The ongoing Swarm satellite mission provides an opportunity for better
knowledge of the near-Earth electromagnetic environment. Herein, we use a new
methodological approach for the detection and classification of ultra
low-frequency (ULF) wave events observed by Swarm based on an existing
time-frequency analysis (TFA) tool and utilizing a state-of-the-art high-resolution magnetic field model and Swarm
Level 2 products (i.e., field-aligned currents – FACs – and the Ionospheric
Bubble Index – IBI). We present maps of the dependence of ULF wave power
with magnetic latitude and magnetic local time (MLT) as
well as geographic latitude and longitude from the three satellites at their
different locations in low-Earth orbit (LEO) for a period spanning 2 years
after the constellation's final configuration. We show that the inclusion of
the Swarm single-spacecraft FAC product in our analysis eliminates all the
wave activity at high altitudes, which is physically unrealistic. Moreover,
we derive a Swarm orbit-by-orbit Pc3 wave (20–100 MHz) index for the
topside ionosphere and compare its values with the corresponding variations
of solar wind variables and geomagnetic activity indices. This is the first
attempt, to our knowledge, to derive a ULF wave index from LEO satellite
data. The technique can be potentially used to define a new Level 2 product
from the mission, the Swarm ULF wave index, which would be suitable for space
weather applications.
Space plasma physics (waves and instabilities)Introduction
Swarm is the fourth Earth Explorer mission of the European Space
Agency (ESA), launched on 23 November 2013. The mission measures the
geomagnetic field by identifying and measuring magnetic signals from the
Earth's core, mantle, crust, oceans, ionosphere, and magnetosphere
(Friis-Christensen et al., 2006). Additionally, Swarm data are used to study
the Sun's influence on the Earth system by analyzing electric currents in the magnetosphere and ionosphere and
understanding the impact of solar wind on the dynamics of the upper
atmosphere. Swarm currently offers one of the best-ever surveys of the
Earth's main and crustal magnetic field (Civet et al., 2015; De Michelis et
al., 2015; Hulot et al., 2015; Olsen et al., 2015; Schnepf et al., 2015) as
well as the near-Earth electromagnetic environment (Alken et al., 2015;
Archer et al., 2015; Buchert et al., 2015; Dunlop et al., 2015; Goodwin et
al., 2015; Iyemori et al., 2015; Lühr et al., 2015a, b; Park et al.,
2015; Pitout et al., 2015; Spicher et al., 2015). The interested reader is
also referred to the special issue “Swarm science results after 2 years in
space” (for details, see Olsen et al., 2016). The final constellation of the
three-satellite mission with two spacecraft (Swarm A and C) flying side by
side at low altitude (∼ 460 km) and one (Swarm B) flying at a slightly
higher altitude (∼ 510 km) was achieved on 17 April 2014.
Magnetospheric ultra low-frequency (ULF) waves in the topside ionosphere are
typically transmitted from magnetospheric and upstream solar wind sources.
Just as is the case for ULF waves observed on the ground, the amplitude of
the waves in the topside ionosphere is significantly smaller than that of the
background magnetic field. Observations in the topside ionosphere therefore
require magnetometers that are both extremely sensitive (< 1 nT) and have
a large dynamic range (±60 000 nT). ULF wave observations in the
ionosphere were first reported in the late 80s during the MAGSAT era (Iyemori
and Hayashi, 1989) when data from the mission were used to detect Pc1 waves
(with frequency f≃ 0.2–5 Hz). A number of magnetic and electric
field missions flying in a low-Earth orbit (LEO), like CHAMP, Ørsted,
SAC-C, or ST5, have enabled us to study in situ the occurrence of ULF waves
in the topside ionosphere. In particular, ULF wave monitoring from LEO
satellites has been most prominently reported in the Pc3 frequency range
(f≃ 20–100 MHz) (e.g., Jadhav et al., 2001; Vellante et al.,
2004; Heilig et al., 2007, 2013; Ndiitwani and Sutcliffe, 2009; Le et al.,
2011; Balasis et al., 2012, 2015a; Chi and Le, 2015; Yagova et al., 2015),
while for Pc1 waves (e.g., Engebretson et al., 2008; Park et al., 2013a) and
Pi2 waves (f≃ 2–25 MHz) (e.g., Sutcliffe and Lühr, 2003)
there have been fewer studies.
