Simultaneous ground-based and in situ Swarm observations of equatorial F-region irregularities over Jicamarca
- 1Mbarara University of Science and Technology, Department of Physics, Mbarara, Uganda
- 2Swedish Institute of Space Physics, Uppsala, Sweden
- 3Radio Observatorio de Jicamarca, Instituto Geofísico del Perú, Lima, Peru
Correspondence: Sharon Aol (email@example.com)
Ionospheric irregularities are a common phenomenon in the low-latitude ionosphere. They can be seen in situ as depletions of plasma density, radar plasma plumes, or ionogram spread F by ionosondes. In this paper, we compared simultaneous observations of plasma plumes by the Jicamarca Unattended Long-term Investigations of the Ionosphere and Atmosphere (JULIA) radar, ionogram spread F generated from ionosonde observations installed at the Jicamarca Radio Observatory (JRO), and irregularities observed in situ by Swarm in order to determine whether Swarm in situ observations can be used as indicators of the presence of plasma plumes and spread F on the ground. The study covered the years from 2014 to 2018, as this was the period for which JULIA, Swarm, and ionosonde data sets were available. Overall, the results showed that Swarm's in situ density fluctuations on magnetic flux tubes passing over (or near) the JRO may be used as indicators of plasma plumes and spread F over (or near) the observatory. For Swarm and the ground-based observations, a classification procedure was conducted based on the presence or absence of ionospheric irregularities. There was a strong consensus between ground-based observations of ionospheric irregularities and Swarm's depth of disturbance of electron density for most passes. Cases, where ionospheric irregularities were observed on the ground with no apparent variation in the in situ electron density or vice versa, suggest that irregularities may either be localized horizontally or restricted to particular height intervals. The results also showed that the Swarm and ground-based observations of ionospheric irregularities had similar local time statistical trends with the highest occurrence obtained between 20:00 and 22:00 LT. Moreover, similar seasonal patterns of the occurrence of in situ and ground-based ionospheric irregularities were observed with the highest percentage occurrence at the December solstice and the equinoxes and low occurrence at the June solstice. The observed seasonal pattern was explained in terms of the pre-reversal enhancement (PRE) of the vertical plasma drift. Initial findings from this research indicate that fluctuations in the in situ density observed meridionally along magnetic field lines passing through the JRO can be used as an indication of the existence of well-developed plasma plumes.
Generally, the ionosphere can be viewed as a layer with a relatively uniform plasma density distribution (Ngwira et al., 2013). However, the night-time low-latitude ionosphere is characterized by localized plasma density structures, known as ionospheric irregularities (Stolle et al., 2006). The equatorial ionospheric irregularities may be identified as irregular plasma density “bite-outs” observed in situ along low Earth orbit (LEO) satellite tracks in the topside ionosphere (Woodman and La Hoz, 1976; Tsunoda, 1980; Tsunoda et al., 1982; Kelley, 2009). The equatorial ionospheric irregularities may also manifest as equatorial spread-F (ESF) signatures, which are irregular signatures on ionograms due to backscattering from the bottom side of the nighttime F-layer and also above (Woodman and La Hoz, 1976; Hysell and Burcham, 1998). Ionospheric irregularities have also been called plasma plumes because of their appearance in range versus time radar displays (Woodman and La Hoz, 1976). The plumes are characterized by elongated, wedge-like cross sections that extend from the bottom of the F layer to higher altitudes (Tsunoda, 1980; Tsunoda et al., 1982; Ma and Maruyama, 2006). Equatorial ionospheric irregularities usually extend along magnetic field lines to magnetic latitudes of about to (Ossakow, 1979; Kil and Heelis, 1998; Nishioka et al., 2008; Kelley, 2009).
Ionospheric irregularities in the low latitudes arise after sunset due to the Rayleigh–Taylor instability (RTI) which originates from the lower F region (Woodman and La Hoz, 1976; Kelley, 2009; Schunk and Nagy, 2009). These irregularities vary with respect to scale, from several centimetres to hundreds of kilometres (Lühr et al., 2014; Xiong et al., 2016; Rino et al., 2016). A width of about 100 km was observed for the depleted ESF bands using an all-sky airglow imager (Otsuka et al., 2004). The occurrence of ionospheric irregularities varies according to local time, season, longitude, latitude, and solar and magnetic activity (Kil et al., 2009). Their occurrence is a subject of interest because of the effect they have on propagating radio signals. Their presence in the ionosphere may cause amplitude and phase scintillations of radio signals, thereby affecting many applications that rely on these signals (Yeh and Liu, 1982).
