Zonal winds in the stratosphere and mesosphere play
important roles in atmospheric dynamics and aeronomy. However, the
direct measurement of winds in this height range is difficult. We present a
dataset of the monthly mean zonal wind in the height range of 18–100 km and
at latitudes of 50∘ S–50∘ N from 2002 to 2019,
derived by the gradient balance wind theory and the temperature and pressure
observed by the SABER instrument. The tide alias above 80 km at the Equator
is replaced by the monthly mean zonal wind measured by a meteor radar at
0.2∘ S. The dataset (named BU) is validated by comparing with
the zonal wind from MERRA2 (MerU), UARP (UraU), the HWM14 empirical model
(HwmU), meteor radar (MetU), and lidar (LidU) at seven stations from around
50∘ N to 29.7∘ S. At 18–70 km, BU and MerU have (i)
nearly identical zero wind lines and (ii) year-to-year variations of the
eastward and westward wind jets at middle and high latitudes, and (iii) the
quasi-biennial oscillation (QBO) and semi-annual oscillation (SAO)
especially the disrupted QBO in early 2016. The comparisons among BU, UraU,
and HwmU show good agreement in general below 80 km. Above 80 km, the
agreements among BU, UraU, HwmU, MetU, and LidU are good in general, except
some discrepancies at limited heights and months. The BU data are archived
as netCDF files and are available at 10.12176/01.99.00574 (Liu et al., 2021). The advantages
of the global BU dataset are its large vertical extent (from the
stratosphere to the lower thermosphere) and 18-year internally
consistent time series (2002–2019). The BU data is useful to study the
temporal variations with periods ranging from seasons to decades at
50∘ S–50∘ N. It can also be used as the background wind
for atmospheric wave propagation.
Introduction
Zonal mean zonal wind in the middle and upper atmosphere is critical to the
propagation and dissipation (via filtering or prohibiting) of atmospheric waves
(e.g., gravity waves, tides, and planetary waves) while the waves propagate
against or along the zonal winds (Forbes, 1995; Fritts and Alexander, 2003).
On the other hand, the waves dissipate their energy and momentum in the mean
flow and accelerate or decelerate the mean wind. This changes the
atmospheric thermal and wind structures and even reverses the wind direction
(McLandress, 1998; Zhang and Shepherd, 2005; Watanabe and Miyahara, 2009;
Liu et al., 2014; Becker and Vadas, 2018). Thus, the zonal wind climatology
and the mean wind–wave interactions are important topics in atmosphere
dynamics.
Ground-based observations (e.g., using radiosondes, rockets, Fabry–Pérot
interferometers, radars, and lidars) have a long history of use for wind
measurement. They provide horizontal winds in a limited altitude range
and/or location but have wide and even full local time (LT) coverage. On
the other hand, satellite observations provide global observations of winds
in the middle and upper atmosphere in limited LT or height ranges. For
example, the High Resolution Doppler Imager (HRDI) on the Upper Atmosphere
Research Satellite (UARS) observed winds of 10–40 and 65–110 km
during the daytime from 1991 to 1999 (Hays et al., 1993). The Wind Imaging
Interferometer (WINDII) on the UARS observed winds of 90–120 km during
both day and night from 1991 to 1997 (Zhang and Shepherd, 2005;
Shepherd et al., 2012). Onboard the Thermosphere, Ionosphere, Mesosphere
Energetics and Dynamics (TIMED) satellite, the TIMED Doppler Interferometer
(TIDI) has observed wind of 70–115 km during the day and 80–105 km at night
since 2002 (Killeen et al., 2006). The TIDI wind data are mainly used to
study tides and planetary waves due to the uncertainties in absolute
zero wind (Niciejewski et al., 2006; Wu et al., 2006, 2008; Gu et al., 2013).
On 10 September 2019, NASA's Ionospheric Connection Explorer (ICON)
was launched to study the Earth's ionosphere (Immel et al., 2018). The
Michelson Interferometer for Global High-Resolution Thermospheric Imaging
(MIGHTI) onboard the ICON satellite has two identical sensor units, MIGHTI-A
and MIGHTI-B, which can be used to retrieve temperature at 90–115 km and
line-of-sight winds and the vector winds at 90–300 km (Englert et al., 2017;
Harding et al., 2017; Stevens et al., 2018). These ground-based and
satellite observations and rocket soundings are useful to construct
empirical wind models, such as the COSPAR International Reference Atmosphere
(CIRA-86) (Fleming et al., 1990), the Horizontal Wind Model (HWM) (Drob et
al., 2008, 2015; Emmert et al., 2008), and the Upper Atmosphere Research
Satellite (UARS) Reference Atmosphere Project (URAP) wind climatology
(Swinbank and Ortland, 2003).
These observations are useful to constrain the reanalysis wind data, such as
the Modern-Era Retrospective analysis for Research and Applications, version
2 (MERRA2) (Molod et al., 2015; Gelaro et al., 2017), and the European
Centre for Medium-Range Weather Forecasts ERA5 (Hoffmann et al., 2019;
Hersbach et al., 2020). A recent study by Ern et al. (2021) showed that both
MERRA2 and ERA5 capture the semi-annual oscillation (SAO) in the
stratopause and the lower mesosphere around the Equator. In the middle
mesosphere, MERRA2 produces a reasonable SAO due to the assimilated Aura
Microwave Limb Sounder (MLS) data (Schwartz et al., 2008; Molod et al.,
2015). Above 70 km, the mesopause SAO produced by ERA5 is stronger than that
of MERRA2. This is because the stronger damping of MERRA2 reduces the
amplitude of the mesopause SAO. These observations and models greatly
improve our knowledge of the winds in the middle and upper atmosphere.
The zonal winds provided by CIRA-86 and UARP are important in global
climatology and are found at 0–120 and 0–110 km, respectively (Fleming et al.,
1990; Swinbank and Ortland, 2003). The zonal and meridional winds provided
by the HWM series are a function of day of the year and LT and range from the surface to the
thermosphere (∼ 500 km) (Drob et al., 2008, 2015; Emmert et
al., 2008). The zonal winds from these models are useful to study the
seasonal variations but not for variations with periods longer than 1
year. The zonal winds provided by reanalysis data (e.g., MERRA2 and ERA5) are in a height range from the surface to ∼ 70–80 km and
are useful to study variations with periods from several days to several
years (Gelaro et al., 2017; Hoffmann et al., 2019; Ern et al., 2021).
At present, direct global measurement of zonal wind in the
upper stratosphere and mesosphere is difficult, and the model-inherent
damping in the upper model levels of MERRA2 and ERA5 is still a challenge for
retrieving realistic wind in the mesosphere and lower thermosphere (MLT) region
(Ern et al., 2021). A candidate is now combining the observations of temperature
and pressure with balance wind theory to retrieve zonal wind in the MLT region:
Smith et al. (2017) have derived the balance wind (BU) at the
Equator based on the gradient wind balance theory (Randel, 1987)
and observation data. The observation data are (1) the geopotential height
observed by the MLS (Schwartz et al., 2008) from 2004 to 2016 and (2) the
pressure and temperature measured by the Sounding of the Atmosphere Using
Broadband Emission Radiometry (SABER) instrument (Russell et al., 1999) on
the TIMED satellite from 2002 to 2015. They showed the SAO of zonal wind and
its relation with the quasi-biennial oscillation (QBO) in the tropical upper
stratosphere and mesosphere. Smith et al. (2017) noted that the BU is
reasonable below ∼ 84 km but not above ∼ 84 km.
