School of
OCEANOGRAPHY
Analysis of Meteorological
Observations from An Array
of Buoys during BASIN
by
Hiroshi Ishlda
Office of Naval Research
N00014-76-C-0067
N00014-79-C-0004
NR 083 102
OREGON STATE UNIVERSITY
Reference 80-2
January 1980
Masters Thesis
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5. TYPE OF REPORT & PERIOD COVERED
ANALYSIS OF METEOROLOIGCAL OBSERVATIONS
FROM AN ARRAY OF BUOYS DURING JASIN
M.S. Thesis, December
1979
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Hiroshi Ishida
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School of Oceanography
Oregon State University
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Air-Sea Interaction
Wind over the Sea
Meteorolgical Observations from Buoys
Taylor's Hypothesis
-
20.
Wind
t
Temperature Spectra over the Sea
Sea Surface Temperature Spectra
ver the Sea
ABSTRACT (Continue on reverse side It necessary and Identify by block number)
Observations of wind speed and direction, air and sea temperature, and
solar radiation were obtained from an array of buoys in JASIN.
The
observations were analyzed to show spatial and temporal variability.
Spectra of wind speed and air and sea temperature were computed to illustrate the distribution of variance over periods ranging from 3.5 minutes
to 40 days.
When plotted on log-log graphs the spectral estimates generally
decrease with increasing frequency with slopes between -3/2 and -2.
Spectra
of air and sea temperature have a peak-a-t-t*e-diu-rna-1---freer eney.
FORM
1 JAN 73
T
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plotted in variance-preserving form, the spectrum of wind speed is consistent
with a spectral gap and is qualitatively similar to other observations of low
frequency spectra. On the basis of a cross-correlation analysis, it appears
that mesoscale eddies propagated with the mean wind speed except during
frontal passages. Based on the cross-correlation between wind and air
temperature, there is evidence of horizontal roll vortices or organized
convection.
Unclassified
AN ABSTRACT OF THE THESIS OF
Hiroshi Ishida
Oceanography
in
Title:
for the degree of
presented on
Master of Science
December 14, 1979
Analysis of Meteorological Observations from an Array of
Buoys during JASIN
Abstract approved:
Observations of wind speed and direction, air and sea temper-
ature, and solar radiation were obtained from an array of buoys in
JASIN.
The observations were analyzed to show spatial and temporal
variability. Spectra of wind speed and air and sea temperature were
computed to illustrate the distribution of variance over periods
ranging from 3.5 minutes to 40 days.
When plotted on
log-log graphs
the spectral estimates generally decrease with increasing frequency
with slopes between -3/2 and -2.
Spectra of air and sea temperature
have a peak at the diurnal frequency.
When plotted in variance-pre-
serving form, the spectrum of wind speed is consistent with a spectral gap and is qualitatively similar to other observations of low
frequency spectra.
On the basis of a cross-correlation analysis, it
appears that mesoscale eddies propagated with the mean wind speed
except during frontal passages.
Based on the cross-correlation
between wind speed and air temperature, there is evidence of hori-
zontal roll vortices or organized convection.
G
Analysis of Meteorological Observations
from an Array of Buoys during JASIN
by
Hiroshi Ishida
A THESIS
submitted to
Oregon State University
in partial fulfillment of
the requirements for the degree of
Master of Science
Completed December 14, 1979
Commencement June 1980
APPROVED:
Professor of Oceanography
in charge of major
Dean of the School of Oceanography
Dean of the Graduate School
Date thesis is presented
Typed by
Gail Henwood
December 14, 1979
for
Hiroshi Ishida
TABLE OF CONTENTS
Page
1.
INTRODUCTION--------------------------------------------------1
II.
INSTRUMENTS---------------------------------------------------3
III.
OBSERVATIONS--------------------------------------------------5
IV.
SPECTRA------------------------------------------------------10
V.
IV.
TAYLOR'S
HYPOTHESIS------------------------------------------15
HORIZONTAL ROLL
VORTICES-------------------------------------18
ACKNOWLEDGMENTS----------------------------------------------------20
REFERENCES---------------------------------------------------------21
TABLES-------------------------------------------------------------24
FIGURES------------------------------------------------------------ 28
APPENDIX----------------------------------------------------------- 43
Preface
This thesis has been written in manuscript format rather than
in the traditional format.
The School of Oceanography encourages
this approach to expedite the publication of the results of graduate
research projects in scientific journals.
For this
reason, some
deviations from the ordering of a traditional thesis are present:
1) Tables appear in order after the References; 2) Figures
order after the Tables; 3) Acknowledgments
rather than before.
are placed
appear in
after the text,
This manuscript will be submitted to the Journal
of Geophysical Research with Hiroshi Ishida, Clayton
A. Paulson and
Wayne V. Burt as first, second and third authors, respectively.
FIGURE LEGENDS
Page
Figure
Locations of meteorological buoys, JASIN-1978.
28
2
Time series of hourly averaged variables observed at
B3 from 28 July to 6 September 1978.
29
3
Progressive vector diagram of wind at B3 from 2300 GMT
on 28 July to 6 September 1978.
Each square is
plotted at 0000 GMT.
30
4
Composite spectrum of wind speed from B1 and B3. The
symbols X are spectra from one-hourly averages, C) are
spectra from 3.5-minute averages, and + are spectra
from 1.75-minute averages. The vertical bars show
the 90% confidence interval.
31
5
Composite spectrum of air temperature from B2 and B3.
The symbols X, ®, +, and I are defined in Figure 4.
32
6
Composite spectrum of sea temperature from B1 and B3.
The symbols X, [3, +, and I are defined in Figure 4.
33
7
Variance-preserving plot of the spectrum of wind
speed from Bl and B3 together with the spectrum from
Kaimal et al. [1972]. The symbols X, ®, and + are
defined in Figure 4, and o is Kaimal et al's [1972]
spectrum. The broken line shows the spectrum measured
by Smedman-Hogstrom and Hogstrom [1975] over land.
34
1
8
9
Rotary spectra (A) and rotary coefficient (B) of hourly 35
averaged wind velocity from R. The broken line
represents clockwise rotatiri and the solid line
represents counterclockwise rotation.
Mean auto-correlation functions cf unfiltered wind
speed from parts A, B and C. The auto-correlation
functions are averages over buoys B1, B2, B3 and B4.
The lengths of the vertical bars are twice the
standard deviation. Cross-correlation coefficients
from pairs of buoys lying along the mean wind direcThe symbols X, C1, sand + repretion are plotted.
sent the combinations Bl-B4, B2-B4, B2-B3, and B3-B4
respectively in parts A and B. The symbol X represents the combination Bl-B2 in part C.
36
Figure
Page
10
Mean auto-correlation functions of unfiltered air
temperature from parts A and B.
See Figure 9 for
explanation.
Part C is not included because the
temperature record from B1 was incomplete.
37
11
Mean auto-correlation functions of filtered wind speed
from parts A, B and C. See Figure 9 for explanation.
38
12
Mean auto-correlation functions of filtered air temperature from parts A and B. Part C is not included
because the temperature record from Bl was incom-
39
plete.
13
Example of cross-correlation functions of wind speed
(u) from B1 and B4 and air temperature (Ta) from the
same buoys used to determine the eddy travel time in
the downwind direction. The records are high-pass
filtered, part A.
40
14
Schematic diagram of horizontal roll vortices and
associated fluctuations of horizontal wind velocity
and air temperature (assuming unstable stratification).
41
15
Cross-correlation function of high-passed wind speed
.and air temperature at B4, part C. Positive lags
indicate that air temperature leads wind speed.
42
LIST OF TABLES
Table
Page
Locations and periods of buoy observations, JASIN-
1
24
1978.
2
Parts of meteorological' records having approximately
constant wind speed and direction which were selected
for cross-correlation analyses. The beginning and
ending time for each part is 0000 and 1140 GMT respectively.
RiB is the mean bulk Richardson number,
averaged over reliable buoys and the R/V METEOR.
25
Wind speed and direction are similarly averaged.
Observations from the METEOR were reduced to a
height of 2.5 m assuming a log profile and Zo = 0.015
cm.
Comparison of means from the buoys and the R/V METEOR.
3
26
The records, parts A, B and C, are each 59 hr long
and are defined in Table 3. Means from the. R/V
METEOR are the averages of hourly ship observations.
The symbols are defined as follows:
u, wind speed;
e, wind direction;
T
air temperature; Tsl, sea
temperature at 0.5 m depth (buoy) or bucket temperature (METEOR); T 2, sea temperature at 2 m depth.