The CHAMP satellite has been one of the most successful missions for the
study of the Earth's magnetic field, with high-sensitivity and accuracy
magnetometer measurements orbiting within an altitude range of 450–300 km
for more than a decade (July 2000–September 2010). For the first time
long-term statistical studies on the occurrence of compressional Pc3 waves in
the topside ionosphere were possible (Heilig et al., 2007). Recently, new
features of Pc3 wave power in the topside ionosphere were revealed by Swarm
observations based on 1 year of mission data (Balasis et al., 2015b).
Moreover, Heilig and Sutcliffe (2016) used Swarm data to investigate the
distribution of wave coherence and phase difference as functions of magnetic
latitude and local time.
A satellite flying in a polar, low-Earth orbit is a suitable platform for
observing ionospheric instabilities in the F-region like the post-sunset
equatorial spread-F (ESF) events (Stolle et al., 2006). These instabilities
are generally accompanied by local depletions of the electron density.
In this study, we present a new technique that combines a wavelet spectral
analysis technique (Balasis et al., 2013), a state-of-the-art high-resolution
magnetic field model (Finlay et al., 2016), and Swarm Level 2 products (i.e.,
field-aligned currents – FAC – and the Ionospheric Bubble Index – IBI) in
order to study the occurrence and distribution of compressional Pc3 waves in
the topside ionosphere based on Swarm observations for a time period spanning
2 years. We derive orbit-by-orbit (i.e., ∼ 1.5 h) variations of the
Pc3 wave power, thus leading to the calculation of the Swarm ULF wave index
for the topside ionosphere, and compare them to variation of the geomagnetic
activity indices and solar wind parameters from the same time interval.
The rest of the paper is structured as follows: in Sect. 2 we describe the
processing related to Swarm data and the analysis technique used for
monitoring ULF waves with LEO satellites. Section 3 presents our results on
Pc3 wave occurrence mapping and the corresponding Pc3 power index for the
three Swarm satellites. In Sect. 4 we conclude with a discussion.
Data processing and analysis technique
LEO observations of ULF waves can only be reliably done and without too much
spatial aliasing for the Pc1/Pi1 and Pc2/3 waves. Due to the fast motion
through field lines in a LEO orbit, lower-frequency Pc4–5 waves (1–10 MHz)
cannot be accurately determined by LEO satellites, their period being longer
than the spacecraft transition time through the wave region. Though Pi2 waves
have lower frequencies, thanks to their large spatial scales at low
latitudes, they have also been detected by LEO satellites (Sutcliffe and
Lühr, 2003; Han et al., 2004; Cuturrufo et al., 2015). Two types of Pc3
waves are observed by LEO satellites: intense localized Alfvén-type waves
with transverse magnetic disturbance or weak global compression-type waves
recorded in the field-aligned component. In this study, we analyze the
magnitude of the magnetic field, thus considering the second type of wave.
In particular, we use the low-resolution magnetic field data with a sampling
rate of 1 Hz, and hence we had to limit our analysis to the Pc3 class,
covering frequencies from 20 MHz (50 s) to 100 MHz (10 s). An
electromagnetic wave of higher frequency, e.g., at 200 MHz, would be
captured in the low-resolution data by a pulsation with a period of merely 5
data points, making the analysis statistically dubious.
Our method consists of two parts. The first is the construction of a database
of daily power spectra, while the second consists of the actual wave
detection. For the construction of the database we used the last available
version of magnetic data from the vector fluxgate magnetometer (VFM)
instrument (version 4.8 for Swarm A and B and versions 4.9 and 4.10 for Swarm
C) as well as additional data from the electric field instrument – EFI
(version 4). To further enhance our analysis, we also incorporated data from
the daily Level 2 products concerning the FAC and IBI (version 2 for both).
