OCTOBEB 1956 MONTHLY WEATHER REVIEW 363
THE WEATHER AND CIRCULATION OF OCTOBER 1956'
Including a Discussion of the Relationship of Mean 700-mb. Height Anomalies to Sea Level Flow
HARRY F. HAWKINS, JR.
Extended Forecast Section, U. S. Weather Bureau, Washington, D. C.
1. WEEKLY CIRCULATION STATES RELATED
TO DROUGHT RELIEF
As October began, critical drought conditions prevailed
over most of Texas, the Central Plains, and southeastern
Rocky Mountain States. Moisture deficiencies, par-
ticularly during the growing season, had mounted to
record proportions in some areas; e. g., western Texas
was already in its sixth year of drought [ll]. Unirrigated
crops had been a failure, pastureland of little use, and
there was insufficient moisture for germination of seed
for winter small grains.
First week.-Salient details of the first week in October
are pictured in figure 1. Over North America the gross
features of a ridge in the West and a trough in the East
continued, as in September, to be the overriding charac-
teristics [3]. Warmth predominated over the United
States with ridge conditions along the eastern Rockies
(fig. la) and heights well above normal aloft. The
eastern North American trough was stronger than normal
and off the coast in the north, although it lay inland over
the Appalachians in the south. At sea level (fig. lb), a
maritime high pressure ridge extended from the Far
Northwest to the Central Plains. With the exception of
extreme eastern Texas and central California, no precipi-
tation of note occurred west of the Mississippi-Ohio
Valleys(fig. Id). Widespread rains in the East were
due to cyclonic activity in the Appalachian trough. The
rather unseasonal California precipitation was associated
with entry of a coId front into the closed California Low
shown in figure la. No appreciable drought reliefwas
experienced in central United States.
Second week.-Significant changes in circulation became
manifest toward mid-month. During the last five days
of this period (fig. 2a and b) mean ridge conditions a t
700 mb. moved rapidly northeastward toward the central
Appalachians. The closedLow off the California coast
(Sg. la) was gradually transformed into a vigorous polar
trough. The entire west coast wasnow subjected to the
effects of westerly perturbations which gradually extended
their area of influence to lower United States latitudes.
In the fast westerly band across the North Pacific (cf.
I See Oharts I-XVII following p. 377 for analyzed climatological data for the month.
700-mb. and sea level patterns in fig.2) disturbances
travelled rapidly eastward. Although major centers
passed into central Canada (Chart X), trailing fronts and
secondary centers brought cold air and precipitation into
the Northwest. Toward the end of this period, an upper-
levelcyclonic circulation worked eastward at lower
latitudes to the midcontinent and in concert with the
frontal advance of cold air, effected a meridional release
of precipitation which fell in a swath from southern Texas
to the western Lakes (fig. 2d).
While these welcome rains fell in the Midwest, the East
was enjoying one of its famous spells of fine autumn
weather. This resulted from eastward motion of the
upper-level ridge (noted above) in conjunction with a
cold Canadian High at sea level. The High swept down
out of Canada on the 9th (Chart IX) and passed eastward
into New England. The upper-level ridge came eastward
during this period and intensification a t both levels took
place from the southwestern Appalachians into New
England. Dynamic anticyclogenesis was apparently in-
volved in the maximum sea level pressure (daily) of
1040 mb. noted in New England on the 12th. Although
the high center passed off eastward, ridge conditions were
maintained over much of the East and in the almost
stagnant circulation the cumulatory effects of industrial
pollution of the air were noted in a number of eastern
cities. In general, however, crisp cool nights and hazy
autumn days were the order, except in those more
southerly areas where onshore easterly flow to the south
of the ridge line brought cloudiness and precipitation
(note Florida, fig. 2d). Simultaneously the mid-United
States was warmed by return flow to the rear of the High,
but the East remained below normal due to the initial
low temperatures of the Canadian air.
Third week.-Further extension of weak westerly influ-
ence into central and southeastern United States was noted
during the third week. (See fig. 3a for latter part of week.)
