Magnetic Field Gradient Across the Flank Magnetopause

1 Introduction

The magnetopause is a current sheet forming the boundary between the magnetic pressure of the Earth’s dipole on the one side and the shocked supersonic solar wind with an embedded interplanetary magnetic field (IMF) on the other side. However, the total pressure even at the subsolar magnetopause is not exactly equal to the solar wind dynamic pressure (e.g., Spreiter et al., 1966; Samsonov et al., 2012), and the total magnetospheric magnetic field is a superposition of the magnetic field of the Earth’s dipole field and the field of several magnetospheric current systems (e.g., Tsyganenko and Andreeva, 2015). Since the magnetopause position is given by the total pressure balance of plasmas and fields on either side, the magnetopause is constantly moving back and forth due to solar wind pressure variations at all timescales. The motion is controlled by a combination of direct solar wind variations (predominantly by changes in the solar wind dynamic pressure) and surface waves such as Kelvin-Helmholtz (Haaland et al., 2019). At the flanks, the latter probably plays a larger role because some theories (e.g., Kavosi and Raeder, 2015; Fadanelli et al., 2018) suppose that waves are excited by local instabilities at the dayside and propagate toward the flanks. At present, there does not seem to be a clear consensus about whether surface waves are more frequent on the dawn or dusk flanks; nevertheless, a dawndusk asymmetry of the macroscopic parameters was a subject of the study by Haaland et al. (2020), and they found, based on MMS data, that the dawn magnetopause is thicker than at dusk, while the dusk flank is more dynamic, with a higher average normal velocity.

The magnetopause is one of the most complex boundaries in space because its formation involves electrical currents, gradients of the plasma density and pressure, flow shear, and/or anisotropy of velocity distributions of particles (Němeček et al., 2020). Therefore, different forms of free energy are accessible at and around the magnetopause, and a variety of instabilities such as current-driven (e.g., magnetic reconnection (Paschmann et al., 1979; Sonnerup et al., 1981)), flow shear-driven (e.g., nonlinear Kelvin-Helmholtz waves (Hasegawa et al., 2004, 2009)), and/or anisotropy-driven (e.g., mirror) instabilities can be excited there (Hasegawa, 2012), but also diffusion (e.g., Treumann et al., 1995) and impulsive penetration (e.g., Lemaire et al., 1979) have been suggested to enable transport across the magnetopause. In addition, the magnetopause is curved on a large scale, and thus, when the upstream flow is super-magnetosonic, it is exposed to a highly time-varying and inhomogeneous plasma of the magnetosheath, the region of a shocked solar wind situated between the magnetopause and bow shock (Berchem and Russell, 1982). Moreover, when the magnetopause thickness is comparable to (or less than) the ion Larmor radius, the boundary structure could also be affected by kinetic effects (Cai et al., 1990; Nakamura et al., 2010).

Due to the focus on processes responsible for the transfer of momentum and energy across the magnetopause and the associated impact on magnetospheric dynamics, much attention has been paid to the dayside magnetopause near the SunEarth line. The interaction between the IMF and geomagnetic field at the dayside magnetopause has a direct consequence on the large-scale plasma circulation in the magnetosphere and magnetically connected ionosphere. The magnetopause flanks and possible dawndusk asymmetries have received less attention, partly because interactions along the flanks probably have a smaller effect on the geomagnetic activity and partly due to results of observations in this region which demonstrate a small difference of boundary layer characteristics between dayside and flanks. A study of Artemyev et al. (2017) showed that plasma and magnetic field characteristics are very similar for boundary layers observed at the lunar orbit ($\approx 55R_E$) and farther downtail as far as $\approx 200R_E$ and that the dynamical magnetosheath pressure does not contribute to the pressure balance across the boundary layer at these distances. Furthermore, Lukin et al. (2020) compared the characteristics of magnetic field and plasma populations during simultaneous magnetopause crossings, which are separated by about 50 R_E (dayside vs night sides), and found that the magnetosheath current sheet profiles are similar at these two locations. Nevertheless, a flank magnetopause configuration and dynamics are critical for understanding the transport of magnetosheath plasma toward the magnetotail (Wing et al., 2014; Haaland et al., 2019).