This is because the aliasing of diurnal tide to mean wind is notable above
84 km (McLandress et al., 2006; Xu et al., 2009). The reason for the tidal
alias is ascribed to the diurnal tide being prominent and exhibiting short-term
(single-day to several-day) variations. The full diurnal cycle is composed of the
data from many days (e.g., 60 d for SABER observations). Thus, the
obtained values are the mean of diurnal tides over these days. However, the
short-term variations of diurnal tides are still in the background and alias
the derived winds based on the gradient wind balance theory.
The focus of this work is to provide a global dataset of the monthly mean
zonal wind (short for BU dataset) at 18–100 km based on the
gradient wind balance theory and the temperature and pressure measured by
the SABER instrument. The BU dataset extends from 2002 to 2019 and from
50∘ S to 50∘ N. To overcome the unrealistic BU above 84 km over the Equator (Smith et al., 2017), we replace the BU above 80 km with
the zonal wind measured by the meteor radar at Kototabang (0.20∘ S, 100.32∘ E). The validation of the BU dataset will be performed
by comparing it with those from MERRA2, UARP, HWM, and meteor radar and lidar
observations from around 50∘ N to 29.7∘ S.
The advantages of the global BU dataset are (1) its large vertical extent
(from the stratosphere to the lower thermosphere) and (2) 18-year
internally consistent time series (2002 to 2019). Thus, the BU dataset can
be used to study the global variations of zonal wind at timescales ranging
from seasons to decades and from the stratosphere to the lower thermosphere.
These variations include SAO (Semi-Annual Oscillation), AO (Annual Oscillation), QBO, and ENSO (El Niño–Southern
Oscillation, i.e., periods of 2–8 years, Baldwin and O'Sullivan, 1995). Although
QBO and ENSO originate from the lower atmosphere or sea surface, their
influence is global and can extend to the stratosphere or to even higher
heights and latitudes (Baldwin and O'Sullivan, 1995; Baldwin et al., 2001).
Moreover, the interactions among SAO, AO, QBO, and ENSO are also important in
modulating global atmospheric waves and composition from the stratosphere to
the lower thermosphere (e.g., Xu et al., 2009; Liu et al., 2017; Diallo et
al., 2018; Ern et al., 2011, 2014, 2021; Kawatani et al., 2020).
Data and methodData description
MERRA2 is the new version of atmospheric reanalysis dataset developed by
NASA's Global Modeling and Assimilation Office (Molod et al., 2015; Gelaro
et al., 2017). We use the 72-level (∼ 0–75 km) assimilated
meteorological fields, which have time, longitude, and latitude intervals of
3 h, 0.625∘, and 0.5∘, respectively. The MERRA2
zonal winds are interpolated to uniform vertical grids from 2 to 72 km
with a step of 1 km. Then they are averaged in a latitude band of
5∘ with an overlap of 2.5∘ in each month such that the
monthly zonal mean (MerU) wind can be obtained and will be used to validate
the BU at 50∘ N–50∘ S.
The URAP zonal wind (UraU) is based on the winds observed by the HRDI
instrument, the stratospheric assimilation data from the Met Office, and the
gradient wind balance calculated from URAP temperature data from April 1992
to March 1993 (Swinbank and Ortland, 2003). The UraU mainly represents the
period of 1992–1993 and can be used as a reference wind dataset in the
climatology sense. The UraU covers from 1000 hPa
(∼z=0 km) to 4.6 × 10-5 hPa (∼z=110 km) and from 80∘ S to 80∘ N with equal
intervals of 4∘ (Swinbank and Ortland, 2003).
HWM14 is the latest version of HWM, which provides the global zonal and
meridional winds from the surface to thermosphere (∼ 500 km)
and their variations with LT and day of year (Drob et al., 2015). After
setting the longitude to be 0 and changing the time from 0:00 to 23:00 LT each day,
we get the hourly zonal winds from 18 to 100 km with a step of 1 km and from
50∘ S to 50∘ N with a latitude interval of
2.5∘. Following this, the daily mean zonal wind is calculated by averaging the
hourly zonal winds over 1 d. Finally, we change the day numbers from 1 to
365 to get the monthly mean zonal winds, which is referred to be the HWM14
zonal wind (HwmU). We note that the monthly mean zonal wind does not depend
on longitude since the stationary planetary waves and migrating tides
reproduced by HWM14 can be removed on a timescale of 1 month (Drob et
al., 2015).
The zonal winds measured by meteor radar and lidar are used to improve the
BU over the Equator and to validate BU at middle and high latitudes. The
radars' locations and their data periods are listed in Table 1. The
meteor radar measure the zonal and meridional winds at 80–100 km with
a vertical interval of 2 km and a temporal interval of 1 h. The zonal
winds measured by these meteor radar are averaged over each calendar month
to get the monthly zonal wind (MetU). The MetU spans from 53.5∘ N
to 29.7∘ S and is useful to compare the BU at 80–100 km and in
both the Northern Hemisphere (NH) and Southern Hemisphere (SH). The MetU
at Koto Tabang (KT, 0.20∘ S) can be used to replace the tidal aliased BU over
the Equator (McLandress et al., 2006; Xu et al., 2009; Smith et al., 2017).
As they are affected by the weather conditions, the zonal winds measured by the Colorado State University (CSU)
lidar (LidU) from 2002 to 2008 are rearranged in a composite year according
to calendar month in 80–100 km with a vertical interval of 0.5 km. The LidU
is compared with the BU in the climatology sense. A detailed
description of the meteor radar and lidar, as well as their measurement
uncertainties, can be found in the references listed in Table 1.
Locations of radar and lidar and their data periods.
InstrumentStationLocationPeriodReferencesMeteor radarMohe (MH)53.5∘ N, 122.3∘ E2011–2019Li et al. (2012), Xiong et al. (2013), Yu et al. (2013, 2015)Meteor radarBeijing (BJ)40.3∘ N, 116.2∘ E2009–2019Meteor radarSanya (SY)18.3∘ N, 109.6∘ E2011–2016Meteor radarKoto Tabang (KT)0.2∘ S, 100.3∘ E2002–2017Batubara et al. (2011), Rao et al. (2011, 2012), Hayashi et al. (2013), Abe et al. (2014), Matsumoto et al. (2016)Meteor radarBiak (BK)1.2∘ S, 136.1∘ E2011–2015Meteor radarCachoeira Paulista (CP)22.7∘ S, 45.0∘ W2004–2008Batista et al. (2004), Andrioli et al. (2009, 2013, 2015)Meteor radarSanta Maria (SM)29.7∘ S, 53.8∘ W2005–2008Na (sodium) lidarColorado State University (CSU)40.6∘ N, 105.1∘ W2002–2008She (2004), Yuan et al. (2008)
The BU is derived from the temperature and pressure profiles (level 2A,
version 2.07) measured by the SABER instrument (Russell et al., 1999) from
2002 to 2019. These profiles cover ∼ 15–110 km and latitudes
of 53∘ S–83∘ N or 83∘ S–53∘ N. The
temperature accuracy is 1–3 K from 30 to 80 km and 5–10 K from 90 to 100 km
(Remsberg et al., 2008). The detailed procedure for deriving BU is described
in the next subsection.