Most noteworthy event was the slow movement across
the southern United States of an upper-level cyclonic cir-
culation which spread precipitation from New Mexico
eastward. Central and southern Texas received 1 to 2
inches generally, and temporary local drought relief was
accomplished(fig. 3d). Heavy amounts of rainfall were
364 MONTHLY WEATHER REVIEW OCTOBER 1956
FIGURE 1.-(a) and (b) 5-day mean 700-mb. and sea level charts
showing continuation of September pattern of mean ridge west of
Continental Divide with mean trough along or off the east
coast. (c) and (d) show continuation of September's temperature
and precipitation regime with no drought relief in central United
States.
FIGURE 2.-Major changes in circulation pattern took place toward
middle of month. Development of west coast trough and rapid
motion of mean ridge into Yortheast (a) and building of dynamic
anticyclone in New England (b) brought changes in temperature
regime, (c) and first Midwest drought relief (d).
OCTOBER 1956 MONTHLY WEATHER REVIEW 365
Temperature departure ,?
FIGURE 4.-(a) and (b) show an intensification of the new pattern
which first emerged in figure 2. Fresh cold air from the north
Pacific was swept through the trough to the Divide (c) as pre-
cipitation spread eastward. Note rain-shadow over much of
drought area (d), with precipitation in Mississippi Valley in
region removed from foehn components (a).
366 M O N T H L Y W E A T H OCTOBEB 1956
FIGURE 5.-Mean 700-mb. height contours and departures from normal (both in tens of feet) for October 2-31, 1956. Abnormal Pacificr
ridge led to strong development of west coast trough and complete suppression of east coast trough activity except in Florida.
also noted in the far Northwest, with strong onshore flow achieved during a momentary relaxation of the New Eng-
or trailing fronts providing daily rains. land blocking as a fresh cold surge moved in. The storm
Anticyclonic circulation maintained itself over New left two or more inches of precipitation along most of the
England (fig.3b) as two new migratory Highs entered coast from Florida to southern New Jersey. St. Cloud,
this area during the week (Chart IX). This continued Fla., reported 17.30 in.
the regional circulation pattern established the preceding Temperatures were generally warm during this third
week,whichwas reintensified during the last week(fig. week.Aninflux of marine air accompanying the storm
4a,b). Early in the third week a “semitropical” Low noted above and rapid passage of Highs off the coast re-
formed near Cuba in the easterlies well south of the High stored above normal conditions to most of the East (fig.
over New England. The Low moved up along the Florida 3c). In the West, the major trough was off the coast, and
coast and turned abruptly eastward only after reaching Pacific air from a more southerly and warmer source
Chesapeake Bay on the 18th (Chart X). This turn was moderated previously cool conditions.
I \
OCTOBEB 1956 MONTHLYWEATHERREVIEW 367
Fourth week.-During this period a return to, and in-
tensification of, the general circulation type of the second
week was noted. The west coast trough and New England
Highbecame stronger than before(fig. 4a and b). This
was part of a general increase in amplitude of the mid-
latitude wave system (fig. 4a) and a marked decline in
zonalwesterlies from what had been a typical October
high index.
Below normal temperatures again dominated the West
(fig. 4c), as the eastern Pacific trough came eastward and
great quantities of cold North Pacific air were swept
inland. Precipitation (fig. 4d) extended from the Mexi-
can to the Canadian border in the West, with greatest
amounts in the Northwest, where heights were below nor-
mal and cyclonic activity most marked. Again precipita-
tion spread eastward as westerly perturbations were prop-
agated downstream. A prelude to winter couldbeseen
in the storm of the 23d to 24th which left up to 2 feet of
snow in the northern Cascades; 19 inches at Alta, Utah;
lesser amounts over Colorado and Wyoming; and 6 inches
over the Black Hills of South Dakota.2 As the cold air
advanced eastward, precipitation also fell over the North-
ern and Eastern Plains, but foehn action extended the rain
shadow of the Rockies over most of Texas.
The eastern half of the country was warm since the two
daily Highs affecting the area were mainly of modified
Pacific air (Chart IX). Precipitation in the East was
associated with cyclonic developments in the east coast
trough and orographic control of the strong onshore moist
flow.
In the last few days of October (not shown here) another
westerly disturbance worked eastward at lower latitudes
from the west coast trough. Modest but significant
amounts of precipitation fell over much of the drought
area.
Thus October brought temporary relief to many critical
drought areas. The further restoration of soil moisture
and adequate water tables remained to the future.