For details on the definition and derivation of these products, see Park et
al. (2013b) and Ritter et al. (2013), respectively.
For every day in the time interval of interest, which spanned the time period
from 15 May 2014 to 15 May 2016, we perform the following analysis. First,
the magnetic data cdf files corresponding to the day in question are read,
along with the files of the previous and next days. Since all spectral
methods are plagued by edge effects (Torrence and Compo, 1998), we append the
magnetic field time series of the current day, with a few hours long time
series from the previous and next days, so that whatever edge effects appear
they will affect these additional “margins”, which can then be safely
removed from the process, leaving the spectral data of the day under
processing free from such issues. From the magnetic time series of the VFM
instrument we derive the magnitude of the magnetic field and subtract from it
the total field that is predicted, for the same position and moment in time,
by the CHAOS-6 model (Finlay et al., 2016). CHAOS-6 is a geomagnetic field
model spanning 1999–2016.5, derived from Swarm, CHAMP, Ørsted, and SAC-C
satellite magnetic data and ground observatory data. The model uses spatial
differences along-track from CHAMP and Swarm and also east–west differences
from Swarm (Kotsiaros et al., 2014). To the derived field time series we then
apply a Chebyshev type II, zero-phase, high-pass filter with a cutoff
frequency of 20 MHz to remove all lower-frequency components from the signal
and to place the Pc3 range in the spotlight (Williams and Taylors, 1988).
A series of studies highlighted the significance of applying wavelet
analysis, especially its suitability for multi-point, small-scale
disturbances, in the investigation of ULF wave events (e.g., Nosé et al.,
1998; Balasis et al, 2012; Xu et al., 2013). Using the wavelet method, with
the Morlet mother function, we produce the power spectrum of the magnetic
field series for 50 logarithmically spaced frequencies from 20 to 100 MHz
(Balasis et al., 2013), and remove the aforementioned margins. In parallel to
that, the positional vector of the spacecraft is extracted from the files and
converted to magnetic coordinates (magnetic latitude, longitude and local
time), as well as the electron density series from the EFI data files of the
same day. The final spectrum, along with the time series of the magnetic
field, the electron density, and all positional information are then exported
in a daily file and saved in the database.
The wave detection begins by reading the daily output files and segmenting
them in tracks (half-orbits) from -90∘ to +90∘ at
magnetic latitude. For each such track, the maximum power per second that is
stored in the spectrum is calculated and all segments of consecutive points
(seconds) that exceed a threshold of 0.5 nT2 Hz-1 (which roughly corresponds to a pulsation with a minimum amplitude
of 0.15 nT) are labeled “candidate events”. Each candidate is tested
against a series of criteria that help rule out artificial signals that might
result from instrument or telemetry errors. As such, for the candidate event
to not be discarded, it must exhibit a duration of at least 2 times its peak
period, it must have an amplitude that does not exceed certain limits
(10 nT), and it must be smooth enough to constitute a continuous pulsation,
so its difference series must always be smaller than ±1 nT. These
threshold values have been deduced empirically, by visual examination of a
large number of events, and it was found that candidates that exceed these
values were polluted by spikes or large discontinuities and thus should be
removed from the process. In order to avoid traces of activity from lower Pc
classes (below 20 MHz) that have not been completely eradicated by the
filtering process, we further demand that the peak of the wave activity be at
a frequency that does not lie at the limits of the examined range, so only
pulsations with a peak frequency that lies above 21 MHz are accepted.
In order to remove events that are influenced or caused by ESFs at low
latitudes, field-aligned or auroral currents at higher latitudes, or in
general by other, unclassified anomalies in the electron density profiles, we
introduce the Plasma Instabilities category and assign to it all wave-like
events that can be attributed to these kinds of phenomena. In order to do so,
we impose two criteria on the Level 2 product series and demand that in order
for a candidate to be a true Pc3 wave event, it must exhibit a value of
bubble probability (as defined in the IBI product) of less than 1 % and a
field-aligned current amplitude (taken from the FAC product) that is less
than 0.5 µA m-2, both of which must be met for the entire
duration of the event. Additionally, if the candidate was detected when the
satellite was located in the nightside sector, an additional criterion must
be met, namely that its electron density series (extracted from the EFI data
files) must not display abrupt changes. In any of these cases the candidate
is classified as belonging to the Plasma Instabilities class and is saved in
a separate database. On the other hand, if the candidate successfully passes
the two criteria for ESF and FAC detection and is located either in the
dayside sector or on the nightside, but exhibits a smooth enough electron
density series, then it is classified as a Pc3 wave.