Equatorial ionospheric irregularities have been observed many times using ground-based instruments, such as incoherent and coherent scatter radars, ionosonde, and airglow cameras, and space-based instruments, such as rockets and LEO satellites (e.g. Woodman and La Hoz, 1976; Hysell et al., 1997; Nishioka et al., 2008; Fejer et al., 1999; Burke et al., 2003; Sripathi et al., 2008; Wang et al., 2015; Hickey et al., 2018; Aa et al., 2020). It should be noted that although ionospheric irregularities have been studied extensively, uncertainties still exist in understanding their evolution because of their varying scale with respect to size (Abdu, 2001; Sripathi et al., 2008; Aa et al., 2020). In this regard, different instruments are limited to observing ionospheric irregularities of specific sizes (Sripathi et al., 2008; Aa et al., 2020). Therefore, coordinated observation of ionospheric irregularities using different instruments is an effective way to generate an integrated and comprehensive image for specifying ionospheric irregularities of different sizes (e.g. Sripathi et al., 2008; Cherniak et al., 2019; Aa et al., 2019, 2020). Specifically, the Jicamarca Radio Observatory (JRO) has provided a rare opportunity to observe ionospheric irregularities using multiple ground-based instruments due to its strategic location (12.0∘ S, 76.8∘ W; magnetic latitude 0.6∘ S) at the magnetic equator. Many studies have reported the connection between scintillation-producing ionospheric irregularities observed by JULIA and equatorial plasma bubbles (EPBs) observed in situ over Jicamarca (e.g. Morse et al., 1977; Basu et al., 1980; Hysell and Burcham, 2002; Burke et al., 2003; Kelley et al., 2009; Siefring et al., 2009; Roddy et al., 2010; Nishioka et al., 2011). However, the relationship between metre-scale irregularities detected by coherent scatter radars and the underlying state parameters of the ionospheric plasma is not yet well understood (Hysell et al., 2009). Previous studies (e.g. Kelley et al., 2009; Siefring et al., 2009; Hysell et al., 2009; Roddy et al., 2010; Nishioka et al., 2011) have mostly compared zonally oriented in situ plasma density measurements from the Communication Navigation Outage Forecasting System (C/NOFS) satellite with JULIA observations. The European Space Agency's Swarm satellites neatly revisit the JRO in orbits oriented in the meridional direction, providing a renewed opportunity to study in situ ionospheric irregularities recorded by Swarm in the meridional direction in comparison with observations from Jicamarca.
A quantitative statistical relationship between plasma bubbles observed in situ in the meridional direction, 250 MHz amplitude scintillation, and JULIA observations was reported by Burke et al. (2003) using data recorded by the polar-orbiting Defense Meteorological Satellite Program (DMSP). From the observations made by Burke et al. (2004), the plasma plumes recorded by JULIA frequently occurred at altitudes lower than that of the DMSP orbit. Most of the plasma plumes failed to reach altitudes >600 km and, therefore, were not observed by DMSP satellites that orbited at an altitude of about 840 km. It is possible to compare in situ measurements made by Swarm and JULIA observations at altitudes of 460 km (Swarm A and C) and 510 km (Swarm B). In contrast to DMSP, Swarm allows a comparison of measurements from identical instruments at different altitudes and in different longitudinal sectors (Zakharenkova et al., 2016). Previous comparison of Swarm in situ measurements with ground-based radar observations (e.g. Zakharenkova et al., 2016) mostly used Langmuir Probe (LP) measurements at a 2 Hz frequency. The faceplate carried by Swarm as part of the electric field instrument (EFI) has enabled the discovery of small-scale (down to 500 m length along the spacecraft track) ionospheric irregularities. Moreover, the previous comparison of Swarm in situ measurements with ground-based radar observations was mostly a single-case presentation. Zakharenkova et al. (2016) demonstrated that the gradual spatial separation between Swarm A, C, and B would decrease the likelihood that all three satellites could capture ionospheric irregularity signatures in the same localized region or near particular equipment installed on the ground, such as ionosonde and radars. Nevertheless, only one single case of comparison between Swarm and JULIA observation was provided by Zakharenkova et al. (2016).
In this paper, we quantitatively compared the in situ observations of ionospheric irregularities recorded by the Swarm satellites with ground-based measurements of plasma plumes made by the JULIA radar for the years from 2014 to 2018 in order to determine whether Swarm in situ observations can be used as indicators of the presence of plasma plumes and spread F on the ground. The comparison is complemented by ionosonde measurements of spread F over the JRO. Booker and Wells (1938) observed echoes on ionograms from ionosonde observations and proposed that these echo signatures were originating from ionosphere disturbances. As far as we know, Wang et al. (2015) were among the first to make concurrent observations of strong range spread F and ionospheric irregularities measured in situ using the ROCSAT-1 satellite; they found that strong spread F were caused by the ionospheric irregularities. However, ROCSAT-1 orbited at an altitude of about 600 km with a 35∘orbital inclination. Therefore, we also compared the JULIA and Swarm observations of ionospheric irregularities with spread-F signatures recorded by an ionosonde co-located with the JULIA radar. To understand the range of altitude above sea level where ionospheric irregularities occur and the effect that they have on ground observations, a comparison of in situ electron density variation with ground-based measurements over a long time period is essential.
This paper is organized as follows: in Sect. 2, the data and methods used in this study are described; in Sect. 3, the results are presented and discussed; and the findings of this study are summarized in Sect. 4.
This section provides brief descriptions of the instruments and data sets used to examine the signatures of ionospheric irregularities in this research: we analysed data obtained from Swarm, the JULIA radar, and ionosonde.
2.1.1 Swarm measurements of electron density
The Swarm mission consists of three polar-orbiting satellites – Swarm A, B, and C (Friis-Christensen et al., 2006). They were launched into near-polar orbits at an initial altitude of about 500 km on 22 November 2013 (Xiong et al., 2016; Wan et al., 2018). Each satellite is equipped with an electric field instrument (EFI) that is mounted on the ram side of the spacecraft (Friis-Christensen et al., 2006; Knudsen et al., 2017). The ion density Ni is derived from the EFI faceplate current assuming that the current is carried by ions hitting the faceplate due to the orbital motion of the spacecraft (Buchert, 2016). However, due to quasi-neutrality, Ni must be equal to the electron density Ne. With the 16 Hz Ne measurements, Swarm observes ionospheric irregularities with sizes of up to 500 m. Friis-Christensen et al. (2006) and Knudsen et al. (2017) provide detailed information on Swarm and the onboard instruments. In this study, we used the 16 Hz Ne measurements to examine topside ionospheric irregularities. The faceplate Ne data are readily available at http://earth.esa.int/swarm (last access: 23 February 2020).