The temperature, Isl, in part A from the R/V METEOR
was corrected by subtracting 0.40C from the observed
mean following the suggestion of A. Macklin (personal
,
communication).
4
Comparison of along-wind eddy travel times estimated
by use of Taylor's hypothesi- (Tf), from lags (TU)
associated with peaks in th cross-correlation of wind
speed measured at buoys lying on ,a line parallel to
the mean wind direction and from similar-lags (Tt)
associated with peaks in the cross-correlation of
temperature.
27
ANALYSIS OF METEOROLOGICAL OBSERVATIONS
FROM AN ARRAY OF BUOYS DURING JASIN
I. INTRODUCTION
In the past ten
years,
many observational and theoretical inves-
tigations have been directed toward understanding mesoscale processes
Internationally or-
in the atmospheric boundary layer over the sea.
ganized programs, all part of the Global Atmospheric Research Program
have included:
(GARP),
1) the Air-Mass Transformation Experiment
(AMTEX);
2) the Barbados Oceanographic and Meteorological Experiment
(BOMEX);
3) the GARP Atlantic Tropical Experiment (GATE); and 4) the
Joint Air-Sea Interaction
(JASIN) Experiments.
The observations
re-
ported in this paper were made from an array of meteorological buoys
about 400 km northwest of Scotland in the summer of 1978 as a part
of JASIN.
The JASIN project was proposed in 1966 by the Royal Meteorolog-
ical Society as an appropriate United Kingdom contribution to the
GARP.
A summary of the scientific and operational plans for the
experiment is given by Pollard [1978].
JASIN were:
The primary objectives of
"(1) to observe and distinguish between physical
pro-
cesses causing mixing in the oceanic and atmospheric boundary layers
and relate them to mean properties of the
layers;
(2) to examine and
quantify aspects of the momentum and heat budgets in the ocean and
atmospheric boundary layers and fluxes across and between them."
The objectives of this paper are to analyze the meteorological
observations obtained from an array of buoys deployed during JASIN.
We will describe temporal and spatial variability and examine the
2
data for the existence of organized structures, such as horizontal
roll vortices.
3
II.
INSTRUMENTS
Moored, toroidal buoys provided the platform for the instruments.
They
were similar to those used in JASIN 70 and 72 [Burt
Wind speed and direction were measured with a cup
et al., 1974].
anemometer and a highly-damped wind vane and magnetic compass system
manufactured by Ivar Aanderaa of Bergen, Norway.
Dry and wet-bulb
temperatures were measured with thermistors exposed to the air inside
radiation shields ventilated
by the wind.
temperature were not reliable because
the thermistor
entirely
of the difficulty
of keeping
wetted by means of a wick and reservoir and
The solar radiation sensor was
were excluded from the analysis.
manufactured by Lintronics.
mean sea level.
The measurements of wet-bulb
The instruments were mounted 2.5 m above
Water temperatures were measured at 0.5 m and 2 m
depth with rugged Aanderaa platinum resistance thermometers.
The data
were recorded digitally on magnetic tape by an Aanderaa
data logger attached to each
buoy.
Wind speed was averaged over
sampling intervals while the other variables were sampled instantaneously.
Variables were sampled at intervals
of 3.5 or
1.75 minutes.
Data obtained by instantaneously sampling a fluctuating record
are subject to aliasing errors.
If fluctuations are present with
frequencies greater than the Nyquist frequency (half the sampling
frequency),
spectral energy at frequencies greater than the Nyquist
will be folded back to lower
frequencies.
Despite damping, the wind
direction measurments were particularly susceptible to aliasing error.
The error is magnified by erroneous fluctuations in wind direction
4
induced by the motion of the buoy.
R. Weller-[personal communication,
1979] has compared rotary spectra measured by a vector-averaging meter
with spectra from an Aanderaa cup and vane and found excess energy in
the Aanderaa spectra in the highest decade of frequency.
Measurements
of temperature and solar radiation are not seriously affected by
aliasing because the response time of the sensors is generally about
one minute.
The measurements of wind speed are not expected to be seriously
in error.
Even though the buoy motion induces fictitious fluctuations
of wind speed, averaging over the sampling interval practically eliminates aliasing.
The effects of buoy motion on measurements of mean
wind speed have been estimated by Pond [1968] and Badgley et al.
[1972] and are expected to be small.
5
III. OBSERVATIONS
Observations were made from 28 July to 6 September 1978 about
400 km north-west of Scotland at the four
1
and Table 1.
As shown in Table 1, the measurements were briefly
interrupted on 12 and 30
buoy.
locations shown in Figure
August to
change the data logger at each
The sampling interval was 3.5 minutes during the
first two
periods and 1.75 minutes during the last period.
Meteorological observations were also taken from ships operating
in the
area.
The most complete record was taken
by the R/V METEOR.
She was stationed near buoys B1, B2 and B3 during the experiment.
Meteorological measurements were also made from other buoys.
The general weather in
early
August was influenced by high pres-
sure in the Norwegian Sea resulting in north winds in the experimental
In the middle of
area.
experimental site.
August,
two low pressure systems passed the
In late August, there were westerly winds due to
stationary high pressure west of
England.
The strongest winds during
the experiment occurred over a period of several days beginning on 17
August,
reaching a maximum of 15 m/s on 20
sea temperature decreased by about 1°C during
as the result of deepening
decrease of wind speed 24
of the
August,
about 1°C over a period of several
The near-surface
August.
well-mixed
this
event, presumably
layer.
Following the
the sea surface temperature rose
days, very likely
due to weak
mixing and net heating of the upper layers.
A progressive vector diagram of the wind at B3 is shown in Figure
3. The first section of
the wind direction record from B3 was cor-
rected prior to plotting Figure 3.
The correction was based on a
6
linear regression
to the data from B2 and B3.
Three parts of the
record, A, B and C, each 2.5 days long, were selected for the crosscorrelation analysis discussed
in subsequent
sections.
The criterion
used in making the selections was to require that the wind be nearly
constant
in speed and
direction.
The times
of beginning
and ending of
each part are tabulated in Table 2 together with average bulk
Richardson numbers, wind direction and wind speed.
The effect of the
vertical humidity gradient on the bulk Richardson number was included
by use of the hourly wet and dry bulb temperature observations from
the R/V METEOR.
The effect was equivalent to an air-sea potential tem-
perature difference of -0.31, -0.08 and -0.16°C for parts A, B and
C respectively.
The stratification during part C was close to neu-
However, the estimates
tral.
(B3, B3,
METEOR) used to obtain the mean
bulk Richardson number are all negative making it highly probable that
the stratification
was unstable during part
C.
No allowance was made
for a cool skin temperature in the calculation of the bulk Richardson
number.
However, the error (- 0.1°C) is probably compensated by
errors caused by daytime radiatior
I
heating of the air temperature
sensors.
The accuracy of the measurements can be estimated by comparing
averages from the buoys and the R/V METEOR. Such a comparison for
parts A, B and C shown in Table 3.
The hourly observations of wind
speed and direction from the METEOR were taken at a height of 23 m
above mean sea level while observations of wet and dry bulb temper-
atures were taken at a height of 11 m.
The wind speeds from the
7
METEOR were reduced to a height of 2.5 m based on the assumption of a
log profile and a roughness length of 0.015
cm.
Measured wind speeds
from B1, B2 and B3 averaged over part A differ by no more than 0.24
m/s with each other and differ no more than 0.1 m/s with means over
parts B and C.
0.5 m/s.
When B4 is included, the means differ by no more than
The difference between B4 and the other buoys may be
accounted for by the distance between B4 and the other buoys (See
Figure 1 and Table
4).
The average over part A of hourly observations
of wind speed from the METEOR (2.5 m) differs with means from B1, B2
and B3 by as much as 1.3 m/s.
in parts B and C.
The difference is no more than 0.5 m/s
Part of the difference may be ascribed to an error
in reduction of wind speed from the METEOR to a height of 2.5 m, i.e.
the neglect of the effect of stability and
roughness length.
uncertainty
in the value of
In addition, the effect of interference of the ship's
hull with the air flow could cause an error in measurements from the
METEOR.
In
summary,
agreement to within 0.5 m/s between the buoys and
METEOR should be considered good.
There were systematic errors in the observation of wind direction
from some of the buoys (See Table 3).
Observations from B1, B3 and
B4 averaged over part A were in error by about 40°.
Observations from
B4 averaged over parts B and C continued to systematically disagree
with the other means by
24°
and 40° respectively.