Method of deriving balanced wind
Deriving BU is performed using the following two steps. The first
step is to derive the zonal mean temperature and pressure. All the original
profiles measured by the SABER instrument are interpolated linearly to
18–108 km with a vertical interval of 1 km. Following this, these profiles are sorted
into latitude bands that have width of 5∘ with an overlap of
2.5∘ and extend from 50∘ S to 50∘ N. At each
latitude band (φ) and height (z), the temperature can be
expressed as TtUT,λ (λ is
longitude). Then the zonal mean temperature in each universal time (UT) day,
TZMUTtZMLT, for the ascending and descending nodes,
respectively, can be expressed as follows:
TZMUTtZMLT,z,φ=12π∫02πTtUT,λ,z,φdλ,tZMLTz,φ=12π∫02πtLTλ,z,φdλ.
Thus, TZMUTtZMLT,z,φ
excludes the nonmigrating tides and stationary planetary waves but contains
the zonal mean temperature in an LT day (TZMLTtZMLT,z,φ, short for T¯z,φ) and migrating tides (Xu et al., 2007, 2014; Gan et al., 2014). It
takes about 60 d to get a nearly complete LT coverage for the SABER
measurements. Thus, TZMLTtZMLT,z,φ and migrating tides can be calculated by the least-squares fitting
TZMUTtZMLT,z,φ in a time
window of 60 d and forward 1 d. Here both the ascending and descending
data are used for the fitting. The fitting function is expressed as follows:
TZMUTtZMLT,z,φ=T¯z,φ+Ancosnω0tZMLT-tn..
Here, ω0=2π/24h,
n=1,2,3,4 is the frequency (in d-1) of migrating
tides. An and tn are the amplitude and phase, respectively, of the migrating
tides with frequency of n. T¯z,φ is
the zonal mean temperature in an LT day. In the same way, the zonal mean
pressure p¯z,φ can be obtained.
The second step is to calculate the BU from T¯ and p¯. The
zonal mean of the momentum equation in the zonal direction is used to
calculate the gradient balance wind (Randel, 1987; Fleming et al., 1990; Xu
et al., 2009),
u¯2atanφ+fu¯=-1aρ¯∂p¯∂φ.
Here, f=2Ωsinφ is the Coriolis factor,
Ω=2π/24×60×60 is
the Earth rotation frequency (rad s-1), and a is the
radius of the Earth. u¯ and ρ¯=p¯/RT¯ are the BU and zonal mean density,
respectively. R is the gas constant for dry air. Equation (3) has been
successfully applied to the latitude bands of 70–8∘ S
and 8–70∘ N to get zonal mean wind (Fleming et al.,
1990; Smith et al., 2017). We restrict Eq. (3) at 10–50∘ N and 10–50∘ S due to the
noncontinuous sampling of the SABER measurements poleward of 53∘ N/S. At the Equator, the solution of Eq. (3) is an indeterminate form
of 0/0 as φ→0 and can be solved through
L'Hôpital's rule if we get continuous values of p¯ and ρ¯. In fact, only the discrete values p¯ and ρ¯ with a
latitude interval of 2.5∘ can be obtained from observations. To
apply Eq. (3) at the Equator, one needs to differentiate Eq. (3) with
φ. As φ→0, we have tanφ→φ, sinφ→φ. Thus, Eq. (3) can be
simplified as follows (Fleming et al., 1990):
u¯2a+2Ωu¯=-1aρ¯∂2p¯∂φ2.
According to Fleming et al. (1990) and Smith et al. (2017), the monthly mean
zonal mean wind is mainly in the range of ±75 m s-1. Thus, the
term u¯2/a is 1 to 2 orders of magnitude smaller than
2Ωu¯ and can be neglected. Thus, u¯ at the
Equator can be expressed as follows (Fleming et al., 1990; Swinbank and Ortland,
2003):
u¯=-12Ωaρ¯∂2p¯∂φ2.
Here the BU below 80 km is obtained from Eq. (5). Due to the alias of
diurnal tide to the BU above 84 km at the Equator (McLandress et al., 2006;
Xu et al., 2009; Smith et al., 2017), the BU in 80–100 km calculated by Eq. (5) will be replaced by the MetU at KT (0.20∘ S). Consequently,
the reconstructed BU should be reliable throughout the height ranges from 18
to 100 km. The replaced BU will be described in the next subsection.
At 2.5–7.5∘ N and 2.5–7.5∘ S,
the BU is estimated by a cubic spline interpolation of the BU at
10–50∘ N, 10–50∘ S and the
reconstructed BU at the Equator (Smith et al., 2017).
Modification of equatorial balance wind by the wind measured by meteor
radar at Koto Tabang
The MetU measured at KT (0.20∘ S) provides a unique advantage to
modify the BU at the Equator such that one can get reliable BU up to 100 km. Figure 1 shows the daily mean (black) and monthly mean (red) zonal wind at
86 km measured by the meteor radar at KT station. We can see that the wind
data are continuous from November 2002 to September 2017 except during some
months in 2013 and 2014. To match the SABER measurements from 2002 to 2019,
we have to get a continuous dataset from 2002 to 2019 through filling the
missing data in 2013 and 2014 and extending the data backward to February
2002 and forward to December 2019.
The daily mean (black dots) and monthly mean (red line with dots) zonal winds (positive for eastward) at 86 km measured by the KT (Koto Tabang) meteor radar and their regression results (blue line with dots) from 2002 to 2019. The ticks on the x axis mark the beginning of each year.
The continuous dataset is constructed by multiple linear regression (MLR,
chap. 6 of Kutner et al., 2005) through the following three steps: (i) separating the data into four segments (A: 2002–2007; B: 2006–2011; C:
2010–2015; D: 2014–2019) with an overlap of 24 months. The separation seems
arbitrary but includes continuous observation in segment B, which is
regarded as a reference segment and used as a predictor variable in MLR.