2.1.2 The JULIA radar
The JULIA radar is a PC-based system for data acquisition. JULIA uses low-power transmitters with a frequency of approximately 50 MHz and Jicamarca's main antenna (Hysell and Burcham, 1998, 2002; Burke et al., 2003). Its aim is to record ionospheric irregularities and neutral atmospheric waves at the equatorial region for long periods of time. The pulse width used in the JULIA experiments during the period of study was 25 µs, and the pulse repetition was 160 pulses per second. In addition, 248 range gates that were separated by 3.75 km were sampled – from 0 km to about 930 km – during the period of study. For the identification of 3 m scale ionospheric irregularities, the backscattered 50 MHz JULIA radar echo was used. The radar observations provide the signal-to-noise ratio (SNR), Doppler velocity, and spectral width as a function of height and time. Data collected by the JULIA radar are readily available at http://jro.igp.gob.pe/madrigal/ (last access: 23 February 2020). The website provides JULIA data from 1996 to date. Our analysis was restricted to the years from 2014 to 2018, as this was the period for which JULIA, Swarm, and ionosonde data sets were available.
2.1.3 The digital ionosonde
The equatorial spread-F (ESF) signatures are often recorded by ionosondes installed at the JRO. The ionosonde at the JRO is a Digisonde DPS-4 (Reinisch et al., 1998) which records ionograms (altitude versus frequency plots) at 15 min intervals. The Automatic Real-Time Ionogram Scaler with True height (ARTIST) ionogram autoscaling tool, developed at University of Massachusetts Lowell Center for Atmospheric Research (UMLCAR), is used to scale the ionograms, and the outputs are plasma frequency profiles versus altitude (Reinisch et al., 2005; Zhang et al., 2015). The equatorial spread-F signatures were analysed from the ionograms. The ionosonde data are also available on the Madrigal website, and we used all of the Jicamarca ionograms for the years from 2014 to 2018.
This section presents the analysis techniques used in this study to identify the observed ionospheric irregularity signatures with Swarm, JULIA, and the ionosonde.
2.2.1 In situ ionospheric irregularity identification
To examine topside ionospheric irregularities, the 16 Hz Ne Swarm faceplate data were used. We followed the same method as Ngwira et al. (2013), Huang et al. (2014), and Aol et al. (2020) to derive the absolute electron density perturbation along Swarm orbital tracks, but we focused mainly on small-scale equatorial plasma structures. We utilized a 2 s running mean filter to determine the mean Ne. The selected running mean is equivalent to a 15 km scale length, given Swarm's velocity of about 7.5 km s−1. The mean Ne was subtracted from the original observations to get the residual, ΔNe, in a similar fashion to Ngwira et al. (2013), who obtained the residual using total electron content (TEC) data. The standard deviation of the residuals was then calculated at a running window of 2 s to represent the magnitude of the perturbation, std(ΔNe). There is no standard threshold definition of how large std(ΔNe) must be to identify plasma irregularities (Huang et al., 2014; Wan et al., 2018). However, the period considered in this study was characterized by low solar activity, and the recorded ionospheric irregularities were very weak. Therefore, a threshold value of std m−3, similar to that adopted by Huang et al. (2014), was selected to provide a reasonable irregularity event identification at the small scales and the relatively low Swarm altitudes during the study period.
2.2.2 Ground-based ionospheric irregularity identification
The JULIA system computes and stores measurements of the zeroth and first lags of the autocorrelation function (ACF) of the signals from two receivers connected to the eastern and western quarters of the main antenna (Smith et al., 2015; Zhan et al., 2018). The total power, Doppler velocity at first moment, and Doppler spectral width of the scattering signals can be determined from these measurements (Hysell et al., 1997; Hysell and Burcham, 1998). Of particular interest was the SNR measurements derived by the JULIA system to check plasma plumes for a given evening. In addition, we also used the vertical plasma drift measurements made by the Jicamarca incoherent scatter radar (ISR) to examine the pre-reversal enhancement (PRE) drifts (Fejer et al., 1996; Smith et al., 2016). Field-aligned irregularities in the F region are often observed by the JULIA radar between 18:00 and 06:00 LT (Hysell and Burcham, 1998; Smith et al., 2016). Therefore, to compare the Swarm observations with the JULIA measurements, only swarm satellite passes for the time between 18:00 and 06:00 LT were considered.
The comparison of JULIA and Swarm observations was supplemented with ionosonde measurements from the JRO. The ionosonde data analysis was carried out using the SAO Explorer software (Reinisch et al., 2005). To display ionograms, both the raw and processed (SAO) data were loaded into SAO Explorer. In addition, the spread-F index QF, known as the mean spread of the diffusing F-layer trace, was obtained by the ARTIST directly from the ionograms using SAO Explorer (Galkin et al., 2008; Zhang et al., 2015), and this was also used in this study to analyse the spread-F signatures. The spread-F index QF is defined as the extent of the diffuse reflection in kilometres averaged over all frequencies where a diffuse echo appeared. For simplicity, the virtual height is used at each frequency to determine the range extent of the reflection. The ARTIST software for data analysis is described by Galkin et al. (2008). Spread-F ionograms were similarly studied by Abdu et al. (2012) using magnetically conjugate ionosondes in South America and by Zhang et al. (2015) for ionosondes and scintillation receivers at Sanya. In the following section, the results of this study are presented and discussed.
3.1 Observations of ionospheric irregularities
Examples of equatorial ionospheric irregularity events observed by Swarm A and C on 9 March 2015 and Swarm B on 5 April 2015 are shown in Fig. 1.