The discrepancy is
too large to be ascribed to the separation between B4 and the other
buoys.
A possible source of error is the
disturbance.
of the magnetic
field by ferromagnetic materials, although this possibility was
8
minimized by the use of aluminum for the structure of the buoy.
Means from the METEOR and those buoys considered reliable are in
excellent agreement, within 4°, 2° and 9° in parts A, B and C respectively.
The comparison of mean air temperatures tabulated in Table 3
shows temperatures from B2 systematically in disagreement with the
other observations.
The cause of the error is undetermined.
Fluc-
tuations in temperature measured at B2 did not appear to be affected.
Mean temperatures measured at B4 are on average
a few tenths °C
colder than temperatures from Bi and B3, possibly because of the
northward displacement of B4 from the other buoys.
Mean air temper-
atures from Bl and B3 are within 0.45°C of each other.
Mean air
temperature from METEOR is always at least 0.1°C and never more than
0.5°C cooler than temperature from B1 and B3.
The disagreement among
means from different buoys and METEOR may be Fartly caused by the
natural variability of air temperature.
There may also be errors,
e.g. daytime heating of the sensors by solar radiation.
Sea temperature was measured it 0.5 and 2 m depth at most of the
buoys.
The agreement between means from both depths is excellent,
the magnitude of the difference never exceeds 0.11°C and averages
0.04°C.
In only one case is the mean from the upper sensors warmer
than the lower mean, suggesting that the upper 2 m was unstably
stratified during parts A, B and C.
The wind speed was strong
enough during all parts to cause vigorous mixing of the upper few
meters.
The sense of the temperature gradient suggests that there
9
was, on average, net cooling of the surface.
Mean sea temperatures
from B1, B2 and B3 differ by no more than 0.13°C and differences are
on average 0.03°C.
Mean sea temperatures from B4 are systematically
0.1 to 0.4°C cooler than at the other buoys, which is similar to the
behavior of air temperature.
Mean bucket temperatures from METEOR
differ by no more than 0.13°C with averages over Bl, B2 and B3.
Differences in mean sea temperatures among buoys may be partly ascribed to horizontal temperature gradients.
The difference between
mean temperature at 2 m depth from B2 and B3, the two buoys closest
together (2.6 km), did not exceed 0.02°C in part A, B or C.
We con-
clude that measurements of sea temperatures from buoys show excellent
consistency and are likely to be accurate to within ± 0.03°C.
10
IV. SPECTRA
Spectra of wind
speed,
air temperature and sea temperature shown
in Figures 4, 5 and 6 were estimated by averaging and patching spectra
from different
time series.
The low-frequency estimates (X) in each
of the plots were obtained from a spectral analysis of time series of
hourly
averages from two
buoys,
usually B1 and B3.
The air tempera-
ture record from B2 was used in place of B3 because the record from
B3 was incomplete.
the entire
The time series of hourly averages extended over
43 days of
interpolation.
the experiment with the gaps filled by linear
Zeros were added to the series after subtracting the
mean to increase their length
Fast Fourier
of the
Transform.
to 1024 points permitting the use of the
The number of zeros added was less than 10%
total length of the record in every case.
Spectra were
smoothed by averaging in non-overlapping frequency bands, equally
spaced on a logarithmic
scale.
Finally, spectra from each of two
buoys were averaged to obtain the
Figures 4, 5 and
6.
estimated by analysis
low-frequency spectra shown in
The spectra at intermediate frequencies were
of the first 4096 points
obtained during periods one and t+--, (See
spectra were obtained
from
analysis
of each of the records
Table 1).
of the first
4096 points of
records obtained during the third period (sampling
For both intermediate and high-frequency
for analysis were more than two-thirds
spectra,
of the
The high-frequency
interval,
1.75 min).
the records used
total available length.
The smoothing and averaging used to obtain the intermediate and highfrequency spectra was
spectra.
similar to that
The validity of the
used to obtain the low-frequency
procedure used to obtain the composite
11
spectra can be judged from the agreement between spectra in the overlapping frequency ranges.
The spectrum of wind
speed,
shown in Figure 4, suggests a plateau
at a period of about 20 days, falls off with a slope of about -2 for
periods between 5 days and 2 hr, and falls off with
periods between 2 hr and 3.5
spectrum.
a slope
of -5/4 for
There are no significant peaks in the
min.
Unlike spectra from near-shore locations under the influence
of a sea breeze [Halpern, 1974; O'Brien and Pillsbury, 1974] there is
no significant peak or shoulder at diurnal frequences.
The spectrum of air
temperature,
some respects from the wind speed
a peak or plateau at low
shown in Figure 5, differs in
spectra.
frequencies.
There is no suggestion of
The spectra fall off with slope
about -3/2 for periods between 10 days and 8 hr.
8 hr and 15 min, the slope
is about
-5/3.
For periods between
The increase in slope to
greater than -1 at periods less than 15 min is very likely caused by
aliasing associated with instantaneously sampling a thermistor having a
time response less than 3.5
min.
There is a significant peak in the
spectrum at a period of one day associated with diurnal solar heating of
the lower atmosphere.
The spectrum of sea temperature at 2 m depth is shown in Figure
6.
The spectra fall off with a slope of about -2 for periods between
10 days and 3 hr.
hr and 3.5 min.
The slope increases to -3/2 for periods between 1
There is a large peak in the spectrum at the diurnal
period which is larger in comparison to background energy than the
similar peak in the spectrum of air temperature.
There is no evidence
that the high-frequency end of the spectrum is affected by aliasing.
12
The spectrum of wind speed was examined for consistency with
the concept of a gap or region of low spectral energy, separating
macro- and microscales.
The spectrum in
variance-preserving form in Figure 7.
Figure 5 is plotted in
This form is called variance-
preserving because equal areas under the curve contribute equally to
the variance.
A region of low energy in spectra plotted in this form
is often found between about 0.5 and 5 cph and is referred to as the
spectral
Most observations of this gap have been over land (Van
gap.
der Hoven, 1957; Vinnichenko, 1970; Fiedler and Panofsky, 1970].
Millard
[1968]
taken over the
found a prominent gap between 0.1 and 10 cph in spectra
However, the observation may be suspect because
sea.
of errors caused by buoy motions.
Our spectra do not extend to
sufficiently high frequencies to demonstrate by themselves the
existence of a spectral gap.
We have, therefo-°e, plotted the simi-
larity spectrum of Kaimal et al. [1972] to extend the spectrum to
high frequencies.
In so
drag coefficient of
observation
height
doing,
a vat" equivalent to 1,3xl0-3 for an
1.8x10-3,
of 10 m.
we assumed neutral stability and a
KaimL, et al's. spectrum matches ours
at intermediate frequences and is
fication for using
consi-tent with a gap.
The justi-
the Kaimal spectrum is strengthened by the obser-
vation that microscale spectra
over the sea scale similarly
to those
over land [e.g. Leavitt, 1975].
For purposes of additional comparison, the spectrum of wind speed
over land from Smedman-Hogstrom and Hogstrom [1974] is also shown
in Figure 7.
The microscale peak in Smedman-Hogstrom and Hogstrom's
13
spectrum occurs at lower frequences than in Kaimal et al's. spectrum
because conditions were unstably stratified for the spectrum reported by
Smedman-Hogstrom and Hogstrom.
The shift in the peak associated with
stratification changing from neutral to unstable agrees qualitatively
with Kaimal et al. [1972].
Rotary spectral analysis is a useful technique for analyzing
time series of two-dimensional vectors [Gonella, 1972; Mooers, 1973].
The rotary spectrum is composed of two parts, clockwise and counterclosewise components which correspond to the distribution of variance
with frequency of fluctuations associated with clockwise and counterclockwise rotation respectively.
For example, if there is a peak in
the clockwise component larger than that in the counterclockwise at
the same frequency, and the rotary coefficient is -1, that means the
vector rotates clockwise at the prescribed frequency, its tip tracing
a circle.
The rotary spectrum of hourly averages of horizontal wind veloThe spectrum was smoothed
city observed at B3 is shown in Figure 8.
as previously described
in non-overlapping
frequency
bands, 10 per
decade. The clockwise spectral density exceeds the counterclockwise
for frequencies above .015 cph.
This result agrees with observations
reported by Burt et al. [1974] who found clockwise spectral levels
generally higher than counterclockwise.
However, Burt et al. also
found evidence of diurnal and inertial oscillations in the clockwise
spectra, evidence of which is lacking in Figure 8.
