Temperature changes over storms from measurements of spacecraft TIMED
In the present work we have studied changes of mesospheric temperature over the powerful storms Wilma, Haitang, and Katrina using measurements of the space vehicle TIMED. We have found the temperature increasing at the altitude range 80-100 km. We have found the explanations for the obtained results...
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| Цитувати: | Temperature changes over storms from measurements of spacecraft TIMED / S. Pylypenko, O. Motsyk, L. Kozak // Advances in Astronomy and Space Physics. — 2016. — Т. 6., вип. 1. — С. 50-55. — Бібліогр.: 43 назв. — англ. |
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Pylypenko, S. Motsyk, O. Kozak, L. 2017-06-10T13:11:44Z 2017-06-10T13:11:44Z 2016 Temperature changes over storms from measurements of spacecraft TIMED / S. Pylypenko, O. Motsyk, L. Kozak // Advances in Astronomy and Space Physics. — 2016. — Т. 6., вип. 1. — С. 50-55. — Бібліогр.: 43 назв. — англ. 2227-1481 DOI:10.17721/2227-1481.6.50-55 https://nasplib.isofts.kiev.ua/handle/123456789/119943 In the present work we have studied changes of mesospheric temperature over the powerful storms Wilma, Haitang, and Katrina using measurements of the space vehicle TIMED. We have found the temperature increasing at the altitude range 80-100 km. We have found the explanations for the obtained results by the dissipation of the gravity waves. Propagation of atmospheric gravity waves in a non-isothermal, windless atmosphere, with taking into account the viscosity and the thermal conductivity, has also been modelled in this work. We have determined that the maximum of amplitude of the atmospheric-gravity waves at the considered characteristics corresponds to altitudes of near 90 km (mesopause). It was found that the main factor influencing propagation and dissipation of the wave in such cases is the vertical temperature gradient. Viscosity and thermal conductivity have less influence on the wave amplitude. The work is done in the frame of complex program of NAS of Ukraine on space researches for 2012-1016, the grant Az. 90 312 from the Volkswagen Foundation ("VW-Stiftung") and within the framework of the educational program No.2201250 "Education, Training of students, PhD students, scientific and pedagogical staff abroad" launched by the Ministry of Education and Science of Ukraine. en Головна астрономічна обсерваторія НАН України Advances in Astronomy and Space Physics Temperature changes over storms from measurements of spacecraft TIMED Article published earlier |
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Temperature changes over storms from measurements of spacecraft TIMED |
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Temperature changes over storms from measurements of spacecraft TIMED Pylypenko, S. Motsyk, O. Kozak, L. |
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Temperature changes over storms from measurements of spacecraft TIMED |
| title_full |
Temperature changes over storms from measurements of spacecraft TIMED |
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Temperature changes over storms from measurements of spacecraft TIMED |
| title_full_unstemmed |
Temperature changes over storms from measurements of spacecraft TIMED |
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temperature changes over storms from measurements of spacecraft timed |
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Pylypenko, S. Motsyk, O. Kozak, L. |
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Pylypenko, S. Motsyk, O. Kozak, L. |
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2016 |
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English |
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Advances in Astronomy and Space Physics |
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Головна астрономічна обсерваторія НАН України |
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Article |
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In the present work we have studied changes of mesospheric temperature over the powerful storms Wilma, Haitang, and Katrina using measurements of the space vehicle TIMED. We have found the temperature increasing at the altitude range 80-100 km. We have found the explanations for the obtained results by the dissipation of the gravity waves. Propagation of atmospheric gravity waves in a non-isothermal, windless atmosphere, with taking into account the viscosity and the thermal conductivity, has also been modelled in this work. We have determined that the maximum of amplitude of the atmospheric-gravity waves at the considered characteristics corresponds to altitudes of near 90 km (mesopause). It was found that the main factor influencing propagation and dissipation of the wave in such cases is the vertical temperature gradient. Viscosity and thermal conductivity have less influence on the wave amplitude.