Moreover, the separation retains just as many observations in the other
three segments to improve the confidence level of MLR. The overlap of 24
months is to cover the missing observations from October 2017 to December 2019. (ii) Following this, the predictor variables of MLR are constructed. The first predictor
variable is the constant of 1. Its regression coefficient represents the
mean wind of each segment. The second predictor variable is the wind data in
segment B. Figure 1 shows that the temporal variations of winds in segments A,
C, and D are similar to that in the segment B but have slightly different
oscillation amplitudes. After inspecting each segment, we see that the
prominent oscillations have periods of 12 and 6 months, which are used as
the third and fourth predictor variables. To reproduce more realistic
regression, we also include oscillations of periods of 36, 24, 4, and 3
months as the fifth to eighth predictor variables. The predictor variables
can be summarized as a constant of 1; the wind data in segment B; and
oscillations with periods of 36, 24, 12, 6, 4, and 3 months. (iii) Using the
predictor variables mentioned in step (ii), we perform MLR on segments A,
C, and D. Following this, the missing observations are filled with MLR
predictions (shown as a blue line with dots in Fig. 1).
To quantify the rationality of the MLR method, we used R2 score, which
is the ratio of the variations in the observation data explained by the
model and defined as follows:
R2=1-∑i=1Nyi-fi2/∑i=1Nyi-y¯2,y¯=1N∑i=1Nyi.
Here, yi and fi are the observation data and model results with
data numbers of N, respectively. The best R2 score is 1, where the
predicted values are the same as the observation data. For segments A, C,
and D, their R2 scores are 0.63, 0.59, and 0.65, respectively, and
their available observation months are 60, 57, and 34, respectively. It
should be noted that the R2 scores increase with the increasing number
of predictor variables. However, the increasing number of predictor
variables reduces the robustness of the model when the available observation
months are short (e.g., segment C). Thus, the predictor variables chosen
here are an optimal compromise between the R2 score and the robustness
of the MLR model. Figure 1 shows that the MLR fittings coincide well with the
observed monthly mean zonal winds when observations were available. It is
reasonable to expect that the MLR predictions in the time intervals of
missing observations are reliable (e.g., 2013, 2014, before November 2002,
and after September 2017) and can be used to construct BU.
After applying the MLR on the zonal wind measured by the KT meteor radar at
80–100 km, we obtain a continuous dataset of MetU. This continuous dataset
is composed of the observed data when they were available and predicted
values when the observed data were missing. This continuous dataset is
used to replace the BU calculated by Eq. (5) at 80–100 km. Combined
with the BU calculated by Eq. (5) at 18–80 km and the MetU measured by the
KT meteor radar at 80–100 km, we can get a reconstructed BU at 18–100 km.
Figure 2 shows the BU at 18–100 km calculated by Eq. (5) at the Equator (Fig. 2a)
and the reconstructed BU (Fig. 2b and c). We note that the reconstructed BU is
smoothed by three-point running mean in height and time, respectively. Figure 2
shows that the BU above 80 km (Fig. 2a) is in the eastward direction during most
months, which is the opposite of the replaced BU (Fig. 2b and c). This is because
the BU above 80 km shown in Fig. 2a is aliased by the diurnal tide over
the Equator (McLandress et al., 2006; Xu et al., 2009; Smith et al., 2017).
The BU (color filled contour, positive for eastward) calculated by Eq. (4) at the Equator at 18–100 km (a: 2002–2019) and the reconstructed BU (b: 2002–2010; c: 2011–2019). The over-plotting contour lines show MerU (interval of 15 m s-1; the eastward and westward winds are represented as solid and dashed lines, respectively). The white rectangles highlight the fast westward jet during the beginning of the QBO westward phase. The red and thick black contour lines are the zero winds of BU of MerU, respectively. The solid and dashed red rectangles show the disrupted QBO in 2016. The ticks on the x axis mark the beginning of each year.
Validations of the balance wind
To validate the BU derived from the SABER observations and modified by
meteor radar wind observations near the Equator, we will compare the BU with
(i) monthly mean zonal winds from MERRA2 data (MerU), (ii) the UARP wind
(UarU) and the zonal wind calculated from HWM14, and (iii) the zonal winds
observed by meteor radars (MetU) at latitudes of 29.7∘ S–53.5∘ N and an Na lidar (LidU) at 40.6∘ N.
Comparisons with the wind from MERRA2
First of all, we should note that the BU data are derived from the
temperature and pressure profiles measured by the SABER instrument and the
zonal wind observed by a meteor at Koto Tabang (0.20∘ S). None of
these data are assimilated in MERRA2. Thus, BU and MerU are
independent. Figure 2b and c, and Fig. 3, and Fig. 4 compare the BU derived from
SABER observations and the monthly mean zonal winds from MERRA2 data (MerU)
at the Equator, the midlatitudes (30∘ N/S) and at high latitudes (50∘ N/S), respectively. To perform a more quantitative comparison, in Fig. 5 we show
the wind differences between BU and MerU and their standard
deviations and percentage differences. The wind difference (Δuim) at each height (i) and month (m) is calculated here by subtracting
the wind of other datasets (uimot) from the BU (uimbu). At
each height the percentage difference (Pi) is defined as the ratio of
the standard derivations (σi) of Δuim to the peak BU.
Time–height sections of the BU (color-filled contour, positive for eastward) and MerU (lines with contour interval of 20 m s-1, the eastward and westward winds are represented as solid and dashed lines, respectively) at 30∘ S (a, b) and 30∘ N (c, d). The red and thick black contour lines are the zero winds of BU of MerU, respectively. Different color scales are used at 30∘ S and 30∘ N. The ticks on the x axis mark the beginning of each year.
The same as Fig. 3 but at 50∘ S (a, b) and 50∘ N (c, d).
At the Equator (Fig. 2b and c), the agreements of BU and MerU are good at
least below ∼ 55 km and can be described as follows. (i) At
∼ 40–55 km, the SAO is dominant in both BU and MerU and has
nearly identical amplitudes and phases, as well as zero wind lines. (ii) At
∼ 35–40 km, both SAO and QBO can be seen in BU and MerU. (iii) At ∼ 20–35 km, the QBO is dominant in both BU and MerU and
has nearly identical zero wind lines. (iv) Both BU and MerU reproduce the
disrupted QBO in 2016; i.e., a westward jet (highlighted by a solid red
rectangle) formed within the eastward phase of QBO at 18–23 km. Meanwhile
the eastward wind shifts to a higher height (above 23 km) (Newman et al.,
2016; Osprey et al., 2016; Diallo et al., 2018). Subsequently, the westward
wind (highlighted by a red dashed rectangle) occurred in the eastward phase
of QBO at ∼ 30–35 km during late 2016. (v) At ∼ 40–50 km, the fast westward jet (shown as white rectangles) seems to be an
extension of the westward phase of QBO to a higher height just after the QBO
changes its phase from eastward to westward. This feature can also be seen
in Fig. 6 of Smith et al. (2017), which showed the BU derived from the SABER
observations. The wind differences shown in Fig. 5a exhibit that BU is
more westward (eastward) than MerU below ∼ 30 km during the
period of QBO westward (eastward) phase. At ∼ 30–55 km, BU is
more westward than MerU with peak differences of ∼ 20 m s-1. Above ∼ 55 km, the BU is more eastward than MerU
with peak differences of ∼ 60 m s-1. A possible reason for
the less eastward MerU is the strong damping of MERRA2 (Ern et al., 2021).