Inertial oscilla-
tions are expected to be small in the atmosphere [Holton, 1972], may
depend on weather conditions and may not be sufficiently persistent
14
or energetic to appear in the spectrum of a 43-day record.
Diurnal
variations in wind will likely be associated with diurnal fluctuations
in stability which may have been small during JASIN.
15
V. TAYLOR'S HYPOTHESIS
It is a common and ordinarily well-justified practice to convert
frequency spectra of microscale turbulence to wavenumber spectra by
use of Taylor's hypothesis, the hypothesis that turbulence structure
changes slowly while being advected past a point by the mean wind
speed.
It is tempting to also use Taylor's hypothesis to infer the
statistics of mesoscale structure because time series at a single
point are usually more easily obtained than spatial samples. However,
the justification for using Taylor's hypothesis to infer mesoscale
spatial structure is not well established.
An analysis was carried out to test the validity of Taylor's
hypothesis for mesoscale
structure.
The three wind speed and air
temperature records, parts A, B and C (Table 2) were used in the
analysis.
The autocorrelation function of wind speed averaged over
all buoys is shown in Figure 9 for each part.
If Taylor's hypothesis
is strictly true, the cross-correlation coefficient computed between
buoys lying along the path of the mean wind will be equal to the
autocorrelation function at a lag, r = x/u where x is the separation
between the buoys and u is the mean wind
speed.
Values of the cross-
correlation coefficient plotted in Figure 9 are qualitatively consistent with Taylor's hypothesis.
The autocorrelation function of air
temperature in parts A and B averaged over all buoys is shown in
Figure 10 together with cross-correlation coefficients between buoys
lying along the path of the mean wind.
Part C was not included be-
cause the air temperature record from B1 was incomplete.
The
16
cross-correlation coefficients are qualitatively consistent with
Taylor's hypothesis except that in part B the two cross-correlation
coefficients involving the air temperature at B2 are in very poor
agreement with Taylor's hypothesis.
The reason may be the erroneous
drift in the mean value of air temperature at B2 which was previously
noted (Table 3).
A comparison between autocorrelation functions and cross-correlation coefficients
was also
carried out on time series which were
filtered to remove the effect of long-period fluctuations.
The wind
speed and air temperature records from parts A, B and C were high-pass
filtered by subtraction of a running two-hr mean. This filter passes
100% of the spectral energy at a period of two hr and 50% at five hr.
Two hours
is long
compared to the distance between buoys divided by
the mean wind speed. The filtered time series of wind speed and air
temperature were analyzed identically to the unfiltered series as described above.
The comparison between autocorrelation functions and
cross-correlation coefficients is shown in Figures 11 and 12 for wind
speed and air temperature respectively.
with Taylor's hypothesis in parts
The results are consistent
and C and inconsistent in part B.
The results from part B suggest that mesoscale eddies propagate about
twice as fast as the mean wind.
Propagation speeds of mesoscale structures were estimated by
examining cross-correlation functions of high-pass filtered wind speed
and air temperature from parts A, B and C.
An estimate of the propa-
gation time of an eddy between a pair of buoys lying along the path of
17
the mean wind was taken as the lag at which the cross-correlation
function is a maximum.
An example of two cross-correlation functions,
one of wind speed and the other air temperature, is shown in Figure
13.
The estimates of propagation times are tabulated in Table 4 and
are compared with propagation times computed by use of Taylor's
hypothesis.
The results from parts A and C are consistent with
Taylor's hypothesis while the results from part B show
eddy propa-
gation times about half as large as those predicted by Taylor's hypothesis.
The results in Table 4 are consistent with the comparison of
autocorrelation functions and cross-correlation coefficients shown in
Figures 11 and 12, i.e. mesoscale structures travel with the mean
wind in parts A and C but travel twice as fast as the mean wind in
part B.
The reason Taylor's hypothesis fails in part B is probably
associated with frontal passages.
Examination of the barometric
pressure record and the synoptic analysis shows that there were
frontal passages on 18 August about 12 hr into part B and on 20
August near the end of part B.
These frontal passages are visible as
shifts in wind direction in the progressive vector diagram shown in
Figure 3.
The propagation in a direction approximately normal to the
mean wind of pressure disturbances and air masses associated with the
fronts accounts for the failure of Taylor's hypothesis in part B.
18
IV.
HORIZONTAL ROLL VORTICES
There is growing theoretical and observational evidence [Brown,
1970; Kuettner, 1972; Lemone,
1973; Agee et al., 1973; Burt et al.,
1974; Agee and Dowel, 1974; Burt and Agee, 1977] that horizontal roll
vortices are a common feature of the planetary boundary layer.
A
schematic diagram of the circulation associated with these vortices
is shown in Figure 14.
An analysis was carried out to investigate whether there was
evidence of roll vortices in the buoy measurements.
of
course,
It is possible,
that even though there might be vortices present in the
planetary boundary
layer,
their influence on the variability of velocity,
temperature and solar radiation 2.5 m above the sea surface might be
undetectable.
If they are felt at the
they might have impor-
surface,
tant influences on the circulation of the uppe
ocean.
Evidence for the existence of roll vortices was sought by examining
the cross-correlation functions of high-pass filtered data from parts
A, B and C (Table
An example c
2).
the cross-correlation between
wind speed and air temperature durong Part C is shown in Figure 15.
zero lag there is a negative
correlatio1,
between wind speed and air
temperature associated with downward propagation
excess of
momentum.
This result
rolls shown in Figure 14.
cation of
the presence
The result
with cellular convection and perhaps
ture.
of cool
air having an
is consistent with the schematic of
However, it is by no
of rolls.
At
means conclusive verifi-
would also be consistent
other types
The case in favor of rolls is strengthened
of mesoscale strucby the periodic
19
nature of
the cross-correlation function, consistent with the migra-
tion of rolls normal to the mean wind direction.
Assuming the rolls
have cross-wind dimensions of about 1 km, the period of 1 hr is con-
sistent with a migration velocity of about 30 cm/s and an angle of
2° between the roll axis and the mean wind direction.
Cross-correlation functions from other buoys in part C and from
buoys in parts A and B are qualitatively similar to Figure 15 except
that the oscillation of the functions is usually not as periodic.
The cross-correlation functions at zero lag in part B are positive as
might be expected because the stratification was stable (Table 2).
20
Acknowledgments.
by Frank
Evans.
The preparation of the instruments was carried out
Jay Simpkins and James Wagnerassisted in the install-
ation and retrieval of the instruments. Members of the Buoy Group of
the Woods Hole Oceanographic Institution installed and retrieved the
moorings.
We enjoyed the cooperation of the
scientists,
officers
and crew of the R/V Atlantis II; David F. Casiles, commanding;
Melbourne G. Briscoe, Chief Scientist.
by the Office
This
research was supported
of Naval Research through contracts
and N000'14-79-C-0004 under project NR 083-102.
N'00014-76-C-0067
21
REFERENCES
Agee, E. M., T. S.
Chen, and K.
E. Dowell, A review of mesoscale
cellular convection, Bull. Amer. Meteorol. Soc., 54, 1004-1012,
1973.
Agee, E. M., and K. E. Dowell, Observational studies of mesoscale
cellular convection, J. Appi. Meteorol, 13, 46-53, 1974.
Badgley, F.
1., C.,A. Paulson and M. Miyake, Profiles of wind,
temperature and humidity over the Arabian Sea, Intern. Indian
Ocean Exped. Meteor. Mono., 6, 62 pp, The University Press
of Hawaii, 1972.
Brown, R. A., A secondary flow model for the planetary boundary
layer, J. Atmos. Sci., 27, 742-757, 1970.
Burt, W. V., T. Cummings, and C. A. Paulson, The mesoscale wind field
over the ocean, J. Geophys. Res., 79, 5625-5632, 1974.
Burt, W. V., and E. M. Agee, Buoy and satellite observation of
mesoscale cellur convection during AMTEX 75, Boundary layer
Meteorol., 12, 3-24, 1977.
Fielder, F., and H. Panofsky, Atmospheric scales and spectral gaps,
Bull. Amer. Meteorol. Soc., 51, 1114-1119, 1970.
Gonnella,
J., A rotary-component method for analyzing meterological
and oceanic vector time series, Deep Sea Res., 19, 833-846, 1972,
Halpern, D., Summertime surface diurnal period winds measured over an
upwelling region near the Oregon coast, J. Geophys. Res., 79,
2223-2230, 1974.