In both cases, for every event several characteristics are extracted, such as
its duration, peak frequency, average and total power, and bandwidth (the
range of frequencies for which the event exhibits power above 50 % of its
peak value). All these are saved in a separate matrix for further
post-processing and derivation of statistics. For the production of wavemaps,
a slightly different approach was used, since waves are by nature extended in
space and cannot be accurately represented by a single number (or set of
numbers). For this case, the coordinate space, either geographical latitude
versus longitude or magnetic latitude versus magnetic local time (MLT), is
divided into a 50 by 50 grid, which provides a resolution of 3.6∘ in
latitude, 7.2∘ in longitude, and slightly less than half an hour in
local time. For every second in the duration of an event, its total Pc3 power
is calculated and added to the appropriate grid point to which the
measurement belongs, based on the satellite's location at the same moment,
thus allowing the entire extent of the wave to be accurately represented. In
order to make the resulting maps less dependent on the satellite's orbit, we
divide the summed power by the number of seconds the satellite has spent in
the corresponding point.
Swarm Pc3 wave event. A wave event as detected by the Swarm
constellation with Swarm B (a), A (b), and C (c)
showing the filtered series of the magnetic field magnitude (top panels),
their corresponding wavelet spectra for the joined Pc3 and Pc4 range (middle
panels), and a composite plot of the measured electron density (green line)
and their location at magnetic latitude (blue line) from -60∘ to
+60∘ (bottom panels).
Swarm equatorial spread-F event. As in Fig. 1 for another track of
the three satellites.
Swarm Pc3 wave power map in magnetic coordinates. Pc3 wave power per
second mapped on the magnetic latitude versus MLT grid.
Swarm-based ULF wave index
Before delving into the wavemaps and the wave index, it is useful to showcase
two examples of the methodology applied for our analysis. In Figs. 1 and 2 we
show two tracks that correspond to a dayside (MLT ∼ 11:00) detected
wave event and a nightside (MLT ∼ 23:00) episode that is attributed to
the presence of an ESF event. The data are taken from 23 June 2015, a day
which marked the peak activity in the main phase of a geospace magnetic
storm, with a minimum Dst index value of -204 nT, at 05:00 UT. The wave
event is captured by the northbound pass of all three satellites, here
showing only the part from -60∘ to +60∘ in magnetic
latitude, and is depicted from 01:25 to 01:56 UT for the lower Swarm A and C
and, a few minutes later, from 01:42 to 02:14 UT for Swarm B. The
ESF-related event is detected only by Swarm A and C on their southbound pass
from 05:19 to 05:51 UT and is characterized by the two, symmetric around the
magnetic Equator, disturbances in the electron density profile. The ESF
events or equatorial plasma bubbles are nightside phenomena identified by
their plasma signature as sudden depletions in the electron density profile.
We also observe in Fig. 2 the corresponding magnetic signature of the
specific ESF event (middle panel), which can be easily mistaken, if it is
examined alone, for a wave signature unless the accompanying electron density
perturbations are taken into account.