2. MEAN CIRCULATION OF THE MONTH .
From the preceding rather thorough sampling of the
month one should be able to estimate the monthly mean
state without great difficulty. Figure 5 shows the mean
700-mb. circulation pattern and accompanying height
departures from normal. The westerlieswere stronger
and farther north than normal with essentially four mid-
latitude troughs-not counting a weak lee-trough east of
the Canadian Divide. I n t h e Pacific, an anomalously
long wavelength existed; the troughs were on either shore,
separated by an elongated ridge.Across the northern
periphery of the ridge lay a strong, fast westerly belt, while
in the ridge itself heights were 500 ft. above normal. This
is the greatest positive (hemispheric) anomaly of record
for October.
2 8ee adlacent article by Vore and McCarter discussing forecasting problems associated
with this type of development.
In retrospect one can see that the first week of October
(fig. la) was essentially a continuation of the regime which
prevailed during September [3]; i. e., an east coast trough
and a ridge west of the Divide. Only in the second week
of October, as the west coast trough deepened and anti-
cyclogenesis prevailed over the East (fig. 2), did the new
regimebecome manifest. During the last twoweeks
secondary variations of the new pattern prevailed.Con-
sequently, there was a considerable change in circulation
type over North America between September and October
and, as we have seen, a significant change in certain aspects
of the precipitation distribution. Anexception to the
general change, however, should be noted in the low-
latitude trough over Florida which represented little vari-
ation in circulation or weather for this area. For the
country as a whole, temperature changes were greater than
average; i. e., 58 percent of the stations changed tempera-
ture by more than one class compared to 35 percent nor-
mally anticipating so great a change from September to
October.
Another interesting facet of October's weather has been
pointed out by Ballenzweig. I n recent research on hurri-
canes [I], he has established that patterns similar to figure
5 are generally favorable to hurricane development and
subsequent incidence in the Florida area. How then does
one account for only one "semitropical)' Low this October?
His precursory survey of sea surface temperatures as
plotted on current weather maps was expanded and is
presented in figure 6. Although complete data are not
yet available, those so far examined show surface water
temperatures this October werebelownormal [lo] and
almost all boxes were below 81'-83' F., which Palmen has
noted as approximately the lowest water temperature
over which hurricanes are likely to form [12]. Just how
FIGURE 6."Preliminary survey of sea surfacewatertemperatures
(O F .) forOctoberfrom plotted synoptic data on eleven selected
days. Key: inupper left corner of square,number of observa-
tions; center, mean sea surface temperature; lower right, depar-
turefromnormal. Data farfromcompletebutstrongly
suggest prevalence of cooler than normal conditions.
and normal temperature for each station. Limiting departures are determined from past
8 Monthly temperature clssses are defined with reference to the monthly variability
records so that classes below, near, and above normal each occur j4 of the time, while much
below and much above occur $6 of the time.
368 MONTHLY WEATHER REVIEW OUTOBEB 1966
successfully these anomalies can be related to the atmos-
pheric circulations of preceding months is beyond the
scope of this note. However, both August and Septem-
ber were conspicuous for strong westerly trough activity
in western and eastern sectors of the Atlantic. I n fact,
the discussion of September [3] mentioned the unconfirmed
report of an ice floe sighted near the Azores in uncommon
southerly latitudes. Since water temperature anomalies
are usually assumed to change but slowly, there is here a
definite suggestion (cf. Riehl [14]) that such anomalies
have prognostic implications. For a month with similar
regional circulation characteristics, but with hurricane
activity, the reader is referred to October 1947[4]. It
should also be mentioned that the Low near Cuba (Chart
X) on the 30th and 31st became a full-fledged hurricane
on November 4.
3. MEAN HEIGHT DEPARTURES FROM NORMAL
AND WEATHER ANOMALIES
In the course of this series of articles considerable atten-
tion has been paid to the relation between surface weather
and mean 700-mb. height anomalies. The usual proce-
dure is to interpret the height anomaly gradients by means
of the geostrophic relationship and to speak of “anom-
alous components” of flow. This departure from normal
(DN) flow may be considered as that flowwhich,when
added to the appropriate normal flow,wouldyield the
observed flow pattern. Relating mean states of tempera-
ture and precipitation to the observed mean 700-mb. flow
pattern is rendered much easier through explanations
couched in terms of the DN flow, as if the flow has direct
physicalexistence. The general success of this approach
has won it a certain degree of acceptance, but no explicit
justification of its employment has been attempted. It
is therefore proposed that some further rationalization be
offered here.