The standard deviations of the wind differences (left column of Fig. 5a) are
less than 7 m s-1 below ∼ 40 km and is about 10 m s-1
above ∼ 42 km. The large percentage differences (middle column
of Fig. 5a) with magnitudes of ∼ 30 %–40 % occur at around 20 and 43 km. In the other height ranges, the percentage differences are
∼ 20 %.
The wind differences between BU and MerU (right column) and their standard deviations (σ, left column) and percentage differences (P, middle column) at the Equator (a), 30∘ N/S (b, c), and 50∘ N/S (d, e). The black contour lines are the zero wind difference.
At 30∘ N/S (Fig. 3), the excellent agreements between BU and MerU
can be summarized as the following three points. (i) At 30∘ S
(Fig. 3a and b), the eastward jets are asymmetrical around June with peaks at
a lower (higher) height during early (late) summer of most years. (ii) At
30∘ N (Fig. 3c and d), the eastward jets of both BU and MerU
have two relatively weak peaks below ∼ 60 km, and with the
increasing height the two peaks merge into one strong peak above
∼ 70 km during the winter of most years. (iii) Both BU and MerU have
nearly identical patterns of zero wind lines and westward wind jets. The more
quantitative comparisons shown in Fig. 5b and c show that the wind
differences generally exhibit asymmetric AO, except for the short-term
variations with periods of several months. The asymmetry means that the
eastward phase of AO in the wind differences lasts a longer time than the
westward phase. Comparisons between Figs. 5b and 3 show that the AO in
wind difference is generally in phase with that in the zonal wind. This
indicates that the BU is more eastward (westward) than MerU when the wind
phase is eastward (westward). Compared to the wind differences before August
2004, the wind differences are smaller above ∼ 60 km. This
might be a consequence of the improved quality of MERRA2 after assimilating
the MLS data (Molod et al., 2015; Gelaro et al., 2017). The standard
deviations of the wind differences (left column of Fig. 5b and c) vary from
∼ 3 to ∼ 8 m s-1 with increasing
heights. The percentage difference is ∼ 10 % in the entire
height range, except for ∼ 35 % at 21 km and 30∘ S.
At 50∘ N/S (Fig. 4), the eastward jets of both BU and MerU are
stronger at 50∘ S than those at 50∘ N below
∼ 70 km. Moreover, the westward jets of both BU and MerU reach
their peaks at higher heights than those of the eastward jets. At
50∘ S, the BU and MerU agree well with each other and can be
described using the following four aspects: (i) the nearly identical patterns
of zero wind lines, (ii) the fastest (slowest) eastward winds during 2006
(2010), (iii) the nearly identical times (around July) and heights
(∼ 50 km) of the eastward wind jets, and (iv) the nearly identical
times (around January) and heights (∼ 70 km) of the westward
wind jets. At 50∘ N, the good agreements between BU and MerU
exhibit the four aspects mentioned above. Moreover, the double-peak
structure can be seen in both BU and MerU during winter of some years (e.g.,
2003, 2004, 2006, 2008, 2009, 2012, 2013, 2015, 2019). These double-peak
structures caused by the sudden stratospheric warming (SSW), which reduces
eastward wind during minor SSW or even reverses the eastward wind to westward
during major SSW (Butler et al., 2015, 2017). From Fig. 5d and e, we
see that the wind differences exhibit asymmetric AO. Here the asymmetries
mean that the time interval of the eastward and westward phases are
different in each hemisphere, and they are also different between
50∘ N and 50∘ S. At 50∘ S, the westward
(eastward) phase lasts a longer time than the eastward (westward) phase
below (above) ∼ 60 km. In contrast, the eastward phase lasts a
longer time than the eastward phase at 50∘ N. The standard
deviations of the wind differences (left column of Fig. 5d and e) vary
from ∼ 3 to ∼ 12 m s-1 with the
increasing height. The percentage difference is in the range of 10 %–17 %
except for ∼ 20 % at 38 km and 50∘ N.
The above comparisons show that BU and MerU agree well with each other. At
the Equator and below 55 km, BU and MerU have nearly identical zero wind
lines and reproduce the QBO and SAO. Both BU and MerU reproduce the fast
westward jet during the beginning of the QBO westward phase and the
disrupted QBO in early 2016. At middle and high latitudes, BU and MerU have
nearly identical zero wind lines in the height range of 20–70 km and
reproduce the year-to-year variations of the latitude and height-dependent
eastward and westward jets. Both BU and MerU reproduce the double-peak
structures induced by SSW in the NH.
Comparisons with the winds from UARP and HWM14 in a composite year
To compare the UraU with BU, the UraU is interpolated to geometric height
with a vertical interval of 1 km and a latitude interval of 2.5∘.
Moreover, the BU is rearranged in a composite year, which is calculated by
averaging the BU in the same calendar month of the years from 2002 to 2019.
Figure 6 shows the latitude–height sections of BU and UraU and their
differences in each month of the composite year. It shows that zero wind
lines of BU and UraU are nearly identical below ∼ 85 km from
50∘ S to 50∘ N. During winter (November, December,
January, February) in the NH and summer (May, June, July, August) in the SH,
the eastward jet shifts from high to low latitudes with the increasing
height. During summer in the NH and winter in the SH, the westward jet
shifts from low to high latitudes with the increasing height. During spring
(March, April) and autumn (September, October), the westward winds, which
occur at low and middle latitudes and below ∼ 45 km or above
∼ 70 km, are separated by eastward winds at ∼ 45–70 km. These comparisons show the good agreement between BU and UraU
below ∼ 80 km.
Latitude–height sections of BU (color-filled contour, positive for eastward) and UraU (contour lines with interval of 10 m s-1, the eastward and westward winds are represented as solid and dashed lines, respectively) in each month (denoted in the upper-left corner of each panel) of a composite year. The thick black and red contour lines are the zero wind of UraU and BU, respectively. The same color scale is used for all months.
Above 80 km and at middle to high latitudes, both BU and UraU exhibit
similar eastward jets during winter in the SH and during summer in the NH.
During summer in the SH and winter in the NH, both BU and UraU exhibit
decreasing eastward wind with the increasing height and even reverse to
westward near 100 km. This is different from the MetU at MH (53.5∘ N) and BJ (40.3∘ N) (red lines in Fig. 8), in which the westward
winds occur only around March and April. The comparisons among the BU, MetU
and UraU will be shown in the next subsection.
The same as Fig. 5 but for the BU and HWM14. The thick black and red contour lines are the zero wind of HwmU and BU, respectively.
Monthly mean zonal wind from meteor radars (red lines, positive for eastward) at (from left to right) MH (53.5∘ N), BJ (40.3∘ N), SY (18.3∘ N), BK (1.2∘ S), CP (22.7∘ S), and SM (29.7∘ S) stations and the BU (black) at a similar latitude (labeled at the top of each column) at five heights. The correlation coefficient (cc) between BU and MetU is labeled on each panel. The same y axis is used in each row. The ticks on the x axis mark the beginning of each year.