In Fig. 1a, Swarm A and C encountered ionospheric irregularities along their tracks, occurring between about ±10 and ±20∘quasi-dipole latitude (QLat) (Laundal and Richmond, 2016), while they orbited over the JRO on 9 March 2015. Moreover, Swarm B, which orbited at about 510 km altitude above sea level, recorded ionospheric irregularities on 5 April 2015, as seen from Fig. 1b. Zakharenkova et al. (2016) also observed large Ne depletions along Swarm passes using the 2 Hz Ne measurements made by the LP in comparison with JULIA radar observations. With the 16 Hz data, Ne depletions can also be observed at even smaller scales – down to 500 m (Aol et al., 2020). Figure. 1b presents the ΔNe with the background variations subtracted. Figure 1c shows how well the quantified absolute density perturbation captured the small-scale ionospheric irregularities in the faceplate Ne measurements. Given the fact that the ionospheric irregularities were observed in situ at Swarm altitudes, this shows that these ionospheric irregularities were in the topside ionosphere. The observed ionospheric irregularities occurred post-sunset and were most likely due to the generalized RTI (Kelley, 2009).
The coherent scatter radar observations of ionospheric plasma irregularities are often shown in range–time–intensity format in which the SNR is plotted against altitude (range) and time (Woodman and La Hoz, 1976; Hysell and Burcham, 1998). The major categories of plasma plumes that have been observed by the JULIA radar are bottom-type, bottom-side, and topside (e.g. Woodman and La Hoz, 1976; Hysell and Burcham, 1998). Examples of these categories are presented in Fig. 2a–c, which show bottom-type, bottom-side, and topside structures respectively. In Fig. 2, the observed structures are generally visible post-sunset, and this coincides with the time when the generalized RTI is expected to intensify (Kelley, 2009).
In Fig. 2a, bottom-type structures are weak and narrow scattering layers, and their thickness is less than about 50 km. Bottom-type structures are too weak to induce prominent ionogram spread F or cause intense radio scintillation at very high frequency (VHF) frequencies and above (Hysell, 2000). Their disturbance in the ionosphere is also not sufficient to cause signatures on airglows (Hysell, 2000). Bottom-side structures correspond to broad, more structured, and stronger scattering layers at relatively higher altitudes that last for a few hours (as seen in Fig. 2b), whereas topside layers or radar plumes (seen in Fig. 2c) represent larger-scale elongated structures originating from bottom-side layers and extending to the topside ionosphere (Hysell and Burcham, 1998; Hysell, 2000; Chapagain et al., 2009; Chapagain, 2011). They are indicators of strong plasma plumes (Smith et al., 2016).
To check the altitude coverage of the various types of plumes observed by the JULIA radar compared to the Swarm altitudes, a histogram of the percentage occurrence of maximum heights was generated for the different types of plumes. To determine the plume maximum height, SNR outliers were first eliminated to minimize spurious data points. The maximum height then corresponds to the maximum range in kilometres where the SNR was recorded. Figure 3 shows the frequency of occurrence of the maximum height achieved by the various types of plumes for the years from 2014 to 2018.
In Fig. 3, the Swarm altitude range coincides with a high frequency of occurrence of the maximum range of topside plasma plumes. This reveals that the Swarm orbits are most suitable to detect topside plasma plumes compared with bottom-type and bottom-side plumes. The following subsection presents in situ observations of ionospheric irregularities by Swarm over or near the JRO longitude in comparison with the JULIA and ionosonde observations.
3.2 Coincident ground-based and swarm observations of ionospheric irregularities
Here, in comparison with the ground-based observations, selected Swarm orbits that were directly overhead or passed close to the JRO are presented with observed plasma density structures. Figure 4 shows example cases on 2 and 8 March 2015 where Swarm A and C passed directly over and near the JRO respectively.
Column (i) of Fig. 4 shows the range–time–intensity maps overlaid with Swarm A and C positions. The JULIA radar started to detect weak 3 m irregularities from an altitude of about 300 km at approximately 19:30 LT on 2 and 8 March 2015. Gradually, the irregularities evolved into a series of spectacular plume structures that extended to altitudes of about 800 km. The plumes were only visible in the pre-midnight hours, and this corresponds to the time when the RTI dominates (Kelley, 2009; Schunk and Nagy, 2009). The observed plasma plumes coincided with the Swarm passes.
Columns (ii) and (iii) in Fig. 4 show that Swarm satellites encountered ionospheric irregularities along their tracks on 2 March 2015 . The irregularities were more intense near the equatorial ionization anomaly (EIA) belts at about ±10 to ±15∘QLat than at the quasi-dipole equator. Zakharenkova et al. (2016) analysed one sample of plasma plumes recorded by JULIA; from the results they presented, several Global Positioning System (GPS) satellites orbiting over the JRO encountered irregularities near the magnetic equator on 2 March 2015. Therefore, the structures observed by Swarm could be associated with the JULIA plasma plumes on 2 March 2015. Roddy et al. (2010) and Nishioka et al. (2011) also presented single-case events while comparing in situ plasma density measurements made by the C/NOFS satellite with JULIA observations. However, in the results presented by Roddy et al. (2010) and Nishioka et al. (2011), the EIA could not be resolved because C/NOFS orbited in a nearly meridional direction.
On 8 March 2015, Swarm A and C crossed the quasi-dipole equator in the evening sector at geographic longitudes of about 81.6 and 80.17∘ W respectively. The Ne profiles of Swarm A and C in columns (ii) and (iii) of Fig. 4 show depletions near the quasi-dipole equator. However, the longitudes of the Swarm satellites were offset from the JRO longitude to the west. Burke et al. (2003) made a similar observation, comparing DMSP plasma density measurements with JULIA observations. Ionospheric irregularities are generally assumed to drift westward across the magnetic field lines (Kelley, 2009). Therefore, the depletions met by Swarm A and C may not correspond to the plumes observed by the JULIA radar. The ionospheric irregularities observed by Swarm on 8 March 2015 may correspond to the plume remnants that drifted across the radar beam.