|
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2227-1481 |
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https://nasplib.isofts.kiev.ua/handle/123456789/119943 |
| citation_txt |
Temperature changes over storms from measurements of spacecraft TIMED / S. Pylypenko, O. Motsyk, L. Kozak // Advances in Astronomy and Space Physics. — 2016. — Т. 6., вип. 1. — С. 50-55. — Бібліогр.: 43 назв. — англ. |
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| first_indexed |
2025-11-26T00:10:46Z |
| last_indexed |
2025-11-26T00:10:46Z |
| _version_ |
1850595939174055936 |
| fulltext |
Temperature changes over storms from measurements
of spacecraft TIMED
S. Pylypenko1, O.Motsyk2, L.Kozak1∗
Advances in Astronomy and Space Physics, 6, 50-55 (2016) doi: 10.17721/2227-1481.6.50-55
© S. Pylypenko, O.Motsyk, L.Kozak, 2016
1Taras Shevchenko National University of Kyiv, Glushkova ave. 4, 03127, Kyiv, Ukraine
2Delft University of Technology, Mekelweg 2, 2628 CD Delft, the Netherlands
In the present work we have studied changes of mesospheric temperature over the powerful storms Wilma,
Haitang, and Katrina using measurements of the space vehicle TIMED. We have found the temperature increasing
at the altitude range 80�100 km. We have found the explanations for the obtained results by the dissipation of the
gravity waves. Propagation of atmospheric gravity waves in a non-isothermal, windless atmosphere, with taking
into account the viscosity and the thermal conductivity, has also been modelled in this work. We have determined
that the maximum of amplitude of the atmospheric-gravity waves at the considered characteristics corresponds to
altitudes of near 90 km (mesopause). It was found that the main factor in�uencing propagation and dissipation of
the wave in such cases is the vertical temperature gradient. Viscosity and thermal conductivity have less in�uence
on the wave amplitude.
Key words: pressure, density, and temperature; ionosphere-atmosphere interactions; wave propagation; middle
atmosphere dynamics; thermospheric dynamics; tropical meteorology
introduction
Nowadays there is much evidence of the existence
of atmospheric-gravity waves (AGW) in the neutral
Earth's atmosphere. Among the observed facts one
may discern: wave structures on the tropospheric
and noctilucent clouds; variations of the surface pres-
sure at microbarogrammes; wave variations of ozone
concentration and other impurities in the middle
atmosphere; wave structures obtained by the iono-
sphere's radiosounding method, etc. [16, 18, 20, 24].
There are tens of possible sources of AGW, among
which the most potent are: tropospheric cyclons
and frontal systems; solar terminator; hurricanes;
storms; nuclear tests; large-scale anthropogenic dis-
asters; earthquakes; volcanic eruptions; supersonic
rockets' �ight etc. [11, 29].
The spectrum of gravity waves in atmosphere is
very wide. They can have periods from a few min-
utes up to tens of hours [10, 27]. As the AGW prop-
agates upwards in the adiabatic regime, the AGW
amplitude increases as density decreases [15, 24, 42].
Meanwhile, as the altitude increases, the adiabatic
condition of the wave propagation breaks. Such an
e�ect mostly leads to the loss of durability of these
waves and to their dissipation.
Investigation of AGW at altitudes of 80�100 km
and identi�cation of the source of the AGW meets
a range of di�culties [13]. It is particularly di�-
cult studying this problem by ground-based imag-
ing techniques. Short horizontal wavelength AGWs
reach the airglow region a few hundred kilometres
from their source, which means that the ground-
based imagers must be placed close to the source
region. However, the periods of intensive convective
activity are also periods of considerable cloudiness,
which often precludes imaging observations. Then,
there is some evidence that the AGWs, which are
seen in imagers, may be ducted a considerable hor-
izontal distance from their source, making it dif-
�cult to determine the origin of these waves [40].