At the Equator and above 80 km, both BU and UraU exhibit westward
winds but have different height and latitudinal coverages. At
∼ 90 km, the UraU is eastward throughout the composite year
except during February–April. However, the BU is eastward only during June
and December and westward during other months. By analyzing the zonal winds
measured by the medium frequency (MF) radars at Christmas Island
(2∘ N, 157∘ W), Tirunelveli (8.7∘ N,
77.8∘ E), and Pameungpeuk (7.4∘ S, 107.4∘ E)
and meteor radar at Koto Tabang (0.20∘ S, 100.3∘ E) and
Jakarta (6∘ S, 107∘ E), Rao et al. (2012) showed that
the composite zonal winds are westward except around June, July, and December.
This supports the BU derived here. Comparing between the BU calculated from
Eq. (4) (Fig. 2a) and the reconstructed BU (Fig. 2b and c) above 80 km, we
find that the BU calculated from Eq. (4) is eastward in general. While the
reconstructed BU is largely westward and coincides with the radar
observation results of Rao et al. (2012). Thus, the reliability of the BU
around the Equator above 80 km is improved greatly after we combine the BU
derived from the SABER observations and MetU measured by the meteor radar at
KT (0.20∘ S).
Although BU and UraU exhibit general consistency in climatologic sense,
there are still some differences between them. The wind differences between
BU and UraU (the second and fourth rows of Fig. 6) reach eastward maxima of
30 m s-1 around the Equator and at ∼ 70–80 km during
March–April and October–December. There are also westward differences with
peaks larger than 15 m s-1 at ∼ 50 km and the Equator
during January–April. The westward peaks of -30 m s-1 occur at around
30∘ N/S and at ∼ 85–95 km during February–May and
August–October. There are also westward differences, which extend downward
from ∼ 100 to ∼ 50 km in the SH during
November–January and in the NH during June–July. To summarize the
wind differences, the eastward (westward) differences occur around
the Equator (30∘ N/S).
Now, we compare the BU and HwmU. In a same manner as Fig. 6, we show in Fig. 7 the HwmU and BU in a composite year. Below ∼ 85 km the
eastward jets of BU and HwmU agree well during winter in the NH and during
summer in the SH. Meanwhile, the westward jets of HwmU and BU agree well
during summer in the NH and during winter in the SH. During spring and
autumn and at low and middle latitudes, the westward winds below
∼ 45 km or above ∼ 70 km surround the eastward
winds at ∼ 45–70 km. These comparisons show the good agreement
between BU and HwmU below ∼ 80 km.
Around the Equator and at ∼ 90 km, the eastward HwmU occurs
during May–July and November–December, which lasts a shorter time interval
than that of the UraU. At ∼ 20–40∘ N, above the
peaks of the eastward jets (at ∼ 70 km), there are weak
eastward jets in UraU (HwmU) during September–November (September–December)
at 80–90 km with a peak at ∼ 85 km. However, this peak is not as
obvious as in BU or in the MetU at BJ (40.3∘ N) and SY
(18.3∘ N) or in the LidU at CSU (40.6∘ N) shown in the
next subsection.
The differences between BU and HwmU should be mentioned (the second and
fourth rows of Fig. 7). Among the composite years, the eastward differences
with peaks of ∼ 45 m s-1 occur at ∼ 60–80 km
during May–August in the SH. This is different from the wind differences
between BU and UraU, in which the eastward differences reach their peaks
around the Equator. The westward differences with peaks of ∼-30 m s-1 occur at heights of ∼ 30–50 km and latitudes of
30–50∘ N (30–50∘ S) during winter in the NH (SH).
Moreover, the westward differences with peaks of ∼-30 m s-1 occur at ∼ 55–75 km and latitudes of
30–50∘ S (30–50∘ N) during winter in the SH (NH). Above
∼ 80 km, the wind differences are westward in general
throughout the composite year. This is comparable to the wind
difference between BU and UraU.
Comparisons with the time series of winds measured by meter radars
Figure 8 shows the monthly mean zonal wind from meteor radars (MetU) and the
BU at similar latitudes and five height levels. At MH (53.5∘ N)
station, the variations of BU agree well with MetU with correlation
coefficients (CCs) of 0.89–0.98. Moreover, BU and MetU exhibit similar AO
and SAO above 90 km and similar AO below 86 km. The eastward peak of AO in
both BU and MetU shift from below 86 km in winter to above 92 km in summer.
From 2011 to 2019 and above 86 km, both BU and MetU show that the eastward
wind is dominant in almost of all months except March and April, during
which the MetU reversed from eastward to westward. Here we note that the BU
at 50∘ N, which represents the latitude range of 47.5–52.5∘ N, is near the location of MH (53.5∘ N) station.
The slight difference in latitude might contribute some discrepancies
between the BU and MetU at MH (53.5∘ N) station.
At BJ (40.3∘ N) station, the variations of BU agree with MetU with
CCs of 0.85–0.95. The AO and SAO of BU and MetU at BJ vary with height. Both
BU and MetU show that the eastward peaks of AO shift from winter below 82 km
to summer above 90 km. This is a similar situation to that at MH station.
At 86 km, the AO and SAO are almost equally portioned for the MetU with peaks
in both summer and winter, while the AO is dominant with eastward peaks in
winter. From 2009 to 2019 and above 86 km, both BU and MetU show that the
eastward wind is dominant except for some occasional periods.
At SY (18.3∘ N) station, the CCs between BU and MetU are in the
range of 0.78–0.9. However, the temporal variations of BU do not coincide
well with that of MetU since the BU (MetU) is dominated by both AO and SAO
(AO) above 86 km. Only at 82 km do the temporal variations of BU and MetU
agree well with each other. Moreover, at 82, 86, and 90 km, in addition to the
AO and SAO, the QBO signal (with westward peaks in the beginning of 2011 and
2013) appears in both BU and MetU.
At BK (1.2∘ S) station, the BU and MetU agree well with each other
and have CCs of more than 0.88 below 86 km. The smaller CCs above 90 km are
mainly caused by the inconsistency of weak temporal variations in BU and
MetU. It should be noted that the magnitudes of BU agree well with those of
MetU above 90 km. Moreover, both BU and MetU exhibit similar AO and SAO from
82 to 98 km (except at 94 km).
At CP (22.7∘ S) station, the CCs between BU and MetU are in the
range of 0.78–0.96. The temporal variations of BU and MetU agree well below
90 km. At 94 and 98 km, although the BU and MetU have CCs of 0.9 and 0.96,
they are dominated by the SAO and AO, respectively. At SM (29.7∘ S)
station, the CCs between BU and MetU are in the range of 0.82–0.95. The
temporal variations of BU and MetU agree well with each other (except at 86 and 90 km). At 82, 94, and 98 km, both BU and MetU are dominated by AO,
while the AO in MetU has a larger amplitude than that of BU.