We also checked on the spread-F signatures on ionosonde data from JRO in comparison with the results presented in Fig. 4. Figures 5 and 6 show ionograms produced on 2 and 8 March 2015 using the SAO explorer respectively. The ionosonde measurements were recorded at 15 min intervals.
The sequence of ionograms presented in Fig. 5 shows that spread-F signatures were continuously observed from 00:30 to 05:00 UT (19:30 to 24:00 LT), while Swarm encountered ionospheric irregularities on 2 March 2015 between about 20:27 and 21:05 LT (see Fig. 4).
The ionograms on 8 March 2015 also showed strong spread-F signatures starting at 00:15 UT (19:15 LT) and this coincided with the time period when ionospheric irregularities and plasma plumes were recorded by Swarm and JULIA respectively. The results presented in Figs. 4, 5, and 6 show that the in situ ionospheric irregularities, spread-F signatures, and plumes were observed over and near the JRO simultaneously. Strong range spread F is caused by ionospheric irregularities and can, therefore, be regarded as a result of the generalized RTI mechanism (Rastogi et al., 1989; Wang et al., 2008; Shi et al., 2011; Alfonsi et al., 2013). The spread-F signatures are triggered by irregularities at the bottom or within a growing plasma bubble or by declining bubbles (Abdu et al., 2012). Figures 4, 5, and 6 provide evidence that JULIA, Swarm, and the ionosonde simultaneously observed ionospheric irregularities over the JRO. In the next section, we present the results of a statistical analysis of Swarm, JULIA, and ionosonde observations.
3.3 Statistical analysis of occurrence of ionospheric irregularities
The formation of equatorial ionospheric irregularities is influenced by several factors including local time, season, and magnetic latitude and longitude. The data sets accumulated for the years from 2014 to 2018 were sufficient to compare the dependence of ground-based and in situ occurrence of ionospheric irregularities on various factors. Here, we present the results of the statistical analyses carried out in this study. The specific details of each statistical result are described in the following subsections.
3.3.1 Statistics of occurrence of ionospheric irregularities by category
The Swarm satellites regress in longitude by about 22.5∘ between orbital ascending nodes. Therefore, in comparison with JULIA and ionosonde data, the Swarm passes were allowed to be within ±5∘ magnetic longitude of the JRO to make sure that a sufficient amount of Swarm passes could be used for the statistical examination. Both JULIA and ionosonde data during the time when Swarm was within a ±5∘ longitudinal range of the longitude of the ground site were selected. Summary plots, such as those presented in Fig. 4, were generated for all days during the years from 2014 to 2018 for which the data were available. In total, 560 night-time orbits were used for which JULIA, Swarm, and ionosonde data were concurrently available. The outputs of the summary plots could be categorized into four cases considering the presence (or absence) of irregularities. In general, these four cases are as follows: irregularities observed both on the ground and in situ, no irregularities observed on the ground or in situ, irregularities observed only in situ, and irregularities observed only on the ground. For each range–time–intensity plot, the SNR corresponding to the peak height was determined and an event was identified as a significant irregularity when the peak height was ≥400 km. For a peak height less than 400 km, the events were classified as weak irregularities or were not considered to be irregularities. It is important to note that a peak height less than 400 km is a representation of bottom-type, bottom-side, and no equatorial spread-F signatures; therefore, all spread-F altitudes were taken into consideration during the analysis. For the in situ Swarm observations, we considered a threshold of 1×1010 m−3 for std(ΔNe) as a significant irregularity event, whereas std(ΔNe) values less than the threshold were not considered to be irregularities. For the ionosonde measurements, QF values greater than or equal to 20 km were considered to be significant irregularity events. For each category, the percentage occurrence was computed as a ratio of the total number of events in that category to the number of observations. These cases are presented in Fig. 7a for Swarm and JULIA and in Fig. 7b for Swarm and ionosonde.
Ionospheric irregularities were detected by Swarm and JULIA in about 55.08 % of the cases for Swarm A, 56.89 % of the cases for Swarm C, and 58.62 % of the cases for Swarm B (as seen from Fig. 7a). No ionospheric irregularities were detected by the Swarm satellites and JULIA in about 27.12 % of the cases for Swarm A, 25.0 % of the cases for Swarm C, and 21.55 % of the cases for Swarm B. In Fig. 7b, a high percentage occurrence was also observed when there was agreement (irregularities observed by both ionosonde and Swarm and no irregularities observed by the ionosonde and Swarm) between Swarm and ionosonde. The two categories where there was an agreement in Fig. 7a and b indicate that Swarm satellites, JULIA, and the ionosonde simultaneously observed ionospheric irregularities. Burke et al. (2003) also examined the relationship between measurements from JULIA and a DMSP satellite during 110 nights for the years from 1998 to 1999. In comparison with the statistical results presented in Fig. 7 for Swarm and JULIA, the DMSP satellite sampled very few EPBs compared with plumes detected by the JULIA radar. According to Burke et al. (2003), there was a low probability that JULIA and the DMSP satellite would encounter ionospheric irregularities because most plumes could not ascend to altitudes greater than 600 km. There were also some disagreements between the ground-based and space-based observations: JULIA and the ionosonde detected plume structures, whereas Swarm registered no events (as seen from the statistical results in Fig. 7a and b). For these cases, the Swarm altitudes during the pass were examined. It was observed that the plume structures did not ascended to Swarm altitudes by the time the satellites passed over Jicamarca or that the satellites were simply in a different location. For instances when Swarm registered events while JULIA and ionosonde recorded no signatures, we checked on the longitudinal separation between the satellite passes and the ground site. The longitudinal separations obtained between the Swarm passes and the ground site were often , and the magnitude of the in situ perturbations were relatively low. Ionospheric irregularities tend to be magnetic field aligned (Ossakow, 1979; Kil and Heelis, 1998; Nishioka et al., 2008; Kelley, 2009); therefore, Swarm may encounter irregularities of relatively small magnitudes in situ, while JULIA and ionosonde do not identify any events, for a wider longitudinal offset of a pass from the ground site.