One of the most convincing demonstrations of the utility
of thinking in terms of DN flow was offered in Martin’s
temperature studies [8] and, to a lesser extent, in those
of Hawkins relating to precipitation [8]. The common
employment of DN flow in the work of the Extended
Forecast Section [9] stems from about this time (1949)
and the concept was employed from the very first in these
monthly articles on weather and circulation [6]. It is the
author’s opinion that this has proven to be a justifiable
procedure and that the success noted was because there
are component flows on the observed sea level patterns
which correspond, on the whole, quite closely to the con-
comitant 700-mb. height departure from normal (DN) pat-
terns. This might be extended to the effect that, strong
gradients of 700-mb. DN flow usually resemble the total
observed flow at sea level. Where the DN flows are weak,
and over continental areas in general, this correspondence
becomeslesswell marked. In view of the fact that we
are concerned with mean maps, and that cold Lows and
warm Highs are the more stable and longer-lived elements
FIGURE 7.-Vertical component of mean relazive geostrophic
vorticity a t 700 mb. for October 2-31, 1956. Centers are
labeled in units of lode per second, negative-anticyclonic, positive-
cyclonic. Compare overall field with height departures from
normal (fig. 5), and sea level mean pressure (fig. 8).
contributing to these means, the total resemblance essen-
tially reaffirms the hydrostatic equation if one admits the
persistent recurrence of given circulation states. On the
other hand, shallow Highs and Lows are subject to steering
by the upper-level currents. These upper currents are
then generally indicative of the deployment of this class
of sea level systems.
I n this latter connection previous work related the
tracks of daily sea level cyclones and anticyclones to the
relative vorticity field at 700 mb. [5, 131. The relation
between height anomalies and relative vorticity is quite
straightforward, since the anomaly centers are, in effect,
the perturbations superposed upon a normal field of almost
straight westerly flow. If one compares the departures
from normal in height (fig. 5) with the 700-mb.field of
relative vorticity (fig. 7) the general similarity is quite
evident. Correspondence of significant centers was ex-
cellent. For example, major positive anomaly centers in
the Pacific, St. Lawrence Valley, eastern Atlantic, and
southern Siberia found direct reflection in the anticyclonic
(negative) vorticity centers; in like manner, the stronger
negative height centers in the Gulf of Alaska, off south-
eastern Greenland, over European Russia, and in north-
eastern Siberia had cyclonic relative vorticity centers as-
sociated with them. The correlation coefficientbetween
700-mb. height departure from normal pattern (fig. 5) and
the 700-mb. field of relative vorticity (fig. 7) was computed
OCTOBER 1956 MONTHLY WEATHER REVIEW 369
FIGURE 8.-Thirty-day mean sea level pressure,October 2-31,
1956. Strong High over New England resulted in onshore moist
currents over most of east coast and warm return flow in central
United States. Strong Gulf of Alaska Low was accompanied by
weak Basin ridge and anomalouscyclonic activity along west
coast of North America.
at 72 points distributed evenly around the hemisphere
between 30' and 60' N., inclusive, and was found to be
Actually, the relative vorticity field at 700 mb. can also
be directly related to the field of total sea level pressure.
This connection may be found in earlier articles (e. g.,
Klein [5]) but a forthright statement of the relation has
been lacking. Presumably through the agency of the
hydrostatic equation, well-marked centers of vorticity
(fig. 7) can usually be related to similar centers at sea
level(fig. 8 ). The correlation between the patterns of
figures 7 and 8 on the 72-point grid was found to be -0.74.
This was larger in magnitude than the correlation between
700-mb. height departures from normal and the mean sea
level pressure pattern, which was 0.63 for an 81-point grid
(including data at 75' N.). Thus the 700-mb. height de-
partures from normal are closely related to the field of
relative vorticity (at 700 mb.) and, to a slightly lesser
degree, to the sea level pressure field itself.
Of greater relevance to the general problem is the relation
between the upper-level height departures from normal
(fig. 5) and the sea level departures from normal (fig. 9).
Inspection reveals that, although the maps were not
identical, overall similarity was striking. The correlation
coefficient between the two patterns, computed at 81
points distributed evenly around the hemisphere between
30' and 75'N., was 0.82. This demonstrates the desired
relationship since the prime requisite is that the anoma-
lous,%r abnormal, sea level flow be closely related to the
-0.70.