A summary of the comparisons between the time series of BU and MetU
is given below. At MH (53.5∘ N), BJ (40.3∘ N), BK
(1.2∘ S), and SM (29.7∘ S) stations, the agreements
between BU and MetU are good in general. The agreements are better at 82,
94, and 98 km than those at 86 and 90 km. At SY (18.3∘ N)
station, the agreement between BU and MetU is only good at 82 km. At CP
(22.7∘ S) station, the agreement between BU and MetU is good only
below 90 km.
Comparisons with the Winds measured by meteor radar and lidar in a
composite year
To compare BU, UraU, HwmU, and MetU above 80 km in terms of climatology,
we show their monthly mean values and their differences in a composite year
in Fig. 9. At 50∘ N and MH station (the first row of Fig. 9), the
winds of the four datasets exhibit AO and agree well with each other below
85 km. The exception is that the BU and MetU are more westward than UraU and
HwmU in summer and are less eastward than UraU and HwmU in winter. Above 86 km, the agreement is also good except that (i) the westward wind in MetU
during April does not occur in BU, UraU, and HwmU; (ii) the westward wind in
UraU during December does not occur in BU, HwmU, and MetU; and (iii) the SAO in BU
and MetU cannot be seen in UraU and HwmU. The eastward differences of BU–MH
with peaks larger than 15 m s-1 occur above ∼ 85 km and
during April–June. In contrast, the eastward differences of larger than 15 m s-1 last for a longer time interval for UraU–MetU and HwmU–MetU. Moreover,
the westward differences are also larger in UraU–MH and HwmU–MH than those
in BU–MH.
Monthly mean zonal winds of BU, UraU, HwmU, and MetU (from the first to fourth column) and their differences (from the fifth to seventh column) at (from up to below) MH (53.5∘ N), BJ (40.3∘ N), SY (18.3∘ N), BK (1.2∘ S), CP (22.7∘ S), and SM (29.7∘ S) stations in a composite year. The red contour lines show the zero wind in each panel. The black contour lines (interval of 10 m s-1) show the zonal wind measured by the CSU lidar (LidU). The wind difference is represented by color-filled contour and highlighted by contour lines.
At 40∘ N and BJ and CSU stations (the second row of Fig. 9), the
BU exhibits AO and shifts its eastward peak from below ∼ 90 km
in winter to above ∼ 90 km in summer. In contrast, the AOs in
MetU and LidU shift their eastward peaks from below ∼ 85 km in
winter to above ∼ 85 km in summer. The difference between MetU
and LidU is that the westward LidU shift from ∼ 80 km in June
to ∼ 100 km in March, while the westward MetU occurs only
below ∼ 85 km. The weak eastward BU and MetU extend upward
from ∼ 85 km in April and October to ∼ 100 km in
January and December. This is different from those of UraU and HwmU: (i) the
eastward wind peaks of both UraU and HwmU are stronger than those of BU,
MetU, and LidU, and (ii) the weak eastward peaks at ∼ 90 km in March
and September do not appear in either BU or MetU or LidU. Thus, the BU at
40∘ N agrees with MetU and LidU better than with UraU and
HwmU. The westward differences of BU–BJ with peaks less than -15 m s-1
occur below ∼ 88 km and during May–July. In contrast, the
differences of UraU–BJ and HwmU–BJ are eastward with peak values of greater
than 15 m s-1, which are larger than those of BU–BJ. The westward
differences of BU–BJ and eastward differences of UraU–BJ and HwmU–BJ are
responsible for the westward differences of BU–UraU and BU–HwmU at latitudes
higher than 30∘ N (Figs. 6 and 7). When comparing the
differences of BU–BJ, UraU–BJ, and HwmU–BJ, the magnitudes of the differences
of BU–BJ are the smallest, although they vary with month and height.
At 18.75∘ N and SY station (the third row of Fig. 9), the westward
BU at ∼ 80 km in March–May shifts upward to ∼ 100 km in January–April. This agrees with MetU, except that the westward
MetU lasts for a shorter time interval. However, this is different from those of
UraU and HwmU, which experience eastward wind at ∼ 87–95 km.
The westward BU at ∼ 80 km in August shifts upward to
∼ 100 km in October. In contrast, this westward BU does not
occur in either UraU, HwmU, or MetU. The eastward wind peaks during summer at
∼ 80–100 km can be seen in the four datasets. The height
range and duration of westward differences of BU–SY are larger and longer
than those of UraU–SY and HwmU–SY. The peak value of the westward
differences of BU–SY is more negative than -15 m s-1. This contrasts
with the eastward difference of 15 m s-1 for UraU–SY and HwmU–SY.
At 1.25∘ S and BK station (the fourth row of Fig. 9), the
agreement between BU and MetU is excellent for the aspects of both seasonal
and height variations. This is mainly because the BU is reconstructed by the
MetU at the KT station, which is at 0.20∘ S and is very close to
BK station (1.18∘ S). The UraU and HwmU exhibit similar SAO with
eastward peaks during summer and winter. These eastward peaks are much
stronger than those of BU and MetU, especially below ∼ 92 km.
In contrast, above ∼ 92 km the UraU and HwmU are more
westward than those of BU and BK. This is different from the results of Rao
et al. (2012), who showed that the UraU was less westward than the MetU at
KT station (0.20∘ S). A possible reason is that the 3-month
running mean is performed here to construct a smooth BU at the Equator and
reduce the peak magnitudes of zonal winds. The differences of BU–BK are
smaller than those of UraU–BK and HwmU–BK. This might be due to the inclusion of
the zonal wind measured at KT station (0.20∘ S) when we construct
BU at the Equator. In contrast, the differences of UraU–BK and HwmU–BK reach
their peak values of larger than 15 m s-1 in summer and winter.
At 22.5∘ S and CP station (the fifth row of Fig. 9), the agreement
between BU and MetU is good below ∼ 92 km. Both of them
exhibit (i) SAO with eastward peaks in summer and winter and (ii) westward
winds during September–October shifting backward with height. However,
this westward wind cannot be seen in either UraU or HwmU. Above
∼ 92 km, the agreement among the four datasets is good during
January–March and October–December. During May–September, the eastward wind
in BU cannot be seen in the other three datasets. This might be symmetrical to
results at 18.75∘ N, where the eastward wind in BU during
November–December cannot be seen in the other three datasets. The
differences of BU–CP are eastward with peak of more negative than -15 m s-1 in summer and westward in winter with peak of larger than 15 m s-1. In contrast, the differences of UraU–CP are eastward with peak of
larger than 15 m s-1 below ∼ 92 km and westward above
∼ 92 km. Among the four datasets, the differences of HwmU–CP
are smallest in general. A possible reason is that the winds measured by medium-frequency radar at similar latitudes (Bribie Island at 28∘ S) have
been included in the HWM14 model (Drob et al., 2008).