Finally, until recently, there were almost no space-
based instruments capable to make images of AGWs
above the troposphere. Nevertheless, there were sev-
eral studies attempting to determine speci�c AGW
sources. They could be separated into two classes:
those regarding AGWs which travel directly from
the convective source to the observation height, and
those regarding the ducting or trapping of AGWs.
There are only a few such reports of the �rst
former category. The �rst one was a ground-based
study by Taylor and Hapgood [37], which observed
curved wave fronts with a centre approximately 200
to 500 km from the observed wavefronts. They used
the estimates of the wind and temperature pro�les
from the limited satellite and model data available
∗
kozak@univ.kiev.ua
50
Advances in Astronomy and Space Physics S. Pylypenko, O.Motsyk, L.Kozak
for analysis. The horizontal wavelength was about
25 km, and the intrinsic period was found to be ap-
proximately 17min. From meteorological charts and
lightning data it was shown that there were transient
thunderstorms present in the studied region, which
were found to be the source of these AGWs.
Another study was based on space-based obser-
vations by Dewan et al. [4]. It used infrared data
collected by the Midcourse Space Experiment satel-
lite, originating at altitudes of 40 km which showed
circular wave-fronts with a horizontal wavelength of
approximately 25 km. The source of these waves was
also identi�ed as a thunderstorm.
The �nal study was by Sentman et al. [31], who
observed nearly concentric wavefronts emanating
from a tropospheric source region (thunderstorm).
In the second category, there were a number of
investigations that attempted to explain the preva-
lence of AGWs in airglow imagers with horizontal
wavelength values which are typically several tens of
kilometres, have ground-based periods of ten to sev-
eral tens of minutes, and are imaged a long distance
away from a speci�c convective source [5, 12, 13, 23,
26, 36, 38, 40]. Walterscheid et al. [40] presented
the idea that this was due to ducting of the AGWs
in a thermal duct present in the upper mesosphere
and lower thermosphere. Hecht et al. [13] later sug-
gested that modi�cations of this thermal duct by
winds must also be considered and the waves may
be trapped rather than purely ducted.
In [1, 13, 38, 41] the results obtained indicated
that the short-period, short-horizontal wavelength
AGWs are produced by convective activity. However,
these studies also indicate that AGWs with some-
what longer wavelengths (up to several hundred kilo-
metres) may also be produced. Furthermore, Wal-
terscheid et al. [41] suggest that acoustic waves with
periods of a few minutes may also be present in the
region above the storm.
In spite of a large number of works, so far there
is no clearance in understanding what mechanisms
and at which heights are involved in the wave atten-
uation.
observations
Echoes in the upper atmosphere on large-scale
weather formations can become apparent in temper-
ature variations, vector of wind speed, emissions, etc.
In the capacity of researching sources of atmo-
spheric disturbances, hurricanes were chosen. These
powerful vortex �ows of air masses arise above the
warm water basins of the ocean from the powerful
tropical cyclones, inside which the pressure is drop-
ping towards the centre. Meanwhile, the air �ows
move from the periphery to the cyclone's centre.
The rotating component of the wind speed inside
the cyclone is caused by the Coriolis force. Due to
the condensation of water vapour a large amount of
heat is extracted, which increases upstreams and re-
sults in turbulence. Although hurricanes form in the
lower atmosphere and expand only for approximately
twenty kilometres in height, they carry enough en-
ergy to considerably in�uence the structure of the
upper layers.
The e�ects of three hurricanes were stud-
ied, which occurred from July till October
2005. They are as follows: Katrina (23.08.2005�
31.08.2005), Wilma (15.10.2005�25.10.2005) and
Haitang (11.07.2005�19.07.2005). Hurricanes Kat-
rina and Wilma developed above the Atlantic Ocean,
Haitang above the Paci�c Ocean.
We analysed temperatures values above these
hurricanes measured by the satellite TIMED and
particularly by its device TIDI.