Němeček et al. (2002), Zastenker et al. (2002), and Šafránková et al. (2002) compared the magnetosheath measurements with calculations using the Spreiter gasdynamic models of the magnetosheath plasma flow (Spreiter et al., 1966) and IMF modification (Spreiter and Stahara, 1980). They have shown that an average behavior of magnetosheath parameters is predicted rather well by these models. However, they noted that large variations of the ion flux and magnetic field magnitude in the magnetosheath are not always predicted by these models because their variations originated in the magnetosheath itself (or in the foreshock). Such structures are moving tailward along the magnetopause together with the plasma flow (Shevyrev et al., 2003). A suggested explanation for these structures (using the similarity of plasma and magnetic field variation levels) is that they are created near the bow shock as compressional waves.

On the sunward side, the Earth’s magnetic field has mainly compressed dipolar structure, whereas the field is stretched out and forms the magnetotail that consists of the northern and southern lobes separated by the plasma sheet on the night side. Due to lower densities and temperatures in lobes than in the plasma sheet, a force imposed on the magnetotail toward its center is balanced by the plasma pressure in the plasma sheet (Coroniti and Kennel, 1972). While the pressure equilibrium exists most of the time, the plasma sheet can also be highly dynamic because the lobes and plasma sheet store energy, which is often released in explosive events during substorms and storms (McPherron et al., 2011).

Both the solar wind and ionosphere can be sources of the plasma sheet plasma. Wing et al. (2014) and later Kistler (2020) have summarized knowledge on the solar wind entry and transport to the plasma sheet for different IMF orientations. Generally, during a northward IMF, the plasma sheet ion spectrum is well-described by two populations. The colder component ($<\approx 1\mathrm{k}\mathrm{e}\mathrm{V}$) is identified as being the solar wind origin because it is only slightly hotter than in the adjacent magnetosheath plasma. This cold and dense plasma sheet occurs after several hours of northward IMF and is observed predominantly along the flanks and at high magnetic latitudes (e.g., Fujimoto et al., 1998) as a result of double cusp or lobe reconnection at the dayside (e.g., Song and Russell, 1992; Sandholt et al., 1999; Lavraud et al., 2006) or enters from the flanks through Kelvin-Helmholtz instability (Sorathia et al., 2019). According to Yu et al. (2020), the cold and dense plasma sheet probably contributes to the production of storm-time energetic particles (Borovsky et al., 1997) and can result in stronger ring currents during the main phase of storms (e.g., Lavraud et al., 2006) and can also lead to the mass loading of the magnetotail. Therefore, it may have effects on substorms (e.g., Fu et al., 2012) and reduction of the reconnection rate (e.g., Toledo-Redondo et al., 2016).

On the other hand, the source of the hotter component ($>\approx 3\mathrm{k}\mathrm{e}\mathrm{V}$) could either be from the ionosphere or from the solar wind plasma that enters farther down the tail and is heated during its transport; however, the cusp entry leads also to a hotter population. The ionospheric plasma has access to the plasma sheet through ion outflow over a wide range of energies that occur throughout the auroral oval and in the polar cap (Li et al., 2013). In the polar cap, the ion escape is mainly due to the ambipolar electric field, and in the auroral regions, local wave acceleration energizes ionospheric plasma to higher energies. During storms, O⁺ from both the nightside auroral region and dayside cusp regions enters the plasma sheet (Kistler et al., 2019). Statistical studies have shown that the O⁺ content in the plasma sheet increases with both geomagnetic activity (Kp) and solar EUV (F10.7) (Mouikis et al., 2010), and investigations of the storm-time ring current (e.g., Mouikis et al., 2019) have identified a significant fraction of the energy density that is carried by O⁺, indicating the importance of the ionospheric source. Němeček et al. (2016) studied the influence of these effects on the magnetopause location and showed that increased ionospheric conductivity leads to its inward motion.