Figure 3 shows the magnetic latitude versus MLT map of wave power for all
three satellites of the constellation. As can be seen, the bulk of the Pc3
wave activity is located in the equatorial dayside sector (peaking at 09:00,
10:00–11:00, and 12:00–14:00 MLT for Swarm B and at 08:00–09:00,
11:00–12:00, and 14:00–15:00 MLT
for A and C), with the two lower satellites A and C displaying statistically
greater power than the higher Swarm B. We note that overall the Pc3 wave
activity extends to as early as 06:00 and as late as 17:00 MLT. These
results are comparable with the ones derived by Balasis et al. (2015b) for 1
year of Swarm data, with the exception of auroral zones (more information on
this issue is given later in this section). The small shift of approximately
2 h in the peaks of the activity between Swarm B and the lower pair is
attributed to the angular separation of the orbital planes of the satellites,
which for the time period examined ranged from 1 to 2 h in local time. This
is a strong indication that all satellites, despite their latitudinal and
temporal differences, detect the same events (at least as far as the
strongest ones are concerned) and just map them in different local times due
to the shift in their orbital planes. As this angular separation increases
with time, it will further elucidate the extent in local time of Pc3 wave
phenomena. The analogous wavemap in geographic coordinates (latitude versus
longitude) is shown in Fig. 4. The striking observation here is that most of
the activity is located around the area of the South Atlantic Anomaly (SAA),
something that has already been mentioned by Balasis et al. (2015b) and is
attributed to the lower magnitude of the geomagnetic field in this region,
which favors the occurrence of compressional waves.
Swarm Pc3 wave power map in geographic coordinates. Pc3 wave power
per second mapped on the geographic latitude versus geographic longitude
grid.
Based on the latitudinal distribution plots of Figs. 3 and 4, there are no
Pc3 waves observed at all in the topside ionosphere below -60∘ or
above +60∘ in both the magnetic and geographic wave power maps,
which is obviously an erroneous result. This outcome arises from the
application of the Swarm Level 2 single-spacecraft FAC data product
correction in our analysis. Since FAC are practically always present at high
latitudes, the inclusion of this Swarm Level 2 product apparently eliminates
all the Pc3 wave activity there and interprets it as signatures associated
with these currents. For this reason, we have finally decided not to use the
Swarm FAC product in deriving the final version of the ULF wave power maps
based on 2 years of Swarm data, which are now presented in Figs. 5 and 6 in
magnetic and geographic coordinates, respectively.
Summing the total power of each detected wave event for every track
(half-orbit) and keeping only daytime tracks, we get the total track-by-track
power. To reduce the range of these values, which might differ by several
orders of magnitude, we define the Pc3 Power Index as the logarithm (base 10)
of the total track-by-track power and hence produce the three Swarm Pc3 Power
Indices (one for each satellite), which are shown in the top panels of
Figs. 7 and 8. Tracks which exhibit index values below 2 are considered
“quiet”, while for the rest we can define three different activity levels:
“low” for index values between 2 and 3, “moderate” for values between 3
and 4, and “high” for those with index values above 4.
In an attempt to capture the relation between Pc3 waves and geospace
conditions, we incorporate into our analysis the time series of various solar
wind parameters and geomagnetic activity indices, downloaded from the OMNIWeb
Plus data service of NASA's Space Physics Data Facility. These are the
magnitude and three Cartesian components of the interplanetary magnetic field
(BIMF) as well as the solar wind velocity (Vsw), both in the GSE
coordinate system, the solar wind proton density (Np),
temperature (Tp), the solar wind dynamic pressure
(Pdyn), Alfvénic speed (VAlfvén), sound speed
(Vsound) and, based on the latter, the Mach numbers, both
Alfvén (MA) and magnetosonic (MS). In addition to those we
derive the magnetic field's cone angle (θB), defined as the angle
between the BIMF vector and its component along the
Sun–Earth axis (Greenstadt and Olson, 1976), and the magnetopause standoff
distance (RMP), defined as RMP=110.2(NpVx2)-1/6 (Kivelson and Russell, 1995). Finally, to incorporate the
magnetospheric response to the solar wind, we also include two indices of
geomagnetic activity, namely the Auroral Electrojet (AE) index and the
symmetric disturbance index for the horizontal component of the Earth's
magnetic field (SYM-H). The first, being a high-latitude index, operates as
an indicator of substorm activity, while the latter is highly correlated with
the disturbance storm time (Dst) index and therefore can be regarded as a
proxy for the ring current conditions and thus for geomagnetic storms. All
these are depicted in the bottom six panels of Figs. 7 and 8 (for clarity we
have ignored the vector components of BIMF and
Vsw and show only their magnitude).