Holton, J. R., An introduction to meteorology, in International
Geophysical Series, Vol. 16, Academic, New York, 1972.
22
Kaimal, J.
C.
J. C.
Wyngaard,
Y. Izumi, and 0. R. Cote, Spectral
Characteristics of surface layer
Meteorol.
Soc.,
and theory,
M.
Quart. J. Roy.
98, 563-589, 1972.
J. P., Cloud bands in the earth's
Kuettner,
LeMone,
turbulence,
Tellus,
23,
atmosphere:
observations
404-426, 1971.
A., The structure and dynamics of horizontal roll vortices
in the planetary boundary layer,
J. Atmos.
Sci., 30, 1077-1091,
1973.
Leavitt, E., Spectra characteristics of surface layer turbulence
over the tropical ocean, J. Phys. Oceanog., 5(1), 157-163,
1975.
Millard, R. C., Wind measurements from
Tech.
buoys;
A sampling scheme,
Rep. 68-68, 34 pp., Woods Hole Oceanogr. Inst., Woods
Hole, Mass., 1968.
Moore,
C. N. K., A technique for the cross spectrum analysis of
pairs of complex-valved time series, with emphasis on properties
of polarized components and rotational
invariants, Deep Sea
Res., 20, 1129-1141, 1973.
O'Brien,
J. J. and R. D.
a seabreeze regime,
Pillsbury,
J.
Appl.
A note on rotary wind spectrum in
Meteorol.,
Vol. 13,
No. 7, 1974.
Pollard, R. T., 1978, The Joint Air-Sea Interaction Experiment-JASIN
1978.
Bull.
Amer. Meteor.
Soc., 59(10), 13/0-/318.
Pond, S., Some effects of buoy motion on measurements of wind speed
and stress, J.
Geophys.
Res., 73(2), 507-512, 1968.
23
Smedman-Hogstrom,
A. S., and H. Hogstrom, Spectral gap in surface-layer
measurement, J. Atmos. Sci., 32, 340-350, 1975.
Van der Hoven, Power spectrum of horizontal wind speed in the frequency
range from 0.0007 to 900 cycles per year, J. Meteorol., 14,
160-164, 1957.
Vinnichenko,
N. K., The kinetic energy spectrum in the free atmos-
phere 1 second to 5 years, Tellus, 22, 158-166, 1970.
24
TABLE 1.
Locations
and periods
of buoy observations,
JASIN - 1978.
Location
Buoy
Lat.
(N)
Long. (W)
Period 1
Begin End
(GMT)
Bi
B2
B3
B4
590
00.4'
590 00.2'
590
590
01.6'
10.7'
12°33.6'
12°27.5'
12°27.4'
12°31.0'
Period 2
Begin End
(GMT)
Period 3
Begin
End
(GMT)
8/1
8/12
8/12
8/30
8/30
9/6
1221
1538
1553
1302
1409
1100
7/29 8/12
8/12
8/30
8/30
9/6
1030 1847
1859
1235
1247
912
7/28 8/12
8/12
8/30
8/30
9/6
2206 1917
1938
1022
1040
750
7/28 8/12
1350 1253
8/12
8/30
8/30
9/3
1317
1545
1612
1328
TABLE 2.
Parts of meteorological records having approximately constant
wind speed and direction which were selected for cross-correlation
analyses. The beginning and ending time for each part is 0000 and
1140 GMT respectively.
Rig is the mean bulk Richardson number,
averaged over reliable buoys and the R/V METEOR.
Wind speed and
direction are similarly averaged. Observations from the METEOR
were reduced to a height of 2.5 m assuming a log profile and
Zo = 0.015 cm.
Part
Time (GMT)
Begin
End
RiB
Wind
Wind
pee d
Di rec ti on
S
(z = 2.5 m)
(degrees)
(m/s)
-0.0032
357
6.6
8/6
8/8
B
8/18
8/20
0.0004
172
11.1
C
8/22
8/24
-0.0001
266
8.8
TABLE 3.
Comparison of means from the buoys and the R/V METEOR. the records, parts A, B and C, are each
59 hr long and are defined in Table 3. Means from the R/V METEUR are the averages of hourly ship
The symbols are defined as follows: u, wind speed; 0, wind direction; T air
1, sea temperature at 0.5 m depth (buoy) or bucket temperature (MEIEOR);8Ts2,
sea temperatures at 2 m depth. The temperature, Tsl, in part M from the R/V METEUR was corrected
by subtracting 0.4°C from the observed mean following the suggestion of A. Macklin (personal
observations.
temperature; T
communication).
Part A
Part B
Buoy
or
u
6
Ship
(m/s)
(deg)
B1
6.82
42
B2
6.99
B3
Ta
u
e
Ta
Tsl
Ts2
u
e
Ta
(m/s)
(deg)
(°C)
(°C)
(°C)
(m/s)
(deg)
(°C)
172
13.70
12.85
12.87
8.98
270
11.1
173
15.45
12.89
12.91
8.94
7.95
11.1
170
13.50
12.85
12.91
-
12.71
10.7
148
13.27
-
13.05
-
13.95
171
13.43
12.83
Tsl
Ts2
(°C)
(°C)
11.53
12.97
13.00
11.1
355
12.30
12.97
12.93
7.06
42
11.98
12.84
B4
6.58
324
11.37
METEOR
7.08
359
11.45
METEOR
5.8
@2.5m
(°C)
Part C
11.4
Tsl
Ts2
(°C)
(°C)
-
12.13
12.13
264
15.30
12.07
12.14
8.90
269
12.21
12.12
12.13
12.52
8.48
226
12.03
-
12.06
-
10.39
261
12.07
12.24
-
8.5
TABLE 4.
Comparison of along-wind eddy travel times estimated by
use of Taylor's hypothesis (Tf), from lags (TU) associated
with peaks in the cross-correlation of wind speed measured
at buoys lying on a line parallel to the mean wind direction
and from similar lags (Tt) associated with peaks in the
cross-correlation of temperature.
BUOY
SEPARATION
PAIR
(km)
Part B
Part A
Tf
Tu
Tt
Tf
(min)
Part C
Tu
Tt
Tf
(min)
Tu
Tt
(min)
Bl-B4
19.3
46
50
43
29
16
16
-----------------
B2-B4
19.8
46
43
47
29
15
12
-----------------
B3-B4
17.2
40
38
41
25
15
15
-----------------
B2-B3
2.6
6
9
9
4
4
Bl-B2
5.9
-- ----------- ---
-- ----------- ---
----------------11
10
9
28
60° N
B4
f
59-ION
IRELAND
83
BI
B2
59-OON
10°W
12-35W
I
Figure 1.
12-30W
I
Locations of meteorological buoys, JASIN-1978.
29
20 r
WIND SPEED
M/S
0
WIND DIRECTION
360
DEG
°C
SOLAR RADIATION
600
I i
W/ M2
I
0
SEA TEMP AT 0.5 M
15
°C
10
SEA TEMP AT 2.0 M
15
oC
10
3 .1
JUL AUG
Figure 2.
10
20
30
1
SEP
Time series of hourly averaged variables observed at
B3 from 28 July to 6 September 1978.
30
+5000
K-C--)
+5000
Figure
3.
Progressive vector diagram of wind at B3 from 2300 GMT
on 28 July to 6 September 1978. Each square is
plotted at 0000 GMT.
31
PERIOD
1Oday
I hr
Iday
10min
107
106
105
I
E
xx
x
103
102
10
10-7
10-6
10-5
10-4
10-3
2
FREQUENCY (Hz)
Figure 4. Composite spectrum of wind speed from Bi and B3. The
symbols X are spectra from one-hourly average p are
spectra from 3.5-minute averages, and + are ectra
from 1.75-minute averages. The vertical bars show
the 90% confidence interval.
32
pfR100
14
OIQ'
FREaUENOY
Figure 5.
The sy l
C°mPp5jte°}s
X
tO
ait
(Nzl
and B3
temperat re1edrom Figure
in
4- , and I are de
33
PERIOD
loday
iday
1 hr
10min
106
x
x
105
104
103
f
102
10
1
10-'
++
10-2
10-3f
-
10-6
..
10.5
10_4
10-3
.....- -I
10-2
FREQUENCY (Hz)
Figure 6.
Composite spectrum of sea temperature from R' and B3.
gure 4.
The symbols X, 0, +, and I are defined in
34
fS(f)
I
T,
I
X
X
X
S
X
X
X
X
X *X
xx
to
° L
Figure 7.