Zakharenkova et al. (2016) showed two cases of Swarm passes over JULIA: one case where Swarm A encountered ionospheric irregularities and JULIA recorded spread F and another case where Swarm B never registered an ionospheric irregularity and JULIA never recorded a spread F. The statistical results shown in Fig. 7 assert that Swarm B can also detect irregularities and plasma bubbles associated with plumes and spread F, although with more mismatches than for Swarm A and C. Swarm B recorded more mismatches than Swarm A and C due to the progressive temporal and altitudinal separation between Swarm B and Swarm A and C (Zakharenkova et al., 2016). Swarm B orbits at a higher altitude than Swarm A and C, and it crosses the same region later than Swarm A and C. Generally, a difference in the percentage occurrence in all categories is observed between Swarm A and C (Fig. 7), although they orbit at the same altitude above sea level. The large-scale longitudinal bubble structure is sometimes observed with the Swarm A and C satellites (Xiong et al., 2016); however, for small-scale irregularities, the 1.5∘ longitudinal separation between the satellites is too large for a significant correlation between them.
3.3.2 Local time and seasonal variation of ionospheric irregularities
Numerous studies have shown that ionospheric irregularities at low latitudes are a post-sunset phenomenon owing to the electrodynamics launched after sunset (e.g. Stolle et al., 2006; Lühr et al., 2014; Abdu et al., 2012). Here, we also compared the local time dependence of the occurrence of plasma plumes observed by the JULIA radar, spread F recorded by the ionosonde, and small-scale ionospheric irregularities encountered by Swarm for different seasons. Figure 8 shows the percentage occurrence of plasma plumes as a function of local time and height grouped into different seasons: December solstice, June solstice, March equinox, and September equinox.
To obtain the results presented in Fig. 8, ground-based JULIA SNR data for the years from 2014 to 2018 were used. To eliminate the impact of geomagnetically disturbed conditions on the statistical outcomes, the data were filtered and only those recorded during quiet geomagnetic conditions (Kp ≤3) were taken into account. The JULIA data accumulated for the years from 2014 to 2018 were sufficient for examining the seasonal variation. Therefore, the seasonal dependence of the local time distribution of JULIA observations of ionospheric irregularities was also examined by grouping all of the data into different seasons corresponding to the March equinox (February–March–April), the June solstice (May–June–July), the September equinox (August–September–October), and the December solstice (November–December–January). For each local time–height bin, the percentage occurrence was obtained by dividing the number of observations with SNR>10 dB by the total number of observations (e.g. Smith et al., 2016).
It is visible from Fig. 8 that the plasma plumes only occurred at night. Figure 8 shows the occurrence of irregularities in plasma plumes starting at about 19:00 LT that generally last past midnight. This observation is similar to those of previous studies (e.g. Kil and Heelis, 1998; Hysell and Burcham, 2002; Smith et al., 2016). The observed plasma plumes are connected with the non-linear development of the RTI, which is initiated at the bottom of the F region (Woodman and La Hoz, 1976; Huang, 2018). The highest percentage occurrence takes place at the December solstice and the equinoxes. The lowest percentage occurrence is observed at the June solstice. The daily variations in the vertical plasma drift measured by the ISR were used to better understand the seasonal patterns observed in Fig. 8. Figure 9 presents the local time variation of the F-region vertical drift velocity for the years from 2014 to 2018.
From Fig. 9, the PRE of the vertical plasma drifts can be seen around the sunset hours (between 17:00 and 20:00 LT) before its reversal. Figure 9 shows the highest PRE peak during the December solstice and equinox seasons, whereas the PRE peak is the lowest at the June solstice. Similar observations were made by Smith et al. (2016). Comparing the results presented in Fig. 9 with the local time distributions presented in Fig. 8, it follows that a high occurrence of post-sunset topside spread F is associated with enhancements of the PRE peak. A high PRE implies significant E×B vertical drifts that boost the rate of RTI growth (Sultan, 1996; Fejer et al., 1999). The PRE moves the ionospheric F layer to higher altitudes where there is less interaction between ions and neutrals. The decreased interaction between ions and neutrals leads to increased RTI (Jayachandran et al., 1993; Kelley, 2009).
Figure 8 also shows a relatively high occurrence of irregularities after midnight, especially at the solstices and the September equinox. Similar observations were made by Hysell and Burcham (2002) and Smith et al. (2016). The extension of the occurrence of plumes post-midnight may be due to the late reversal time and small post-reversal electric fields (Hysell and Burcham, 2002). Despite the use of low-power transmitters, the JULIA radar can also detect weak post-midnight irregularities, particularly during the solstice seasons (as shown in Fig. 8). However, the detected post-midnight ionospheric irregularities often exist at much lower altitudes than those presented by Smith et al. (2016). Using Jicamarca radar measurements, Fejer et al. (1999) reported that the ionospheric irregularities that occur after midnight are typically well-formed structures that can be connected to the disturbed dynamo.