Swarm Pc3 wave power map in magnetic coordinates without the FAC
correction. As in Fig. 3 without the application of the Swarm Level 2
single-spacecraft FAC data product.
Swarm Pc3 wave power map in geographic coordinates without the FAC
correction. As in Fig. 4 without the application of the Swarm Level 2
single-spacecraft FAC data product.
Swarm ULF wave index time series. From top to bottom: Pc3 power
indices for the three satellites of the Swarm constellation (A: first panel,
B: second panel, C: third panel), solar wind parameters (Vsw,
VAlfvén, MA, Vsound, MS) and the
SYM-H index. Ticks on the x axis denote the middle of the corresponding
month.
Swarm ULF wave index time series. From top to bottom: Pc3 power
indices for the three satellites of the Swarm constellation (A: first panel,
B: second panel, C: third panel), solar wind parameters
(BIMF, θB, Np, Tp,
Pdyn), and the AE index. Ticks on the x axis denote the middle
of the corresponding month.
To calculate the correlations between the three Swarm Pc3 Indices and the
various solar wind parameters and geomagnetic indices, we considered all
possible pairwise combinations, interpolated the parameter series to the
timestamps of each Pc3 Index (using a simple, linear interpolation scheme),
and computed the Pearson correlation coefficient (Pearson, 1895). The results
of this analysis, for all possible combinations, can be seen in Table 1.
Looking at the table it becomes evident that the parameter that is most
correlated with Pc3 wave activity is the solar wind velocity and especially
its component along the XGSE axis. The negative sign in the
VxGSE correlation just points out the obvious fact that it
is the earthward direction that is related to the generation of Pc3 waves.
This observation is well known in the literature, as was first made in the
60s (Saito, 1964), but its presence can be seen as a validation of our
methodology. Next in order of importance are the magnetosonic Mach number
MS and its corresponding velocity Vsound, along with the
magnetopause standoff distance RMP. For the latter the negative
sign indicates that enhanced Pc3 activity takes place when the magnetosphere
is most compressed by the solar wind and thus when RMP exhibits
lower values. All these reinforce the idea of Pc3 waves being generated at
the bow shock and propagating as compressional mode waves up until the
ionosphere, where they are detected by the Swarm satellites (Yumoto et al.,
1984; Heilig et al., 2007). Conversely, on the ground these waves are
detected as surface geomagnetic pulsations, and thus there the prominent
factors are the Alfvénic velocity and its respective Alfvénic Mach number
(Heilig et al., 2010), instead of the magnetosonic one which applies to our
case. Finally, the last two important parameters are the cone angle, which
seems to indicate that enhancements in Pc3 activity are related to low
θB values and thus to more horizontal BIMF
configurations, and the solar wind's proton temperature Tp. In
general though, all correlation values are very low, a fact that is due to
the large noise component that characterizes all time series, since for most
of the time examined the solar wind parameters exhibit very low (background)
levels of activity which are only sparsely interrupted by intense events. We
have repeated the analysis using a moving time window with a length that
corresponds to 50 tracks, in which case we noticed that for some
geomagnetically disturbed periods, the values of the correlations for various
parameters can increase dramatically. As an example, for the Pc3 activity at
the tail of the August 2014 storm we get correlations with the
Vsw that achieve values as high as 0.64 and, for the MS,
values as high as 0.47. Unfortunately, the increase in the correlations does
not always follow the increase in geomagnetic activity, so the interplay
between these parameters is much more complex and almost certainly governed
by nonlinear interactions, although their order of importance remains roughly
the same.
As an extra step, we shifted the various parameters' time series by as much
as 48 h before and after their actual timestamps, with a time step of 1 h,
and re-calculated the correlations, to see whether some specific time lag
might yield better results, since the conditions in the solar wind might need
several minutes up to a few hours to drive Pc3 waves and allow them to
penetrate into the inner magnetosphere until their effects are detected by
the Swarm satellites in LEO. Unfortunately this did not yield any meaningful
results, since most of the above-mentioned quantities exhibit their peak
correlation values for zero time lag and, when they do not, they do not seem
to do so in a consistent way for all three satellite indices. The only
possible exception is the velocities Vsw and Vsound,
which show marginally better correlation factors for a time lag of 2 to 6 h,
but the improvements are so small that it is difficult to draw any
conclusions from that fact alone.