The results are presented in Fig. 1, the tempera-
tures are represented on a grey colour scale. Temper-
ature changes were analysed in the altitude range of
70�110 km prior to the appearance of the hurricane
(left column), during the most powerful stage of the
hurricane (middle column), and following its com-
plete dissipation (right column).
It can be seen from the �gures that the temper-
ature increases above the hurricane regions by 25�
40K at the mesopause level. Obtained temperature
changes cannot be explained by the features of solar
and geomagnetic activity.
numerical modelling
of propagation and damping
of the atmospheric gravity waves
Since AGW are considered to be a possible mech-
anism responsible for the energy transport from the
lower atmospheric layers upwards, we decided to per-
form a numerical modelling of AGW propagation
in the Earth atmosphere. Our method is based
mainly on the method of solution of the Navier-
Stokes equations, described in [6, 7]. It is similar
to the multi-layer methods, which were �rstly con-
sidered by Midgley and Liemohn [22]. AGW, while
propagating in an inhomogeneous atmosphere, can
dissipate its energy both by self-damping and by re-
distribution via various dissipative processes (viscos-
ity, thermal conductivity etc.). Calculations of Midg-
ley and Liemohn [22] are based on the assumption
that energy redistribution between gravity waves and
dissipative processes in the lower atmosphere is neg-
ligibly small, so that waves can be considered as
of gravity type only. The iterative scheme used in
this method is valid until dissipative processes dump
much faster than atmospheric-gravity waves. Vol-
land [39] showed that viscosity and thermal conduc-
tivity may be important at upper atmospheric levels.
He admits that the gravity-wave dominated solution
used for lower altitudes, will be gravity-wave domi-
nated at high altitudes also.
51
Advances in Astronomy and Space Physics S. Pylypenko, O.Motsyk, L.Kozak
Fig. 1: The distribution of temperature by time and height: before (a), during (b) and after (c) the hurricane
Katrina (August 2005); before (d), during (e) and after (f) the hurricane Wilma (October 2005); before (g),
during (h) and after (i) the hurricane Haitang (July 2005).
In this work we solve the Navier-Stokes equation
taking into account dissipative processes. We con-
sider a plane-parallel atmosphere consisting of homo-
geneous layers with constant temperature T0, mass
M , adiabatic constant γ, gravity g, viscosity to den-
sity ratio µ/ρ0 and thermal conductivity to density
ratio λ/ρ0. We linearize the system of equations rel-
ative to the unperturbed steady state of the atmo-
sphere:
ρ0
∂u′′i
∂t
= −∂p′′
∂xi
+ ρ′′gi+
+
∂
∂xi
[
µ
(
∂u′′i
∂xj
+
∂u′′j
∂xi
− 2
3
δij∇ · u′′
)]
,
∂ρ′′
∂t
+∇ · (ρ0u′′) = 0,
ρ0Ra
(γ − 1)M
∂T ′′
∂t
= ∇ · (λ∇T ′′)− ρ0∇ · u′′,
(1)
where u′′, p′′, ρ′′ denote a 1st-order perturbation of
velocity, pressure, and density, caused by the prop-
agation of the wave, Ra is universal gas constant,
p′′ =
ρ′′RaT0
M
+
ρ0RaT
′′
M
.
We search the solution in a plane mode:
p′′
Ap
=
T ′′
AT
=
u′z
Az
=
=
u′x
Ax
∝ exp
(
iωt− ikxx− ikzz +
z
2H
)
. (2)
Ap, AT , Az and Ax are scaling factors. The hori-
zontal wave vector kx and the real frequency ω are
assumed to be constant throughout the atmosphere,
since the atmosphere depends neither on spatial co-
ordinate x nor on time t. On the other hand, verti-
cal wave vector kz varies through the di�erent atmo-
spheric layers.