Variance-preserving plot of the spectrum of wind
speed from B1 and B3 together with the spectrum from
Kaimal et al. [1972]. The symbols X, [3, and + are
defined in Figure 4, and o is Kaimal et al's [1972]
spectrum. The broken line shows the spectrum measured
by Smedman-Hogstrom and Hogstrom [1975] over land.
35
I07
U
U)
E
106
Q
--
0
10
w
a-
104
Q
0
103
102
[
10-7
I
.
10-6
10-6
.1
10-4
10-3
F (Hz)
w
Figure 8.
Rotary spectra (A) and rotary coefficient (B) of hourly
averaged wind velocity from B3. The broken line
represents clockwise rotation and the solid line
represents counterclockwise rotation.
36
2
3
0.5
0.5
J(hours)
I
Figure 9.
2
3
Mean auto-correlation functions of unfiltered wind
speed from parts A, B and C. The auto-correlation
functions are averages over buoys 61, B2, B3 and B4.
The lengths of the vertical bars are twice the
standard deviation. Cross-correlation coefficients
from pairs of buoys lying along the mean wind direction are plotted. The symbols X$ and + represent the combinations B1-B4, B2-64762-B3, and B3-B4
respectively in parts A and B. The symbol X represents the combination Bl-B2 in part C.
37
3
0.5
0.5
x1
(hours)
0
Figure 10.
2
3
Mean auto-correlation functions of unfiltered air
See Figure 9 for
temperature from parts A and B.
Part C is not included because the
explanation.
temperature record from Bl was incomplete.
38
i
0.5
C
(hours)
2
3
0
-0.5--
Figure 11.
Mean auto-correlation functions of filtered wind speed
from parts A, B and C.
See Figure 9 for explanation.
39
0.5
Figure 12.
Mean auto-correlation functions of filtered
perature from parts Aand B. Part C is not
because the temperature record from
plete.
air temincluded
Bi was incom-
40
Figure 13. Example of cross-correlation functions of wind speed
(u) from Bl and B4 and air temperature (Ta) from the
same buoys used to determine the eddy travel time in
the downwind direction. The records are high-pass
filtered, part A.
41
MIGRATION
WIND VELOCITY FLUCTUATION
T
AIR TEMPERATURE FLUCTUATION
Figure 14. Schematic diagram of horizontal roll vortices and
associated fluctuations of horizontal wind velocity
and air temperature (assuming unstable stratification).
2
U,
0
NOI1V138800-SS080
I
42
Figure 15. Cross-correlation function of high-passed wind speed
Positive lags
and air temperature at B4, part C.
indicate that air temperature leads wind speed.
APPENDIX
43
APPENDIX
Hourly Averages From Buoy B3
There follows a listing of hourly averages from buoy B3.
averaging interval extends from a half hour before the hour
hour after the hour.
speed; DIR,
The symbols are defined as follows:
wind direction; TA, air
temperature;
The
to a half
U, wind
TS1, sea temperature
at 0.5 m depth; TS2, sea temperature at 2 m depth; R, incoming solar
radiation.
Wind speed and direction and air temperature were measured
2.5 m above mean sea level.
Wind speed direction has been corrected
between the beginning of the observations and 1917 GMT on 12 August
based on a linear regression between B2 and B3.
44
MN D Y HR
l.1
(M/S;)
(GMT)
7
7
28 23
29 0
29
7
1
.1.
6.36
6.15
5.97
5.62
5.01
29
a.
29
7 29
4
2.5:3
7 29
7 29
7 29
5
1.88
6
7
2.61
3.56
29
7 29
0
4.71
29
10
7
7
9
7
7
7
29 11
29 12
29 13
7
2
14
15
16
17
18
19
29
29
29
29
7 29
7 29 20
7 29 21.
9 22
7 29 23
7 30
0
7 30
1
7 30
2
7 30
3
7 30
4
7 30
5
7 30
6
7 30
7
7 30
8
7 30
9
7 30 10
7 30 11
7 30 12
7 30 13
7 30 14
7 30 15
7 30 16
7 30 17
7 30 18
7 30 19
7 30 20
,
30 21
7 30 22
7
/'
7
7
6.41
6.62
7.51
8.76
8.05
I? is R
(Di..:G)
168
167
143
147
136
114
27
TA
T S 1.
T S2
(C)
(C)
(t_)
13.08
13.12
13.12
13.08
12.73
:12.2;
12. 41
12.39
12.52
12.38
12.50
12.49
12.48
12.49
12.50
12.5()
12.51
12.53
12.56
12.60
12,65
12.67
12.63
12.66
12.69
12.75
12.78
12.80
12.79
343
12.27
289
12.73
12.37
12.36
12.36
12.37
12.36
12.38
249
251
23()
237
237
229
13.0 7
12.4:1
12.17
>-
i
12,44
12.48
6.42
13.47
13.36
13.29
13.45
13.51
2.17
217 13.58
215 13.69
205 13.74
195- 13.80
199 13.68
184
13.58
182 13.36
6.36
221
3
5.94
6.48
6.80
6.89
6.12
6.16
5.09
4.69
12.6:1
204
189
201
202
205
195
218
13.23
12.61
/.49
7. 0 7
6.49
6.63
6.25
6.19
6.21
068
4.33
4.00
3.91
4.32
4463
4.49
3.73
3.94
3.66
3.56
3.67
3.62
3.71
3.66
3.51
220
211
197
2(02
197
204
2:10
210
264
249
262
267
277
290
303
302
293
13. 1 8
13.15
13.20
13.15
13.:17
12.92
13.19
1.3.58
13.61
:13.60
13.61
13.59
13.56
13.58
13.84
13.139
14.03
14.07
14.08
14.21.
13.90
13.59
13.35
12.53
12.53
12.55
12.52
12.54
12.57
12 . 63
12.66
12.67
:12.66
12.6
12.61
:12.61
:12.6:1.
12.63
12.58
:12.54
12.54
12.52
12.52
12.53
12.61
12.71
12.80
1.2.87
:12.9
J.3.09
13-18
13.21
13.12
13.22
13.30.
:1.2.78
12.73
12.73
12.73
12.73
12.74
12.75
:12.70
12,66
12.66
12.65
1.2.64
12.65
12.72
Q.02
12.90
12.98
13.07
13.19
13.29
:13.32
:13.14
13.30
13.34
13,42
13.38
13.27
13.14
13+27
13.26
R
(W,1**'
0.82
1.2-.3
9
6.15
6.15
1.64
6.1,.!
40.5-f','
131,96
154.05
357.37
484.4:1.
509.82
352.86
548.75
534.00
505.11
450.81.
399.99
323.76
204. 0 9
132.37
21.31
0.39
0.00
0.4:1.
0.00
0.82
0.00
0.41
9.68
137.7()
224.58
310.65J
420.07
465.56
516.79
460.98
503.26
540.15
494.25
428.68'
354,91
279.50
239.59
120.90
30.::33
0.00
)
45
MN D Y HR
(GMT)
u
Ii:i
(,MIS)
>c
.
9
3f45
3.45
3a Jl2
3.8.2.
4.48
4.93
4.72
3.62
3.39
3.78
.y>.2
2.86
3.14
3.13
3.51
2.59
2.42
3.18
4.32
4.32
4ati) .S:5.t
5.25
4.61.
3.64
3.89
3.95
4.26
6.84
4.80
;.#.,:.2
3.33
.!.y-/;..
2.86
4.30
5.04
4.89
4.26
3.02
3.71
4.34
3.88
4.62
4.02
3.81
3.26
4.30
3.66
11:CR
f.LDEU;)
2 8!
295
292
281
TA
7'i 1.
'Tr S;2
(0)
(C)
(C)
l
(Wi M**:2.)
13. 1 2
13.25
13.14
13.14
1.23
0.41
0.82
0.39
0.00
0.41
15.57
143.85
263.93
343.43
428.47
405,32
13.31
13.24
13.25
:1.:3a 16
17.08
' 13. ! 7
12.91
12.96
13.01
13.08
:I. ,t6}Z
1.3s:{.2
3:3
1. ,3.:_w
13.82
13.88
14.00
14.14
14.18
14.33
14.10
14.02
13.19
13.30
13.46
13.62
13.70
1,3T18
291
304
314
312
293
299
13.23
13.12
13.45
13.79
13.79
.9 t04
272
270
272
260
245
226
228
240
230
234
248
229
249
223
279
10
310
308
338
1.3.08
1.2.76
1.2.96
1.2.86
277
2:30
13.00
13.01
12.95
1302
13.88
13.90
.
