ charts show that the northerly flow of warm humid air

within the warm sector that was so prominent on the N maps is also

clearly in evidence at the 850 mb level. Further, a change pattern similar

to that on the N maps is also observed at the 850 mb level, particularly

in figure 43 . That is, a rise in Nocp) values in the warm sector and a decrease behind the cold front is apparent. Surprisingly enough, by the

time the frontal system was well developed, at 1000 EST on the 20th, the

Nqc/v values were nearly as large as those on the surface.

The N_QQ charts are more difficult to interpret than those of N

or Nqj.^. It appears that at this altitude the wet term is usually negligible

and N will normally vary inversely as temperature since the pressure is

constant at the 700 mb level. By 1000 EST on the 19th (figure 38) an

intrusion of low N values is observed in the 700 mb warm sector due to

the advection of warm, low-density air northward The chart for 24

hours later (figure 40) displays two prominent highs in which N_qq = 225.

One of these highs lies between the squall line and the cold front and the

other just south of the apex of the 700 mb wave. Interestingly enough,

these two highs are due to quite different causes. The high centered
-22-

over Atlanta appears to have arisen from the unusually high transport

of moisture to the 10, 000 foot level, since the 700 mb wet term at Atlanta

increases from 4.5 to 25 N units in the 24-hour period ending with 1000

EST on the 20th of February. The second high, centered over Omaha,

appears to be due to an intense dome of cold air as indicated by the drop

of the 700 mb temperature from -7. 3°C to -21.4 C in the twelve hours

preceding map time. When temperatures are below 0°C the wet term

contribution to N is quite small and density changes become significant in

producing changes in N. Falling temperatures produce higher density air

and, consequently, a region of high N values around Omaha as depicted on

the N_QQ chart of figure 40 and AN_qq chart of figure 44,which shows this

change more clearly.

7. Vertical Distribution of the Refractive Index Using A Units

The synoptic study of the vertical distribution of the radio refractive index extends the foregoing constant-level analyses by considering

the problem of whether the air mass properties associated with this

typical wintertime outbreak of polar air are reflected in the vertical

refractive index structure. Charts showing the structure of the storm

have been prepared using radiosonde measurements from stations located

along a line normal to the frontal zone between Glasgow, Montana, and Lake

Charles, Louisiana (figure 45). Plots of N versus height along this crosssection line were obtained at 12 -hour intervals during a four -day period

and converted to A units.

Figure 46 is a sample cross-section along the Glasgow-Lake

Charles line analyzed in terms of unmodified N as in the idealized cases

of figures 15 and 16. Compare figure 46 with the A unit analysis of

figure 52 for the highlighting of air mass differences in refractive index.

Examples of the distribution of the N components, temperature and humidity,
-23-

around the front are shown in figures 47 and 48. Various stages in the

advance of this intense storm system across the continent are shown in

figures 49 to 54 in terms of modified N (A units). At the outset of the

period of observation (figure 49) the polar front was located over the

northern Great Plains between Rapid City, South Dakota, and North

Platte, Nebraska. At this time the entire cross section is characterized

by weak to moderate gradients of refractivity. In figure 50, twelve hours

later, this front had moved some 300 km southward. The contrast of

the southward push of polar air and the northerly advection of tropical

maritime air from the Gulf of Mexico into the developing warm sector of

the polar front wave is evidenced by the relatively large gradients in the

neighborhood of Dodge City. The core of tropical maritime air has evidently

not progressed far enough northward to displace the warm but dry air that

had been over the Great Plains prior to the outbreak, with the result that a region of low A values is found between the front and the tropical maritime

air. In figure 51 the effects of the Pacific front are apparent in the buildup of a secondary region of high N some 400 km ahead of the polar front,

located at this time over Dodge City. Twelve hours later (figure 52) the

core of tropical maritime air has become more extensive and now reaches

to a height of 3 km. The second (Pacific) front is picked up now on the

cross section and the area of low A values is confined between the two

fronts. By 0300 Z on the 20th (figure 53) the polar front is approaching

Lake Charles and the Pacific front is reported on the daily weather inap

as a squall line. Finally, by the morning of February 20th (figure 54)

both fronts have passed to the south of Lake Charles and the polar air

just behind the front is characterized by relatively low A values.

The use of space cross -sections does not always yield measurements at the most desirable points along a frontal zone. Another method

of arriving at the probable refractive index structure about the frontal
-24-

interface is to plot radiosonde observations for a single station arranged

according to observation times as on figures 55 to 61.