Figure 10 shows the QF indices derived from ionosonde observations as a function of local time and month. To obtain the results presented in Fig. 10, ground-based ionosonde data for the years from 2014 to 2018 were used. These data were also filtered, and only those recorded during quiet geomagnetic conditions (Kp ≤3) were considered.
Considering that equatorial ionospheric irregularities are night-time phenomena, we only present QF data from 18:00 to 06:00 LT in Fig. 10. To generate Fig. 10, the QF data were averaged over 0.1 h local time bins for each month (y axis). Figure 10 shows that the QF index was high in the post-sunset period with peak values occurring between about 20:00 and 00:00 LT at the December solstice and the equinoxes. The high QF values at the equinoxes and the December solstice are most likely due to the RTI, which is usually triggered at the bottom side of a rising equatorial F layer. The rate of growth of the RTI depends on the meridional wind and the eastward electric field PRE determined by the longitudinal gradient of the flux-tube-integrated conductivity (Sultan, 1996; Basu, 2002). At the June solstice, the QF values were small after sunset, as seen in Fig. 10. Generally, Fig. 10 shows moderate QF values lasting until local midnight or longer (similar to the trend presented in Fig. 8). The low post-sunset QF values at the June solstice can be attributed to the small PRE, which can also be seen in Fig. 9c.
Figure 11 shows the QLat–LT distributions of std(ΔNe) for the Swarm satellites for the years from 2014 to 2018. Recall that the Swarm passes were allowed to be within magnetic longitude. The Ne data collected for the 5 years were also grouped into different seasons similar to those presented in Fig. 8. The results presented in Fig. 11 were also generated considering only the geomagnetically quiet conditions (Kp ≤3). The std(ΔNe) was then calculated in bins of h resolution in QLat and local time. The occurrence rate of ionospheric irregularities does not always correspond to the highest amplitude of ionospheric irregularities (Wan et al., 2018). Therefore, we presented the calculated std(ΔNe) per bin as a function of QLat and local time, as seen in Fig. 11. From Fig. 11, high std(ΔNe) values frequently occurred between about ±10 and QLat, i.e. at the approximate location of the EIA belts. The distribution of the std(ΔNe), as seen in Fig. 11, is essentially symmetrical about the quasi-dipole equator. The symmetrical distribution about the magnetic equator has also been observed in earlier studies (e.g. Stolle et al., 2006; Carter et al., 2013; Wan et al., 2018); this confirms that equatorial ionospheric irregularities usually extend along the magnetic field lines in the northern and southern directions, and they are concentrated at the EIA belts (Kelley, 2009). The std(ΔNe) attained a maximum between 20:00 and 22:00 LT. A decrease was detected after 22:00 until 06:00 LT. The local time distribution of std(ΔNe) for Swarm A, B, and C is the same as that of the quiet-time F-region echoes presented in Fig. 8 and the QF distribution presented in Fig. 10. The distribution of std(ΔNe) shown in Fig. 11 has peak values at local times and QLat ranges where the RTI is expected. In terms of seasons, as observed from Fig. 11, high values of std(ΔNe) were seen at the equinoxes and the December solstice, whereas the lowest values were detected at the June solstice. This is similar to the seasonal dependence of quiet-time F-region echoes presented in Fig. 8. In Fig. 11, Swarm hardly encountered post-midnight irregularities while orbiting over South America during all seasons. In Fig. 8, it is observed that the post-midnight plumes often existed at lower altitudes at the solstices and the September equinox. Therefore, the low post-midnight ionospheric irregularity observations by Swarm may be because the plumes failed to reach Swarm altitudes.
For comparison, Fig. 12 shows the quasi-dipole versus local time distribution of ionospheric irregularities based on the Swarm Ionospheric Bubble Index (IBI), which is a standard Level 2 product of the Swarm mission (Park et al., 2013). The IBI provides information on the climatology of ionospheric irregularities and the level of magnetic field disturbance by taking both the electron density and magnetic field measurements into account (Park et al., 2013; Wan et al., 2018). It is important to note that the IBI is has a value of 1, 0, or −1 for bubble detected, not detected, or undetermined respectively. Therefore, to generate the results in Fig. 12, the data sets were first grouped into different seasons corresponding to the March equinox, the June solstice, the September equinox, and the December solstice. For each season, the data were then binned into h quasi-dipole latitude–local time bins. For each quasi-dipole latitude–local time bin, the percentage occurrence was obtained by dividing the number of observations with an IBI of 1 by the total number of observations. The binned percentage occurrence of an IBI of 1 shown in Fig. 12 has similar seasonal characteristics as the in situ irregularities shown in Fig. 11. The percentage occurrence of an IBI of 1 ranges from 0 % to 20 % which is relatively low. The low percentage occurrence of ionospheric irregularities derived from the IBI was also observed by Wan et al. (2018). This may be because the magnitude of ionospheric irregularities must be large enough to cause magnetic field fluctuations (Wan et al., 2018). The latitudinal profile of std(ΔNe) and the percentage occurrence of an IBI of 1 have peaks near the anomaly crests (about QLat). The diamagnetic effect in fluctuations of Ne are believed to be the cause of an IBI of 1, and this occurs at the anomaly crests (Stolle et al., 2006; Lühr et al., 2003).