Correlation coefficients for each pairwise combination
between the three Swarm Pc3 indices and each of the solar wind or geospace
parameters for the entire May 2014 to May 2016 period.
Swarm A Pc3Swarm B Pc3Swarm C Pc3indexindexindexBIMF0.001-0.0350.009BxGSM0.028-0.0490.035ByGSE-0.044-0.011-0.053BzGSE0.018-0.0180.014ByGSM-0.041-0.015-0.045BzGSM0.013-0.0170.010Vsw0.2590.2200.244VxGSE-0.261-0.221-0.245VyGSE0.0840.1060.080VzGSE-0.037-0.045-0.050Np-0.023-0.0670.006Tp0.1120.1130.139Pdyn0.0830.0290.117MA0.1110.0750.107MS0.1840.1520.178AE0.0610.0200.057SYM-H-0.108-0.052-0.093θB-0.119-0.139-0.109VAlfvén0.0170.009-0.008Vsound0.1480.1510.157RMP-0.138-0.092-0.151
As for the magnetospheric response to the solar wind, it can be said that the
relation between Pc3 waves and magnetic storms is not a simple one. Great
storms always coincide with enhancements in Pc3 activity, as can be seen for
the January, March, June, October, and December events of 2015, while the
extremely quiet period of July and August 2014 also appears completely silent
in the wave power series. On the other hand though, significant increases in
Pc3 activity do not always coincide with geomagnetic disturbances, as can be
seen in the distinct example of February 2015, although for that period there
was a moderate increase in Vsw and Np that
consequently led to an increase in MS. From the two indices employed here,
the SYM-H seems to be more correlated with the type of activity that is
captured by our Pc3 index, as we mostly focus on equatorial to
mid-latitudinal wave activity. The level of the correlations though is again
quite low, contrary to the widely spread misbelief that ULF power and
geomagnetic activity are closely correlated. This misbelief was refuted
recently by Currie and Waters (2014) and it is also evident here, as well.
Discussion and conclusions
Our findings on Pc3 wave power distribution in magnetic and geographic
coordinates based on 24 months of Swarm VFM observations (Figs. 5–6) confirm
the results of a previous study on Pc3 wave power features in the topside
ionosphere revealed by 1 year of Swarm absolute scalar magnetometer (ASM)
observations (Balasis et al., 2015b). It is worth mentioning that the present
study uses a different methodology for the selection of wave events involving
additional steps and following the detection of candidate events with a
wavelet analysis technique and the requirement of a smooth profile for the
electron density data of the previous study. Here, we incorporate additional
analysis steps consisting of the application of the CHAOS-6 model (prior to
the wavelet analysis) and the utilization of Swarm Level 2 products (i.e.,
the FAC and IBI products) to impose constraints on the Swarm data for the
wave event selection.
Forsyth et al. (2017) suggested that many of the magnetic field perturbations
on small scales may contain a significant fraction of perturbations which are
the result of wave activity in the vicinity of the spacecraft or current
sheets inclined to the motion of the spacecraft. As a result, they noted that
extreme care must be taken in interpreting the temporal variation of the
magnetic field observed by a moving spacecraft as relating to the spatial
structures which can be used to infer field-aligned currents. Moreover, they
suggested that since such assumptions are used to produce the Swarm Level 2
single-spacecraft FAC data product (Ritter et al., 2013), care should be
taken when using or interpreting this data product as well. Our results also
demonstrate that the inclusion of this product to constrain the wave activity
in Swarm wave power maps inevitably eliminates all the wave activity at high
latitudes, which is physically unrealistic (Figs. 3 and 4). Therefore, we
have dropped the use of the Swarm FAC product in deriving the final version
of ULF wave power maps based on Swarm observations from May 2014 to May 2016.