The time cross -section for Glasgow, Montana (figure 55), which

is in the cold air behind the polar front for the entire period of observation of the storm, displays gradients of A values that are generally

weak. An exception occurs on the evening of the 19th (20/0300Z),

apparently as a result of subsidence effects. Rapid City, South Dakota

(figure 56), also shows generally weak gradients throughout the cold

air behind the front. North Platte, Nebraska (figure 57), exhibits moderate gradients with increasing A-values in the post-frontal higher-density

polar air. The wet-term contribution to N at North Platte is insignificant

because of the low temperature at this season. Dodge City, Kansas (figure 58),

has a warm, dry low ahead of the polar front and increasing A values in

the cold air just behind the front. Oklahoma City, Oklahoma (figure 59),

represents a classic synoptic situation in which advection of tropical

maritime air from the Gulf of Mexico produces a strong high ahead of

the front and a low within the cool, dry polar continental air. Again in

the region around Little Rock, Arkansas (figure 60), there is warm

moist air of extremely high refractivity ahead of the front being replaced

by polar continental air of characteristically low A value. The time crosssection for Lake Charles, Louisiana (figure 61), is complex but represents again the same general features: high A values ahead of the front

and low values behind.

The time cross -section presentation is referred to as an epoch

chart when the observations are normalized with respect to the frontal

passage. Thus, as a frontal system advances and passes over a station,

one obtains yet another perspective of the space cross -section. Such a
-25-

presentation is given in figures 62 to 68. Figure 63 represents a typical

continental station located in the polar continental air mass throughout

the occurrence of the storm. The essential feature here, as in figure

56, is the absence of detail of A structure due to the presence of a

uniform air mass over this station. Compare this figure with the epoch

chart for Oklahoma City (figure 66), where the structure of the idealized

model is clearly reflected by the prefrontal A-unit high, strong gradient

across the frontal zone, and the A-unit low behind the front. This rather

fortuitous agreement is felt to be due to the strategic location of Oklahoma

City with respect to the motion of contrasting air masses about the polar

front. That is, this epoch chart represents a point of confluence of virtually unmodified polar continental and tropical maritime air.

The exponential correction to the refractive index height distribution used in this storm series allows air mass properties to be clearly

seen. By use of such an exponential correction one may construct an

idealized refractive index field about a frontal transition zone that shows

the temperature and humidity contrasts of the different air masses. Further, when this technique is applied to the analysis of a synoptic tropospheric disturbance, it does indeed highlight air mass differences.

8. Summary

With presently-available techniques, field meteorological

measurements can be converted to a synoptic refractive index analysis

in a few hours. The accuracy of refractive index forecasts depends

largely on the adequacy of current synoptic forecasting techniques in

predicting the distribution of the common meteorological parameters

of pressure, temperature, and relative humidity, since these three

variables determine uniquely the N patterns that will exist. It is well

known that meteorological forecasting skill drops off quite rapidly with
-26-

increasing interval of prognosis. This implies, then, that in certain clearcut situations over short time periods N patterns and profiles may be

predicted with reasonable accuracy. At the outset the use of such a

relatively untested device is limited to obvious synoptic situations.

Gradual perfection of N forecasting techniques may, at some future

date, result in a considerably wider application of N patterns, perhaps

even on a regular synoptic basis.

Because of the extent and complexity of the problem, discussion

of the relationship between N structure and radio propagation phenomena

such as fadeouts, radio ducts and holes, and enhancement of beyond-thehorizon radio fields has been omitted. There is in the literature, however, a large body of evidence supporting a strong correlation betw^een

large gradients of N and enhancement of radio fields. The indicated

direction of future work is toward the understanding of the interrelation

of atmospheric structure and electromagnetic propagation.

Among the plausible avenues for continued research in the field

of synoptic radio meteorology is that suggested by the Moler-Holden

study on atmospheric circulation. These writers clearly demonstrate

a relation between a synoptic situation (a small-scale area of horizontal

mass divergence and local dow^nward -directed vertical motion) and enhancement of field strength on a beyond-the-horizon radio link operating over

a path through the synoptic feature (evidenced by a high pressure area

at the surface). The subsidence mechanism produces an elevated layer

that acts to reflect radio energy and consequently enhance the received

fields. The Moler-Holden study relates atmospheric structure and electromagnetic fields in a fundamental way and represents a definite step

toward a more sophisticated picture of physical processes that change

the character of the atmosphere as a propagation medium.
-27-

References

Arvola, W. A. , Refractive index profiles and associated synoptic

patterns. Bull. Am. Meteor. Soc. 38.' No. 4, 212-220 (April,

1957).