409153-67-2
FIGURE 9.-Mean sea level pressuredeparturefromnormal for
October 2-31, 1956. Note similarity in field of departures to
height departurefield (fig. 5), also correspondence of strong
gradients with sea level gradients (fig. 8).
700-mb. height DN flow. In essence this infers that the
immediate causes of the mean temperature and (to a
lesser extent) precipitation departures from the climatic
average are abnormal components offlow in the lower
troposphere.
The general mode of thinking outlined above is far from
new but explict demonstrations have been seldom offered.
Nonetheless, objections to the use of any departure from
normal map as depicting a real physical entity are com-
monly met. More recently the mathematid expression
of any flow field in terms of normal and abnormal com-
ponents and the utility of such representation has become
more generally appreciated [2]. In practice, one finds few,
if any, cases in which mean DN flows of signscant inten-
sity do not have actual physical currents of like nature on
some of the daily synoptic charts which contribute to the
series. Comparisons can also be made between 5-day mean
height departures at 700 mb. and the concurrent sea level
patterns in figures 1 through 4. Where DN gradients
were strong, sea level gradients were quite similar. In
a number of instances surprising correspondence of detail
can be noted.
I n application then, one would associate the below
normal temperatures in the West (Chart I-B) with the
abnormally strong fetch of cold air from the northeastern
Pacific into the western United States, indicated by the
departure from normal flows a t 700 mb. (fig. 5) and at sea
level (fig. 9). The same deductions are possible from the
total observed sea level pattern (fig. 8 ) although only
comparison with the normal (i. e., fig. 9) or an analog dl
reveal the inherent abnormality in figure 8. In like
370 M O N T H L Y W E A T H OOTOBEB 1956
fashion, the prevailing warmth over the central United
States occurred where DN flows were southerly or weak
and slightly anticyclonic. The east coast was warm in
central sections where onshore, warm, moist flowwas
strong, but below normal in temperature over Florida,
where cyclonic circulation and cloudiness were dominant,
and below normal in southern New England, where radia-
tion effects were a t a maximum at the center of the sea
level High (fig. 8).
Precipitation amounts are (often less directly) asso-
ciated with the circulation anomalies relative to the
pertinent moisture source regions. For instance, precipi-
tation in the West (Charts I1 and 111) was due to the strong
onshore flow, trailing frontal passages in the trough, and
cyclonic developments which occurred immediately down-
stream from the trough. This could be inferred from either
figures 5,8, or 9, but appears more clearly delineated in the
height anomalies of figure 5, or the pressure anomalies of
figure 9. Similarly, most of the east coast precipitation
couldbe associated with onshore easterly flow and per-
turbations associated with it. Heaviest amounts occurred
in the central sector, where onshore flow was strongest,
and over Florida where cyclonic circulation, at sea level
and aloft, was most marked. Precipitation totals in the
central portion of the country were comparatively small
and, in proportion, less directly related. The precipitation
was released by perturbations travelling downstream from
the west coast trough, with moisture supplied from the
Gulf of Mexico and advected northward around the ridge
in the East.
The general utility of concentrating attention upon
abnormal flow features to explain anomalies in weather
has been pointed out in many and diverse writings. The
application of this concept to mean flows is both logical
and demonstrable. However, it must be expected that,
when time means are used, best results will be obtained
when dealing with meteorological elements which are con-
tinuous in nature and appropriate to time averaging; i. e.,
temperature, humidity, etc. A discontinuous element
such as precipitation does not lend itself as readily to such
treatment, although Stidd’s work [15] seems to indicate
that when longer and longer time means are employed.
even these elements can be successfully treated. The
trend of modern meteorology is definitely toward the
predictmion of circulation states, although exceptions may
be noted. The value of using the departure from normal
concept in interpreting these states in terms of weather
is believed to be both sound and useful. Furthermore, it
is possible that one of the more promising available attacks
on the problem of long-range forecasting lies in the treat-
ment of evolution of circulations primarily through con-
sideration of the field of height anomaly 171.
REFERENCES
1. E. M. Ballenzweig, Seasonal Variations in the Fre-
quency of North Atlantic Tropical Cyclones Related
to the General Circulation, unpublished report of
U. S. Weather Bureau, Extended Forecast Section,
Sept. 1956.