At 30.0∘ S and SM station (the sixth row of Fig. 9), the agreement
between BU and MetU is good in general. An exception is that the BU is less
eastward than the other three datasets during March–June at 82–95 km. Both
BU and MetU exhibit much weaker eastward winds than UraU and HwmU during
September–November at ∼ 82–95 km. During May–September and
above ∼ 92 km, the eastward wind in BU cannot be seen in the
other three datasets. However, the eastward wind in BU is weaker and extends
over a shorter time interval compared to that at 22.5∘ S. Moreover,
the eastward wind in BU is closer to the MetU than those of UraU and HwmU.
The differences of BU–SM are mainly westward with a peak that is more negative than
-15 m s-1 during April. In contrast, the differences of UraU–SM are
eastward with peaks of larger than 15 m s-1 at ∼ 82–92 km throughout the composite year. Although the HWM14 model included the winds
measured by the medium frequency radar at Adelaide (34.5∘ S) and
Bribie Island at (28∘ S), there are still eastward differences with
peaks of larger than 15 m s-1 during June and September.
A short summary of the comparisons among BU, UraU, HwmU, LidU, and MetU in
the composite year is given below. The BU agrees with MetU and LidU better than
UraU and HwmU at 50∘ N, 40∘ N, 1.25∘ S, and
30∘ S. At 18.75∘ N and 22.5∘ S, the agreement
between BU and MetU is better than that among UraU, HwmU, and MetU during
spring and summer since the westward winds in BU and MetU cannot be seen in
UraU or HwmU. However, the agreement between BU and MetU is worse than that
among UraU, HwmU, and MetU since the westward BU cannot be seen in the other
three datasets in autumn. The agreement between BU and MetU at
1.25∘ S indicates that the reconstructed BU is a feasible way to
get reliable zonal wind at the Equator above ∼ 80 km. The
agreement between BU and MetU at 50∘ N, 40∘ N, and
30∘ S indicates that the reliability of balance wind theory can be
extend up to the height of 100 km. The weaker agreement between BU and MetU at
18.75∘ N and 22.5∘ S indicates that the tidal aliasing
to the mean wind might not be neglected at these latitudes.
Data availability
The SABER data are downloaded from
https://spdf.gsfc.nasa.gov/pub/data/timed/saber/ (last access:
March 2020, SABER team, 2020). The UARP wind data were obtained from
ftp://sparc-ftp1.ceda.ac.uk/sparc/ref_clim/randel/temp_wind (last access: March 2020, Swinbank and Ortland, 2003). The MERRA2
data were obtained from were obtained from http://disc.sci.gsfc.nasa.gov/mdisc (last access: March 2020, Molod et al., 2015 and Gelaro et al., 2017). The meteor
radar data of MH, BJ, and SY were supported by the Chinese Meridian Project
(Wang, 2010) and provided by Beijing National Observatory of Space
Environment, Institute of Geology and Geophysics Chinese Academy of Sciences
through the Geophysics center, National Earth System Science Data Center
(http://wdc.geophys.ac.cn, last access: March 2020, Yu et al., 2015). The meteor radar data
of KT and BK were provided by the Research Institute for Sustainable
Humanosphere, Kyoto University
(http://database.rish.kyoto-u.ac.jp/arch/iugonet, last access: March 2020, Hayashi et al., 2013).
The database has been arranged by the Inter-university Upper atmosphere
Global Observation NETwork (IUGONET) project (Hayashi et al., 2013). The
meteor radar data at CP and SM are available upon request to Paulo Prado
Batista. The CSU lidar data are available upon request to Tao Yuan. The BU
data developed in this work are available at 10.12176/01.99.00574 (Liu et al., 2021).
Conclusions
Using the temperature and pressure observations by the SABER instrument over
the past 18 years (2002–2019) and the balance wind theory, we derive the
monthly zonal mean zonal wind (BU) at 18–100 km and at 10–50∘ N, 10–50∘ S, and at the Equator.
The BU at the Equator and above 80 km is replaced by the zonal wind measured
by the meteor radar at KT station (0.20∘ S). Therefore, the
reconstructed BU overcomes tide aliasing at 80–100 km. Following this, cubic
interpolation is applied to get BU at 7.5∘ S–7.5∘ N.
The BU is compared with the zonal winds from MERRA2 reanalysis data (MerU),
UARP data (UraU), the HWM14 empirical model (HwmU), and meteor radar
observations (MetU) at MH (53.5∘ N), BJ
(40.3∘ N), SY (18.3∘ N), BK (1.2∘ S), CP
(22.7∘ S), and SM (29.7∘ S) stations and the lidar observations (LidU)
at CSU (40.6∘ N). The main conclusions can be summarized as
follows.
The comparisons between BU and MerU show good consistency. At middle and
high latitudes, BU and MerU have nearly identical zero wind lines in 18–70 km and year-to-year variations in the eastward and westward wind jets due to the
double-peak structures caused by SSW. At the Equator and below 55 km, BU and
MerU have nearly identical zero wind lines and reproduce the QBO and SAO,
especially the disrupted QBO in early 2016.
The comparisons among BU, UraU, and HwmU show good agreement in general below
80 km. They have nearly identical zero wind lines and reproduce the eastward
(westward) jet in the winter (summer) hemisphere. Above 80 km, the good
agreement among BU, UraU, and HwmU is at the high latitudes.
The comparisons among BU, UraU, HwmU, MetU, and LidU show that the BU agrees
with MetU and LidU better than UraU and HwmU at 50∘ N,
40∘ N, 1.25∘ S, and 30∘ S on the aspects of
both their time series and composite year. At 18.75∘ N and
22.5∘ S, the time series of BU agrees with those of MetU only at
82 km and below 90 km, respectively. In a composite year, the BU agrees with
MetU better than UraU and HwmU in spring and summer.
Based on the comparisons, we conclude that the BU derived here is reliable
at 18–100 km and from 50∘ S to 50∘ N in general. The BU
derived here covers a time span of 18 years and can be used to study the
seasonal and interannual variations (e.g., SAO, AO, QBO, ENSO)
and their global interactions from the stratosphere to the lower
thermosphere. It can also serve as the background for wave propagations (e.g., gravity
waves, tides, and planetary waves) and global interactions from
the stratosphere to the lower thermosphere. The BU data have been archived
as netCDF files and are available at National Space Science Data Center
through 10.12176/01.99.00574 (Liu et al., 2021).
Author contributions
XL and JX designed the study and
wrote the manuscript. JY contributed to the discussion of the results and
the preparation of the manuscript. All authors discussed the results and
commented on the manuscript at all stages.
Competing interests
The contact author has declared that neither they nor their co-authors have any competing interests.
Disclaimer
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Financial support
This work was supported by the National
Natural Science Foundation of China (41831073, 41874182, 42174196), the
Natural Science Foundation of Henan (212300410011), the Open Research
Project of Large Research Infrastructures of CAS “Study on the interaction
between low/mid-latitude atmosphere and ionosphere based on the Chinese
Meridian Project” and “the Project of Stable Support for Youth Team in
Basic Research Field, CAS (YSBR-018)”. This work was also supported in part
by the Specialized Research Fund and the Open Research Program of the State
Key Laboratory of Space Weather.
Review statement
This paper was edited by Martin Schultz and reviewed by two anonymous referees.
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