Bean, B. R. , Some meteorological effects on scattered radio waves,

IRE Trans. PGCS-4, No. 1, 32 (March, 1956).

Bean, B. R. , and E. J. Dutton, On the calculation of the departures of

radio wave bending from normal, J. Research NBS, 64D, (Radio

Prop.) No. 3, 259-263 (May, I960).

Bean, B. R. , and J. D. Horn, Radio-refractive-index climate near the

ground, J. Research of NBS, 63D, (Radio Prop. ) 259-27

(November-December, 1959).

Bean, B. R. , J. D. Horn, and A. M. Ozanich, Jr., Climatic charts

and data of the radio refractive index for the United States and

the world, NBS Monograph No. 22 (November, I960).

Bean, B. R. , J. D. Horn, and L. P. Riggs, Refraction of radio waves

at low angles within various air masses, J. Geophys. Research

65, 1183 (April, I960).

Bean, B. R. , and L. P. Riggs, Synoptic variation of the radio refractive

index, J. Research NBS, 63D , (Radio Prop. ) No. 1, 91-97

(1959).

Bean, B. R. , L.. P. Riggs, and J. D. Horn, Synoptic study of the vertical

distribution of the radio refractive index, J. Research NBS, 63D,

(Radio Prop.) No. 2, 249-258 (September-October, 1959).

Bean, B. R. , and G. D. Thayer, On models of the atmospheric radio

refractive index, Proc. IRE, 47, No. 5, 740-755 (May, 1959a).

Bean, B. R. , and G. D. Thayer, CRPL exponential reference atmosphere,

NBS Monograph No. 4, (U. S. Governinent Printing Office, Washington 25, D. C, (October, 1959b).

Berry, F. A., E. Bollay, and Norman F. Beers, Handbook of Meteorology,

page 638 (McGraw-Hill Book Company, Inc., New York, 1945).
-28- I

Booker, H. G. , and W. E. Gordon, A theory of radio scattering in the

troposphere, Proc. IRE, 38, 401-412 (April, 1950).

Byers, H. B., General Meteorology, page 327 (McGraw-Hill Book Company

Inc., New York, 1944).

I England, C. R. , A. B. Crawford, and W. W. Mumford, Ultra- shortwave radio transmission through the non-homogeneous troposphere.

Bull. Am. Meteor. Soc . , J^, (1938).

Fannin, B. M. , and K. H. Jehn, A study of radio elevation angle error

due to atmospheric refraction. Trans. IRE, AP-2, No. 1, 71-77

(1957).

Flavell, R. G. , and J. A. Lane, The application of potential refractive

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Terres. Phys., 24, 47-56 (1962).

Gerson, N. C. , Variations in the index of refraction of the atmosphere,

Geofisica Pura E Applicata ]3, 88 (1948).

Godske, C. C, T. Bergeron, J. Bjerknes, and R. C. Bundgaard,

Dynamic Meteorology and Weather Forecasting, page 5 26

(American Meteorological Society and Carnegie Institute of

Washington, D. C, 1957).

Gray, R. E. , The refractive index of the atmosphere as a factor in

tropospheric propagation far beyond the horizon, IRE National

Convention Record, Part 1, page 3 (1957).

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Hay, D. R. , Air-mass refractivity in central Canada, Can. J. Phys.,

36, 1678-1683 (1958).

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Hull, R. A., Air-wave bending of ultra-high-frequency waves, QST, 21,

16-18 (1937).
-29-

Jehn, K. H. , The use of potential refractive index in synoptic-scale

radio meteorology, J. Meteorology, 17, 264 (June, 1960a).

Jehn, K. H. , Microwave refractive index distributions associated with

the Texas-Gulf cyclone, AMS Bulletin, 4_1, 304-312 (June, 1960b).

Jehn, K. H. , Microwave refractive-index distributions associated with

the central United States cold outbreak, AMS Bulletin, 42, 77-84

(February, 1961).

Katz, I. , Gradient of refractive modulus in homogeneous air, potential

modulus, pages 198-199 in Propagation of Short Radio Waves, by

D. E. Kerr, (McGraw-Hill Book Co. , New York, 1951).

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on Propagation, NDRC, Pages 107-113 (1944).