2. P. F. Clapp, “Application of Barotropic Tendency
Equation to Medium Range Forecasting,” Tellus,
vol. 5, No. 1, Feb. 1953, pp. 80-94.
3. H. F. Hawkins, Jr., “The Weather and Circulation of
September 1956“Including a Discussion of Hurri-
cane Flossy and September’s Typhoon Tracks,”
Monthly Weather Review, vol. 84, No. 9, September
4. C. R. Jordan, “River Stages and Floods for October
1947,” Monthly Weather Review, vol. 75, No. 10,
Oct. 1947, p. 198.
5. W. H. Klein, “The Weather and Circulation of
January 1951,” Monthly Weather Review, vol. 79,
No. 1, Jan. 1951, pp. 16-19.
6. W. H. Klein, “The Weather and Circulation of Jan-
uary 1950,” Monthly Weather Review, vol. 78, No. 1,
Jan. 1950, pp. 13-14.
7. W. H. Klein, “The Central Role of the Height
Anomaly in the Outlook for Long-Range Weather
Forecasting,” Transactions of New York Academy of
Sciences, Series 2, vol. 18, No. 4, Feb. 1956, pp.
375-337.
3. D. E. Martin and H. F. Hawkins, Jr., “Forecasting
the Weather-The Relationship of Temperature
and Circulation Aloft,” Weatherwise, vol. 3, Nos.
1956, pp. 336-342.
1-6, 1950, pp. 16-19,40-43, 65-67,89-92, 113-116,
138-141.
9. J. Namias, “Thirty-Day Forecasting: A Review of a
10-Year Experiment,” Meteorological Monographs,
vol. 2, No, 6, American Meteorological Society, July
1953. (See pp. 1940.)
10. U. S. Navy Hydrographic Office, “World Atlas of Sea
Surface Temperatures,” H. 0. Publication No. 225,
2d Ed., 1944.
11. R. C. Nelson, “Precipitation Deficiencies in Texas,
Oklahoma, Kansas, and Missouri; January-Septem-
ber 1956,” Weekly Weather and Crop Bulletin,
National Summary, vol. XLIII, No. 46, Nov. 12,
1956, p. 7.
12. E. Palmh, “On the Formation and Structure of
Tropical Hurricanes,” Qeophysica (Helsinki), vol. 3,
13. 0. E. Richard, Relation of Sea Level Cyclones and
Anticyclones to the Five-Day Mean 700-mb. Vor-
ticity Field, unpublished Master’s Thesis, Univer-
sity of Chicago, December 1952.
14. H. Riehl, Tropical Meteorology, McGraw-Hill Book
Co., Inc., New York, 1954. (See pp. 331-332.)
15. C. K. Stidd, “The Use of Correlation Fields in Relating
Precipitation to Circulation,” Journal of Meteor-
ology, vol. 11, No. 3, June 1954, pp. 202-213.
1943, pp. 26-38.
B. Departure of Average Temperature from Normal (OF.). October 1956.
LXXXIV-135 OCTOBER 1956 M. W..R..
B. Percentage of Normal Precipitation, October 1956
LXXXIV-137
Chart VI. A. Percen
OCTOBER 1956 M. W. R.
re of Sky Cover Lxween Sunrise and Sunset, October 1956.
B. Percentage of Normal Sky Cover Between Sunrise and Sunset, October 1956.
A. In addition to cloudiness, sky cover includes obscuration or the sky by fog, smoke, snow, etc. tihart based on
visual observations made hourly at Weather Bureau stations and averaged over the month. B. Computations
of normal amount of sky cover are made for stations having at least 10 years of record.
OCTOBER 1956 M. W. R. LXXXIV-138
. .1
.~ Chart VII. A. Percentage of Possible Sunshine, October 1956. ,
B. Percentage of Normal Sunshine, October 1956.
A. Computed from total number of hours of observed sunshme in relation to total number of possible hours of
sunshine during month. B. Normals are computed for stations having at least 10 years of record.
LXXXIV-139 OCTOBER 1956 M. W. R.
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OCTOBER 1956 M. W. R. XXXIV- '
OCTOBER 1956 M. W. R. XXXIV- '
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OCTOBER 1956 M. W. R.
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OCTOBER 1956 M. W. R. LXXXIV-146
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