1 3 .81
13.84
:1.3.83
13.70
13.64
13.61.
1308
:13.00
13.04
13.08
13.14
17.20
1.
13.25 1
13.33
13.50
13.69
13.79
13.92
13.95
13.94
13 f 82
13. !'5
13.73
13.57
13.54
13,63
13.67
13.42
12.95
13.10
13.45
13.41
13.50
13.52
13.51
12o68
13. s4 7
1. ,3 ..J 9
13.44
13.43
13.36
13.57
13.55
13.48
13..;
12.46
12.46
1209
1.3.64
13.63
35t.l !
12.66
19 ' fv31.
13.45
8
13
12.89
13.18
13.08
13.14
13.45
13.72
13.37
13.43
13.46
13.47
13.50
13.60
13.68
13.66
13.48
309
7
330
343
332
327
13.67
13.54
331.
:1.3.65
349
359
13.62
13.82
13.80
13.30
12.89
12.17
3
32
54
70
13 . 68
13 f 72
13.69
13.66
13.63
13.64
13.63
1305
13 59
13.59
13.62
13.7{)
13.79
13.79
13.79
13.84
13.81
13.78
13475
13.77
13,76
R
50018
51 8.84
500.80
411.46
467.61
457.89
211.88
151.22
83.19
.43.85
.z
9.43
0.41
0.39
1.235
0.00
0.41
0.00
0.00
6.15
38.61
86.06
145.08
195.00
259.01
286.06
338.10
450.92
343.84
327.45
340.56
223.76
252+45
175,40
39.09
7.79
0.41
46
TA
TS1
(C)
(C)
MN D Y HR R
(GMT)
u
D i. IR.
(M;'S)
(DEB)
4.34
104
105
79
84
12.47
79
12.37
66
63
48
57
12.08
8
1
23
8
8
8
2
0
2
.`
5. 9 4
8
2
8
2
3
4
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6
6.47
5.74
5.24
8
8
8
ri
L
8
8
8
5
8
8
8
3
0
3
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
0
8
8
0
.3
8
8
2
2
2
2
2
2
2
2
7
ri
8
9
10
11
12
13
2 14
2
2
2
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2
15
16
17
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19
2 20
2 21
2 22
2' 3
3
3
3
3
3
3
3
3
3
3
0
1
2
3
4
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5.22
3 . 79
4.83
r.:.35
r
5
11.96
4,'+3
26
.5.2..5.2
21
20
12.28
4.68
5.29
5.36
5.12
5.66
5.90
5.99
6419
6.38
6.65
6.68
7.11
V90
6.55
6.24
7919
7.69
7.75
8.09
7.60
7.04
8'
3 1.9
8
8
3 20
3 21
3 22
1.1.68r
:1.:I..97
8
9
3 18
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11.54
38
6.82
3 17
11
6
7
3 14
3 15
3 16
11 . /
11.50
6
3 1.3
12.60
51
71
is,./()
3 10
3 11
3 12
d 61
12.81
12.83
4.82
4.34
4.11
3.89
Si
8
8
$
22
7
7
357
0
3
11
2
4
11.74
12.41
12.39
12.47
12.50
12.36
12.07
12408
12. 1 9
3
10
12.44
12.78
12.84
12.72
7
12. 46
5
5
3
5
7
12,38
12.45
12.38
12.29
12.40
13
15
:1.2.56
5.71
5.18
5.34
350
346
12.63
12.82
12.95
12.95
12.96
13.06
12.71
4.41
20
12.20
1'
12.12
4
12.2:1.
1
12.71
2
2
:1.3.12
6.1:3
3.67
3.95
5.38
6.47
6.03
8
7
1.5
5
12.99
1S2
(C)
.
R
(W/M**:2)
13.61
13.73
0,00
13.58
13.58
13.58
13.58
13.50
13.40z
13.3 3
13.28
13.23
13.24
13.28
13.33
13.72
13.70
13.71
0.00
0.00
0.00
0.00
1.23
9.43
1 .37
13.38
13 . 38
13.38
13,40
13.41
13.41
13.39
13.38
13.34
13.25
13.20
13.18
13424
13.7:1.
13.62
13.53
1
3.4 5
4
13441
13.36
13.37
13.41
13.45
13.49
13.50
13.50
13.50
13.51
13.53
13.54-
13.51
13.51
13.46
13.37
13.32
13.30
13.36
22 .
95
43.85
54.51
851.24
158.69
231.55
236.47
336.87
284.42
366.38
209.83
120.37
65.98
28.69
11.08
1.64
2.87
0.00
1.16
0.00
0.00
13.27
13.26
13.23
13.24
13.23
13.18
13.10
13.04
:1.3.40
13.01
13-.14
82.78
12.93
13.05
105.32
12,88
13401
109.83
12 4 99
13.11
13.16
13.14
13.05
13,11
13.23
13.28
13.26
13.18
132.78
106.44
71.31
60.24
59.42
13.39
13.36
13.36
13.35
13.30
13.23
1.3.:1.6
0.41.
0.41
2.05
9,02
21.68
63.52
81.15
13.03
13.15
31.97
13.03
13.01
13.15
13.13
21.31
16.39
12.92
13.04
2.32
12.97
13.09
0.82
47
P1i
Li
DY HR
(M/S)
(GMT)
8
8
8
8
8
8
8
8
8
8
8
0
8
8
8
8
8
8
8
8
3
8
8
8
83
$3
8
8
83
8
6
8
8
83
83
8
i
8
8
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3
0
8
8
83
8
8
8
3 23
4
0
4
1
4
2
4
3
,4
4
4
5
4
6
7
4
64
8
9
4
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4 10
4 11.
4 12
4 13
4 14
4 15
4 16
4 17
4 18
4 19
4 20
4 21
4 22
4 23
0
5
1
5
2
5
3
4
5
5
5
5
6
7
5
5
8
9
5
5
,.,
5
5
5
5
5
5
5
5
5
5
5
10
1.1.
12
13
14
15
16
DIR
(.C EC .)
(C:)
R
(W/M:,*')
0 . 82
13,26
13.22
4418
334
331
355
:13.37
13 , 10
13.36
13.11.
1.3.24
32.79
4.03
0
347
13.18
40.16
5., 2
5.20
5435
59
4.69
4.75
504
4.08
2.79
n. ::,
10
359
0
13.20
13.25
13d ?1
13.26
y
1.3.2
347
.1 3
22
1.3413
13.06
12,98
13.18
13.07
13,09
13.09
1.0
v«??
,3 jw)
:12.96
2.70
3.24
2.31
2.44
2.78
2.91
3.29
3.45
3.43
27
349
344
324
341
13.45
13,30
3.34
28
46
72
82
77
1.2.96
12,63
12.64
13.31
13.31
13.29
13.21
13.11
13.09
83
73
59
67
60
59
12445
1.3.12
x..i'ylJ
3.98
4.81
4.40
5.00
4428
4.28
5.58
6.95
6.836
6.41.
6.54
15
28
1.6
1.1
13.29
L ..3,.3
13.27
13.30
13.31
12.93
12,83
12.93
13.08
1202
10
1
18
19
6482
2
7.21.
358
7.20
7.42
7.98
9
13
4
_
1n`7s%'
{()
:12.74
12.61
12.41
0.00
0-39
0.00
9.84
65.16'
13 4 2 }.
127 . 46
.1..«
13.2
111.96
+a1.n2.1
125.00
238;93
.
13 4 18
13.25
13.31
13.32
13.34
13.29
13.1.4
1.3.26
13.21
13.33
13.30
13442
13.15
13.18
13.21
13.23
.1
13.44
13.43
1.3 4 4 0
13.34
1303
1.3 4 20
1.3.25
13.15
13.18
1..:« `}.039
0.00
0.41
0.00
.7 1,)
4
1.3.06
6.05
3
13..18
12+96
13.01
13.22
13,10
12.99
13.00
13.10
12.86
5.12
13.15
13.03
13.03
41
s
:l%
5.6?
1 3 4 183
12486
e:.f35
:,
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5.88
1 .4
13.65
13.03
6422
({.
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,:),
1
13.31
13.39
13.32
13.17
12.55
2.63
12,65
12.70
76
70
63
52
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7.12
5 22
T::2
(C)
13.2()
13.22
13.24
13.23
//
6499
20
T31.
(C)
13.0 2
13.06
13.02
13.05
13.00
13.10
13.13
5.72
5.56
17
5 21
TA
13.18
13.27
13+20
1.3.15
1 7 .., . 83 :1
204.50
114.34
76.64
40.64
'7 4.46
16.80
1.64
0.41.