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turbulence. Nature, 166 , 1100-1104 (December, 1950).

Misme, P. , Influence of abrupt air mass changes upon tropospheric

propagation, Annales des Telecommunications (Paris, May, 1957).

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index", Proc. IRE, 48, 1498-1501 (August, I960).

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its effect on VHF radio signal strength. Trans. Am. Geophys. U. , 37 , (August, 1956).

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-30-

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Pickard, G. W., and H. T. Stetson, Comparison of tropospheric reception,

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at 44. 1 Mc with 92. 1 Mc over the 167-mile path of Alpine, New

Jersey, to Needham, Massachusetts, Proc. IRE, 38^, 1450 (1950b).

Randall, D. L. , A study of the meteorological effects on radio propagation

at 96. 3 Mc between Richmond, Virginia, and Washington, D. C. , Bull. Amer. Met. Soc . , 35^, 56-59 (February, 1954).

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of metre radio waves beyond the normal horizon, Proc. lEE lU,

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Saxton, J. A. , Propagation of metre radio waves beyond the normal i horizon, Proc. lEE, £8, 360-369 (September, 1951).

|

i Schulkin, M. , Average radio-ray refraction in the lower atmosphere, ' Proc. IRE, 40, No. 5, 554-561 (1952). '

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41, 1035-1037 (August, 1953).

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troposphere, Proc. IRE, 3_5, 1198 (1947).

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11-12, 687-717 (November-December, 1961), Nippon Telegraph

and Telephone Public Corporation, Tokyo, Japan.
31

400

300

N 200

100 -

ISACHSEN, N.W.T

TS'-SO'N., 103°- 50' W.

FEBRUARY 1953-1957

234 PROFILES, N5= 332.5

UPPER AND LOWER

STANDARD DEVIATION \^LIMITS

EXPONENTIAL REFERENCEATMOSPHERE, Ng =332.5

4 6 8 10

h(km)

12 14

Figure 1. Mean N Distribution for Isachs en, N.W.T., Canada
32

400

300

N 200

100

CANTON ISLAND

2°-46'S., I7r-43'W

FEBRUARY 1953-1957

274 PROFILES, Ns=37l.3

'UPPER AND LOWER

STANDARD DEVIATION

LIMITS

EXPONENTIAL REFERENCE^

ATMOSPHERE, Ns=37l3

4 6 8 10

h (km)

12 14

Figure 2. Mean N Distribution for Canton Island, Pacific Ocean
33

<0J

f

I

I

!

8"

to

I

s

ti

I

17

• 5

1.3

I.I

0.9

0.7

0.5

PLOTTING KEY

'f Average wind speed equal

to or more than lOmph

cP Polar continental air mass mP Polar maritime oir mass mT Tropicol moritime oir mass mT

*fnP mT

f mT ^^

cPamP cPamP

c mT

>amT^^^^-^

••

"^ml^

,'^ cP "<+• cPa mT cPamT 1 mT

mP ^^-"''^^ +cPamT mT mT

+ + w

•

4- + cPcPcP

KcP

f cPamT

cPamT

320 330 340 350 360 370 380 390

Hourly Mean Surface RefractMty

Scatter diagram of select hourly median field

strength vs. hourly mean refractivity July 17 to August 8,

1947.

Figure 3. Field Strength versus Refractivity
34

W

Q

§^

Ok

-> c ^

-§

« i

1

^

1 1

1

1^

>*C^

1

$^ 1

»s ;^ §

*^ 1

:§ t

-^ Q

s »>i ^ S

^

^

«t^

OS

'^

3.1

1.9

1.7

1.5 -

1.3

I.I

0.9

0.7

0.5

I

.Coldfront

J passes Ricttmond

0830

Squall line

I crosses pattilCo<d front I>oss«s Was^

1230 1690 2030 July 19,1947

oQao

18

16

-9

"'• -12 Cold front posses VUBSNngfDnl830

- July 19-

8-

10- 7 Squall line crosse s

potf* 1330 July 19

_5

-3

Cold front posses Rtotwnond

S _4 2130 July 19 -2

Points 6, 13, 314 missmg

320 330 340 350 360 370 380 390

Hourly Mean Surface Refractivity

Scatter diagram showing passage of a cold

front system over the Washington-Richmond path and

graph indicating the fluctuation of hourly median field

strength with time.