The Bragg condition for the JULIA radar implies that the coherent spread echoes are from density variations at about a 3 m wavelength (Kelley, 2009). The Bragg condition for backscatter means that a radar can only observe structures in the refractive index with a size close to the half radar wavelength (Kelley, 2009; Hocking et al., 2016). The Swarm electron density measurements used in this study are limited by a sampling rate of 16 Hz and an orbital velocity of about 7.5 km s−1 to wavelengths of about 500 m and longer respectively. The good correlation between the Swarm measurements at these wavelengths and the spread echoes from Swarm altitudes suggest that the irregularities seen by Swarm occur over a spectrum of different wavelengths, at least from about 500 m down to the radar wavelength of 3 m. A non-linear decay of unstable waves could explain this. In addition, we expect that the radar signal could be affected by scintillations which are particularly known from one-way signal propagation such as in Global Navigation Satellite System (GNSS) and VHF satellite beacons (Burke et al., 2003; Zuo et al., 2016). For the radar, this could be relevant for echoes where the Bragg reflection occurs at high altitudes, above Swarm. Fresnel theory shows that wavelengths at the Fresnel scale of are most relevant for causing scintillations. Here, λ is the wavelength (3 m for the JULIA radar), and d is the distance from the perturbation to the receiver (445–510 km for Swarm). This gives a Fresnel scale between about 1.6 and 1.7 km. The Swarm measurements generally indicate that irregularities at such scales are present near the paths of Bragg-reflected radar signals. Therefore, we suggest that spread-F signals may, at times, be a result of both the Bragg backscattering at the highest altitude and scintillations of the radio waves to and from the scatter region.
In this paper, the results of a study of equatorial ionospheric irregularities detected by the JULIA radar and ionosonde in comparison with in situ Ne measurements made by Swarm for the years from 2014 to 2018 was presented. Cases of coincidence between Swarm, JULIA, and ionosonde observations were discussed. Moreover, the JULIA, ionosonde, and Swarm observations were examined statistically during geomagnetically quiet conditions. The local time and seasonal statistical patterns obtained from JULIA, the ionosonde, and Swarm were explained using drift measurements by the ISR.
Results based on the JULIA radar and the ionosonde agreed with the plasma density obtained from measurements of the Swarm faceplate for single satellite passes over or near the JRO. Based on an on–off classification, in the majority of cases, when the JULIA radar detected topside plasma plumes, Swarm also observed plasma bubbles when its trajectory crossed directly overhead or near the JRO. This was also true for the ionosonde measurements. A few exceptions were also observed when the JULIA radar and the ionosonde detected the presence of plasma structures, whereas Swarm did not record any bubbles and vice versa. For the case when JULIA and the ionosonde recorded irregularity signatures whereas Swarm observed no structures, the plume structures may not have ascended to Swarm altitudes by the time the satellites passed over Jicamarca or the satellites may simply have been in a different location. Swarm was able to detect ionospheric irregularities in situ, whereas no signature was recorded on the ground simply because the irregularities occurred at magnetic longitudes that were largely offset from the longitude of the ground site. Statistical differences between Swarm A and C were observed, and these were attributed to the 1.5∘ longitudinal separation between them which becomes significant for small-scale irregularities.
The three phenomena, namely plasma plumes observed by the JULIA radar, spread-F signatures recorded by the ionosonde, and small-scale irregularities detected by Swarm, revealed similarities in the patterns of occurrence based on the local time and different seasons. The highest occurrence rate was observed at the December solstice and at the equinoxes, whereas a low occurrence rate was observed at the June solstice. Measurements of the vertical plasma drift, made by the ISR, were used to understand the seasonal dependence of the occurrence of topside spread F and in situ density irregularities. The seasonal dependence of the occurrence of topside spread F and in situ Ne irregularities can be explained by the extent to which plasma is drifted vertically upwards.
The 5 year Swarm faceplate Ne data set has revealed a lot of detailed features regarding the electron density variations associated with plasma bubbles. In situ measurements of Ne by Swarm are a promising tool to indicate the likelihood of plasma plumes and spread-F occurrence at times and locations where radar or ionosonde measurements are not available. The geometry, however, is an important factor; therefore, when determining whether satellite observations are valid or accurate for any given ground site, algorithms should take the position of the satellite and the apex height of the magnetic field lines into account.
The official Swarm website is http://earth.esa.int/swarm (last access: 30 September 2020, ESA Earth Observations, 2020), and ftp://swarm-diss.eo.esa.int (last access: 30 September 2020, IRF, 2020a) is the server for the distribution of Swarm data. The IBI measurements used in this study can be obtained from https://swarm-diss.eo.esa.int/#swarm%2FLevel2daily%2FLatest_baselines%2FIBI (last access: 30 September 2020, IRF, 2020b). The radar measurements used in this study can be obtained from the Madrigal database at http://jro.igp.gob.pe/madrigal/ (last access: 30 September 2020, Jicamarca Radio Observatory, 2020). The Kp index values used in this study were obtained from http://omniweb.gsfc.nasa.gov/ (last access: 30 September 2020, Space Physics Data Facility, 2020). The SAO Explorer software was obtained from http://ulcar.uml.edu/SAO-X/SAO-X.html (last access: 30 September 2020, UMLCAR, 2020).
The ideas presented in this paper were designed and implemented by AS, SB, EJ, and MM. AS prepared the paper with contributions from all the co-authors.
The authors declare that they have no conflict of interest.
This study was financially supported by the International Science Programme (ISP) of the Uppsala University, Sweden, and by the Jicamarca International Research Experience Program (JIREP, http://www.igp.gob.pe/convocatorias/jirep) of the Instituto Geofísico del Perú with support from the US National Science Foundation (NSF). The authors acknowledge the European Space Agency's Swarm team for the Swarm mission. We also acknowledge the anonymous referees for their insightful comments which significantly improved the quality of this paper.
This research has been supported by the International Science Programme of the Uppsala University, Sweden (grant no. UGA 02) and the Jicamarca International Research Experience Program (NSF grant no. AGS-1732209).
This paper was edited by Keisuke Hosokawa and reviewed by two anonymous referees.
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