52
Advances in Astronomy and Space Physics S. Pylypenko, O.Motsyk, L.Kozak
Substituting a plain mode solution (2) into the (1)
we turn the system of di�erential equations into a
system of algebraic equations. We join the solutions
for waves in di�erent adjacent layers by assuming
continuity for vertical velocity and moment �ux. For
a certain ω and a horizontal wave number kx, the
scale parameters Az, Ax, Ap, and AT are de�ned by
the following formula:
Az =
ω
kx
[
(1 + η)k − 2iηα+
k − iα
(γ − 1)−1 − νR
]
−
− ω
kx
[
1 + η − β + 3ηR+
1
(γ − 1)−1 − νR
]
, (3)
Ax =
ω
kx
[
(1 + η)k − iα(1 + 3η) +
k
(γ − 1)−1 − νR
]
−
− ω
kx
[
(1 + 4η)R− η − β − 1 +
R− 1
(γ − 1)−1 − νR
]
, (4)
AT =
T0kx
ω
[
Ax + kAz
(γ − 1)−1 − νR
]
, (5)
Ap =
p0kx
ω
[Ax +Az (k − iα)] + p0
AT
T0
. (6)
where the dimensionless parameters are: k = (kz +
i/2H)/kx, R = k2 − iαk + 1, α = 1/kxH, β =
ω2/gk2xH, η = iωµ/3p0, ν = iλT0k
2
x/ωp0.
If the values u′x, u′z, p′′ and T ′′ are valid for
Eq. (2), then they are valid for the Navier-Stokes
equations.
In the course of numerical modelling while us-
ing Eqs. (2)�(6) we have calculated the amplitudes
of velocity disturbances (both vertical u′′z and hor-
izontal components u′′x), pressure p′′, and altitu-
dinal measurements of temperature T ′′ caused by
the motion of AGW with a period of 65 minutes
and horizontal component of the wave vector kx =
10−5m−1 [11, 19]. At the period and kx changing
the scales of processes are also changing, however,
the regularity of changes of atmosphere parameters
in the case of AGW is still the same. For the analysis
of the investigated parameters the initial conditions
(temperature pro�les, concentrations of all compo-
nents, altitude of uniform atmosphere) were calcu-
lated using the model of MSIS [14] for the days of
maximal intensities of considered storms. The pres-
ence of experimental data with temperature mea-
surements above storms allowed us to use the value
30 K as the maximal increase of temperature as a
result of the wave presence (border conditions).
In the course of the analysis we considered an at-
mosphere that has no wind, is non-isothermal, and
is strati�cated in terms of density and concentration
of main components, while taking into account vis-
cosity and heat-conductivity.
The results of numerical modelling of the change
with the altitude of vertical and horizontal compo-
nents of AGW velocity, pressure, and temperature,
as a result of waves passing, are shown in Figures 2�
5. We should note that the disturbances of tempera-
ture and pressure as a result of AGW spreading are
put onto the usual view of changes of pressure and
temperature with the altitude.
It can be seen that for the chosen set of the mod-
elling parameters, the waves propagate to heights of
approximately 120 km and reach a maximum ampli-
tude in the range of 90 to 100 km.
discussion and conclusion
Analysing the changes of the upper atmosphere
temperature over hurricanes we found that the lo-
cal temperature increases to some marked extent at
the mesopause heights. We modelled propagation
of atmospheric gravity waves in a windless, non-
isothermal atmosphere with a strati�cation of den-
sity and main components, but while taking into ac-
count viscosity and thermal conductivity. Our main
conclusions are:
� An AGW has its maximum amplitude at the
mesopause level.
� The altitude at which the waves reach max-
imum amplitude depends essentially on the
height temperature gradient in that area.
� The waves begin to dampen from altitudes 100
km above sea level.
� Wave amplitude depends mainly on viscosity
and thermal conductivity. Dependence of the
dissipation height on these parameters is much
lower.
� Propagation of AGWs disturbs the mesopause
so that the vertical component of the velocity
changes by approximately 1�2m/s, the hori-
zontal component�by 6�10m/s, and the pres-
sure � by 60�100mPa, while the temperature
changes by 15�30K.