Figure 4. Field Strength and N Changes During Frontal Passage
35

20

E 14 ^^

iD 12

Z

Q 10

2^

LU

CD 8

-J

<H 6 O

1-

4

TROPICAL MARITIME AIR

^POLAR CONTINENTAL AIR

20 40 60 80 100 120 140 160 180 200

ANGLE OF ARRIVAL OR DEPARTURE, 9o,(mr)

Figure 5. Mean Angular Bending for Two Air Masses
36

40

36 h

32

28 -

E 24 -

Z 20

16

12

8

-

4

-

LU

A(h,3l3)

'A (h, 313)

^313

1 r

MARITIME

TROPICAL AIR

SAN JUAN, W I. (July Average)

^j/j-^

\ ^C7=^

310 320 330 340 350 360 370 380 390

A(h,3l3), N UNITS

•8 -7 -6 -5 -4 -3 -2

'^3I3"'^(^'^)

Figure 6. Departures of t and N from Normal for Maritime Tropical Air
37

COCO

oJ

COd

o

• 1-1 u>

o

COu

a

Q

0)

• H

(UJ>1) 1H9I3H
38

26 MARCH

SFC. SYNOP

lOOOPST '?-S#-

B

0900 PST

N WWVi

c

1100 PST

Figure 8. Isobaric and Strearaline Maps
39

/ /\

A

\

lO

CO

o o o o

00

03

COu

>

1—

>

1—4a

CO

XIam

X

(D

MW/9a

41
42
43

CD

1 1

l\

_j oSO cr o QL <

< O

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Figure 23. N^ Chart for Storm System 0103E 18 February, 1952

Figure 24. N Chart for Storm System 1330E 18 February, 1952
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Figure 25. N Chart for Storm System 0130E 19 February, 1952

Figure 26. N Chart for Storm System 1330E 19 February, 1952
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Figure 27. N Chart for Storm System 0130E 20 February, 1952

Figure 28. N Chart for Storm System 1330E 20 February, 1952
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Figure 29. N^ Chart for Storm Systems 0130E 21 February, 1952

Figure 30. 24-Hour AN„ Chart, 0130E 19 February, 1952
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Figure 31. 24-Hour AN Chart, 1330E 19 February, 1952

Figure 32. 24-Hour AN^ Chart, 0130E 20 February, 1952
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Figure 33. 24-Hour AN Chart, 1330E 20 February, 1952

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Figure 34. 24-Hour AN Chart, 0130E 21 February, 1952
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Figure 35. Ng^Q Chart, lOOOE 18 February, 1952

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Figure 36. NyQO Chart, lOOOE 18 February, 1952
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Figure 37. Nocr, Chart, lOOOE 19 February, 1952 '850

Figure 38. N-700 Chart, lOOOE 19 February, 1952
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Figure 39. Ng5Q Chart, lOOOE 20 February, 1952

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Figure 41. 24-Hour AN850 Chart, lOOOE 19 February, 1952

Figure 42. 24-Hour ^^^nr.r. Chart, lOOOE 19 February, 1952
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Figure 43. 24-Hour ANqca Chart, lOOOE 20 February, 1952 '850

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* U.S. GOVERNMENT PRINTING OFFICE : 1962 —660665

U. S. DEPARTMENT OF COMMERCE

Luther H. Hodges, Secretary

NATIONAL BUREAU OF STANDARDS

A. V. Astin, Director THE NATIONAL BUREAU OF STANDARDS

The scope of activities of the National Bureau of Standards at its major laboratories in Washington, D,C., and

Boulder, Colorado, is suggested in the iollowing listing of the divisions and sections engaged in technical work.

In general, each section carries out specialized research, develoranent, and engineering] in the field indicated by

its title. A brief description of the activities, and of the resultant publications, appears on the inside of the

front cover. WASHINGTON, D. C.

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Dielectrics. High Voltage.

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Radiation Physics. X-ray. Radioactivity. Radiation Theory. High Energy Radiation. Radiological Equipment.

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Analytical and Inorganic Chemistry. Pme Substances. Spectrochemistry. Solution Chemistry. Standard Refer- ence Materials. Applied Analytical Research, Crystal Chemistry.

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Crystallography.

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Engineering Applications. Systems Analysis.

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Office of Weights and Measures. BOULDER, COLO.

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Standards. Radio Plasma. Millimetei^Wave Research.

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