0.00
0.41
0.39
3.28
0.41
0.00
0.41
12.()
37.29
53.41
:104.10
13.07 i
:1.3.2
n;.:l.
94.67
75.82
13.11
13.08.
13+22
1 6 7.21
13.10 )
1.;:'
13.15
13.16
13.15
13.17
:13.13
:13.14
134 14
13.14
13.20
+21.
1.3.27
13.27
13.27
13.29
13.25
1.3.27
13.25
13.24
215.16
466.38
401.33
331.14
281455
264434
80.74
17.21
2.05
0.39
48
MN LAY HR
8
5
2.3
0
8
6
6
6
2
3
4
8
8
8
8
8
8
8
8
8
8
8
8
8 -,
i5
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8
8
8
8
C'
8
8
8
0
8
8
8
8
8
8
3
8
8
8
_;
8
8
8
8
8
8
8
_;
8
8
8
8
8
8
6
6
6
6
6
,
,6
6
6
1
:.;
6
7
8
9
10
6 11
6 12
6 13
14
.;
1.C:'
6 16
6 17
6 18
6 19
20
6 a..
6 21
6 22
6 23
7
0
6 .)
61
.1
1
7
7
7
7
7
7
7
7
u
n 1: R
(M/S) (DEG)
(GMT)
2
3
4
5
6
7
8
9
7
10
7
7
7
7
7
7
7
11
7
1. S
7
19
7
20
12
13
14
15
16
17
7 21
7 22
8.63
8.66
8.86
9.11
8.63
8,34
8.49
8.62
8.68
8.58
8.68
8.82
8.96
8.46
8,47
8.;3:_ 2
t:
8A1
L:
c3
. :.
1
8.02
7.79
7.68
7.27
6.60
7.12
6.1.8
6.78
6.69
7.04
7.49
7.08
6. 82
6.89
6.56
6,83
7.39
7.:2?'?,
/
7492
7.19
7.36
7.26
6+70
6.15
6.39
5.89
5.75
5.78
5.66
5.98
6.31
10
358
347
357
352
4
7
9
16
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23
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9
8
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13
14
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s. 4 .
14
5
3
358
L: 7
357
356
35()
341
351.
38
339
339
;33 7
344
332
343
344
346
349
350
344
346
TA
is1
(C)
(C)
182
(C)
13.12
1.3. 24
13.22
13.22
1.64
0.00
0.00
13.21
0,
13.19
13.17
13.15
0.00
0.82
0.39
13.02
13.13
'YA. .;
1.:;_9t8
:I.;:?,0y
20.49
36.88
40.57
101.23
12.69
12.62
12.51
12.17
12.12
12.40
12.50
12.4()
12.28
2
1::.:1....
11.92
11.74
11.67
11.99
12,18
1.1..: a0
12,06
12.08
12.01
11.81
1 1. 4 9
11.522
11.59
11.56
11.65
11.64
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+
12 , 86
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12-99
...
12.86
12.81
12.89
12,98
12.93
13.01
1'.2t:Y8(:
{' 2
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12.77
12 A 7 9
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7,
12.89
12.90
1 2_ . 8 9
:l":2.a:.24
:I.:.2 ..7!1
:I.":.2.c3
:12,30
338
341
341
12.95
12.94
12.92
12.90
12.89
13.07
13.06
13.06
13.03
13.03
11,95
12.17
1:1.82
345
:1
:1.2.95
1.3.15
12.67
12.72
12.77
12.70
11.33
11.16
11.52
11.78
352
1
13.09
13.06
13.04
13.04
13.04
12.93
12.93
12.88
12.85
12.82
12.79
12.84
12.89
12.81
:11.65
12.41
12.57
12.56
12.73
12.40
346
350
13.11
13.11
12,32
12.34
12.30
12.30
12.26
11.98
11..60
1.2.81
12 .81
12 . 76
12.72
1 2 .71
12.73
12-74
12.77
12.81
12,85
:12.87
12,82
`.0
1.'Y.c3
12.78
12.75
12.75
1.2.73
12.76
r L...,
12.85
12.85
12.88
12.92
12.95
12.98
1.2.94
12.91
12.90
12.87
12.87
12.85
12.37
(W!M* 2)
4
1.1.81-3
141R 80
129.28
197.13
:3..:
93.85
115.16
99.1
76.64
72.9!.--;
37.54
'
11.013 l:3
0.82
0.41
0.41
0.00
0.00
0.39
0.41
0.00
4.5.1
13.11
39.34
80.74
101.41
193.85
268.43
427-45
480.72
446.71
333.6()
195.85
152.45
99113
68.44
27.87
2.05
0.00
49
MN :ciY
HR
(GMT)
8
8
8
3
8
8
8
8
8
8
8
8
8
W
t:i
8
8
8
8
3
8
8
8
8
8
8
8
8
8
8
8
8
C} ti
8
rt
L}
8
8
8
8
8
8
8
8
8
8
8
8
8
8
3
7 23
0
8
1
8
2
8
8
.3
4
8
8
5
8
6
8
7
-8
8
8
9
LiIR
U
M/ t;)
(DE::G)
6.19
328
347
349
6.18
6.71
6.97
6X5
6.42
5.64
5.29
5.91.
5.42
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13.07
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12.92
12.92
12.92
12.92
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13.06
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331.55
257.37
152.86
97.93
111.06
81.96
15.98
0.41
0.41
50
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HR
DY
(GMT)
9
23
8 10
0
8 10
1
3 10
2
10 3
4
8 10
0 10
5
8 10
6
7
8 10
8 10
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9
8 10 10
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8 10 12
8
8
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8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
8
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DIR
(M/ :3)
(DE G)
6.20
6.54
7.30
7.16
6.76
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12,91
12.90
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12.90
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13.01
13.01
13.01
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151
142
134
12.06
12.09
148
12.35
11.96
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11.70
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7.67
7.64
8.04
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9.04
9.24
9.77
10.25
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139
160
149
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13.59
13.79
13.03
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13.02
127
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13.02
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146
146
158
12.83
12.66
13.14
13.30
13.61
13.65
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10
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10
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18 10.96.
19 10.98
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13.55
13.55
13.68
13,75
13.76
13.91
14.14
14.29
14.50
14.54
14.26
14.12
14.35
14.52
14.37
14.24
13.99
13,55
13.39
13.15
13.07
13.01
13.05
13.20
13.26
13
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10.54
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11.02
10.83
10.94
11
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11
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2
10.49
10.55
10.08
9.85
9.71
9.01
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4
5
6
7
8
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10.23
10.13
15 10.30
16 10.50
17 10,47
18 10.77
19 :10.71
20 10.95
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161
143
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123
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120
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12.92
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12.99
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13,01
13,011
13.01
13,01
13.01
13.03
13.06
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13.13
13.13
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13.13
13.13
13.13
13.09
13.08
13.06
13.02
13.01
13.00
13,05
13,08
13.08
13.08
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13.06
13.04
13.02
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13.02
13.03
13.01
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53.69
99.09
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152.04
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167.21
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0.82
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0.39
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13.00
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13.08
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13 . 0 8
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12.99
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14.7;5
6.15
51
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1:1Y
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(ri/ S) (DEC)
(GMT)
8 11 23 10.40
3 12 0 10.15
8 12 1 10.16
8 12 2 9.72
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8
1'
5
6.47
5.92
6.47
5.06
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120
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235
242
258
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258
248
245
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13.36
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167
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13.36
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13.08
13.088
13.09
13,10
13.13
13.15
13.17
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13.33
13.22
13.22
13.21
13.20
13.20
13.18
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12.66
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13.03
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144,26
174.18
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226.63
365.97
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13.07
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166
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13 t:16
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13.11
13.08
13.08
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13,25
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210
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8 14
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8 15
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10
11
12
13
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16
17
18
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175
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325
321
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10
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13
14
15
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15 21
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232
216
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6.29
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3.39
3.98
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4.59
4.74
7.76
11.78
11.36
11.42
11.61
12.70
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12.50
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12.41
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13.04
13.04
13.06
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13.10
13.14
13.18
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13.32
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13,01
13.03
13.04
13.06
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240
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123.77
136.93
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59.01
22.95
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8
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8
8
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11.85
341
351
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12
13
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12.24
12.18
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20 12.19
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314
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311
294
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262
218
254
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287
2.90
299
312
329
318
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290
287
279
274
280
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179
205
209
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150
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167
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