The obtained results are found to be in good agree-
ment with works of numerical modelling of amplitude
values of temperature variations from orographic
waves at altitudes of 80�90 km over mountain [9], and
temperature disturbances from a tsunami (increasing
by 10�12K [35], wave periods are ∼ 30min [2]), and
also are in good correspondence by order of magni-
tude to experimental estimations [1, 13, 32, 33, 34,
38, 41].
In addition, the results of this work agree with
the results of previous studies [19, 20, 29].
Note that nowadays there are researches in which
the existence of the inverse connection is discussed,
i. e. when the AGWs starting their spread from au-
roral ionosphere regions have an in�uence onto ex-
tratropical cyclones [28].
53
Advances in Astronomy and Space Physics S. Pylypenko, O.Motsyk, L.Kozak
Fig. 2: Vertical AGW velocity dependence on height
(solid line for July 18, 2005, dotted line for August 28,
2005, dashed line for October 19, 2005).
Fig. 3: Horizontal AGW velocity dependence on height
(solid line for July 18, 2005, dotted line for August 28,
2005, dashed line for October 19, 2005).
Fig. 4: Pressure variations due to propagating wave (solid
line for July 18, 2005, dotted line for August 28, 2005,
dashed line for October 19, 2005).
Fig. 5: Temperature variations due to propagating wave
(solid line for July 18, 2005, dotted line for August 28,
2005, dashed line for October 19, 2005).
At that it is suggested that the solar-wind-
generated auroral AGWs contribute to processes that
release instabilities and initiate slantwise convection
thus leading to cloud bands and growth of extrat-
ropical cyclones. Also, if the AGWs are ducted to
low latitudes, they could a�ect the development of
tropical cyclones. The gravity-wave-induced vertical
lift may modulate the slantwise convection by releas-
ing the moist symmetric instability at near-threshold
conditions in the warm frontal zone of extratropical
cyclones. In this case the Joule heating or Lorentz
forcing is responsible for auroral AGWs generation.
As an evidence that the e�ect is observed from
AGWs coming from the cyclone but not spreading
from above could serve the fact that the e�ect to be
observed at height of 90�100 km. We did not detect
any signi�cant deviations from the background value
over 110 km. At the same time according to works
Luhman [21] and Cole [3] gravity waves launched
by the auroral electrojet generally do not cause sig-
ni�cant perturbation of the wind �elds in the mid-
dle atmosphere. However, at altitudes 110�120 km,
upward and downward vertical winds in excess of
30m/s have been observed at high latitudes during
moderately-disturbed geomagnetic conditions [25].
Rees et al. [30] identi�ed sources at high latitudes of
strong vertical winds of more than 100m/s, resulting
from local geomagnetic energy input and subsequent
generation of thermospheric gravity waves.
As was mentioned in introduction the stability
of AGWs is breaking with increasing altitude, and
they dissipate. The dissipation of wave energy at
mesopause altitudes causes heat �ows comparable
with solar ones [8]. As a result the turbulent layers
appear in atmosphere, which are generally observed
in regions with highly de�ected pro�les of the tem-
54
Advances in Astronomy and Space Physics S. Pylypenko, O.Motsyk, L.Kozak
perature and wind velocity [19]. In troposphere the
life time of such layers is longer, and they can ex-
ist for long time after �turning o�� wave source of
the turbulence [17]. These turbulized regions can,
in turn, be sources of AGWs (secondary AGW) that
propagate from the regions of primary wave dissipa-
tion. The possible generation of secondary gravity
waves during wave front breaking and wave decay at
mesopause altitudes is considered in [43].
acknowledgments
The work is done in the frame of complex pro-
gram of NAS of Ukraine on space researches for
2012�1016, the grant Az. 90 312 from the Volkswagen
Foundation (�VW-Stiftung�) and within the frame-
work of the educational program No.2201250 �Edu-
cation, Training of students, PhD students, scienti�c
and pedagogical sta� abroad� launched by the Min-
istry of Education and Science of Ukraine.
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