However, we cannot rule out the possibility that a fraction of the
high-latitude wave activity seen in these maps (Figs. 5 and 6) is probably
attributed to the distribution of field-aligned currents.
In this study, we demonstrate how a Swarm daytime, track-by-track Pc3 wave
index can be systematically derived for the topside ionosphere calculated
using 2 years of the constellation's data. This is the first attempt, at least
to our knowledge, to derive a ULF wave index from LEO satellite data (see,
e.g., Borovsky and Denton, 2014). Consequently, we compare the variations of
Swarm wave index values to corresponding variations of solar wind variables
and geomagnetic activity indices in order to search for possible correlations
between them. Indeed, for epochs around intense magnetic storms (cf. the
storm events of March, June, and December 2015), there seems to be an
increase in Pc3 activity and the values of the Pc3 indices were shown to
correlate with parameters that are well known as suspects for driving of Pc3
waves, like Vsw, Vsound, RMP, and
θB. In the future we plan to examine the possibility of extending
the formulation of the index in a manner similar to the one introduced by
Russell and Fleming (1976), by including the average frequency of the wave
events that have been aggregated for each track and that possibly also
incorporate the values of some index of geomagnetic activity (e.g., Kp).
Moreover, the same technique can also be applied to derive a higher-frequency
Swarm ULF wave index (e.g., in the Pc1 band) using the high-resolution (i.e.,
50 Hz) VFM data from the mission. Pc1 waves are a critical element of space
weather as they are considered responsible for the energetic-particle
pitch-angle diffusion in radiation belts.
Motivated by the potential importance of enhanced ULF wave activity for
particle energization in radiation belts and hence space weather effects,
Kozyreva et al. (2007) and Romanova and Pilipenko (2009) proposed the
calculation of the ULF wave index in the Pc5 band from ground-based
magnetometer data, and, more recently, Pilipenko et al. (2017) outlined
possible directions of this index advancement. Waters and Menk (2016)
suggested that a ground Pc3 pulsation index may be useful for identifying
contamination by background activity in geomagnetic and aeromagnetic surveys
used in geophysical exploration. Based on the results by Heilig et al. (2010)
from ground magnetometers, further development of Pc3 activity indices as
proxies of solar wind conditions was also recommended (Waters and Menk,
2016). Therefore, the Swarm ULF wave index proposed here can be considered a
candidate for a standard Level 2 mission product aiming at the potential
identification of episodes with persistent enhanced solar wind activity. An
alternative option could be to launch a website that provides a database with
a provisional Pc3 index, which would be made available to the international
community for testing and validation. Ultimately, the new index can
potentially serve as an integral part of a space weather risk assessment
scheme for the critical infrastructure existing in the near-Earth
electromagnetic environment.
All data are available through the ESA Earth Online platform, after registration for
an ESA Earth Observation Users' Single Sign On account
https://earth.esa.int/web/guest/umsso?orig_request=/web/guest/picommunity/myearthnet (ESA, 2018). The AE and SYM-H indices data have been obtained
from the World Data Center for Geomagnetism of Kyoto University at
http://wdc.kugi.kyoto-u.ac.jp/index.html (WDC, 2018), whereas the solar wind data have been
retrieved through the NASA OMNIWeb space physics data facility at
http://omniweb.gsfc.nasa.gov/ (GSFC, 2018).
The authors declare that they have no conflict of
interest.
This article is part of the special issue “Dynamics and
interaction of processes in the Earth and its space environment: the
perspective from low Earth orbiting satellites and beyond”. It is not
associated with a conference.
Acknowledgements
This study makes use of data from the Swarm spacecraft mission, which is
funded and managed by the European Space Agency. We acknowledge support of
this work by the PROTEAS II project (MIS 5002515), which is implemented under
the “Reinforcement of the Research and Innovation Infrastructure” action,
funded by the ”Competitiveness, Entrepreneurship and Innovation” operational
programme (NSRF 2014-2020) and co-financed by Greece and the European Union
(European Regional Development Fund).
The topical editor, Rumi Nakamura, thanks Vyacheslav Pilipenko and two
anonymous referees for help in evaluating this paper.
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