During southward IMF conditions, reconnection occurs at the magnetopause on the dayside at low latitudes. The cold and dense plasma can also be observed along both flanks, but the density is smaller than during northward IMF. Thomsen et al. (2003) and Lavraud and Jordanova (2007) investigated the transition when a period of northward IMF is followed by a strongly southward IMF, driving a storm. They have suggested that this dense plasma can load the near-Earth plasma sheet and then get driven into the inner magnetosphere when the IMF turns southward, creating a strong ring current. This would imply that at least at the beginning of a storm, the ring current is formed by solar wind plasma (Kistler, 2020).

Magnetic pressure inside the magnetopause is usually balanced with a sum of thermal plasma pressure and magnetic pressure on the magnetosheath side, but at about 9% of magnetopause crossings, the THEMIS spacecraft encounter the situation when the magnetosheath magnetic field is larger than that in the magnetosphere, and therefore, the enhanced pressure from the magnetosheath side seems to be uncompensated. We call this effect an inverse magnetic gradient across the magnetopause. We investigate the magnetic gradient across the magnetopause and discuss conditions favorable for the creation of an inverse magnetic gradient. An extensive statistical study reveals a large southward IMF in connection with enhanced geomagnetic activity as necessary conditions.

2 Data Processing

The analysis is based on observations of all THEMIS probes (Angelopoulos, 2008) and covers a half of the solar cycle (2007–2017). The available plasma (McFadden et al., 2008a) and magnetic field (Auster et al., 2008) data were surveyed by an automated routine based on a determination of scanned regions (solar wind, magnetosheath, and magnetosphere). The identification of regions is based on ion and electron densities and temperatures and magnetic field strength. We are using spin resolution ground moments whenever available, otherwise we apply the onboard moments. The solar wind parameters from the OMNI database were lagged on the expected propagation time from the bow shock nose. The identification method is analogous to that suggested by Jelínek et al. (2012), but it is applied on the search for individual magnetopause crossings.

The routine provided about 36,000 magnetopause crossing candidates. We have calculated the location predicted by the Lin et al. (2010) model for them, and all candidates exhibiting difference between predicted and observed distances from the Earth larger than 1.5 R_E were checked by a visual inspection of corresponding plots of the plasma and magnetic field, and events under doubt were discarded. The set includes single crossings as well as a series of multiple crossings that were usually observed close to the apogee of a particular spacecraft. The visual inspection left 34,699 crossings for a further processing.

The time and location of each crossing were complemented with the upstream magnetic field and plasma parameters. We are using wind data lagged on the expected propagation time as a proxy of upstream conditions. Five-minute averages of the spin resolution magnetic field strength, B_MSH, the ion density, N_MSH, velocity, V_MSH, and ion temperature, T_MSH, measured by THEMIS just outbound the magnetopause in the magnetosheath and the magnetic field strength just inbound the magnetopause, B_MSP, were added for the later processing. In order to account for the uncertainty of the identification of the exact time of magnetopause crossings by our automated routine, we have skipped 1 min on both sides of a particular crossing.

3 Magnetic Gradient Across the Magnetopause

A distribution of THEMIS crossings projected onto the XY GSM plane is shown in the top left panel of Figure 1. Note that we limited our study to X_GSE > − 5 R_E because the number of crossings behind this limit is very low. We also did not analyze crossings observed by THEMIS B and C at the lunar orbit because the magnetopause is formed in a different way at these distances. Whereas the ram pressure of the solar wind is principal for the formation of the dayside magnetopause, the solar wind flow is nearly parallel with the magnetopause at far flank locations. We have further divided the crossings into three subsets according to the angle, α, between the radius vector and X-axis: subsolar (|α| < 30°), near flank (30° < |α| < 60°), and distant flank (|α| > 60°) that are distinguished by colors in Figure 1. We further selected events satisfying a condition B_MSH/B_MSP > 1 that are a dominant subject of the present study. They are indicated by blue crosses, and their number is sufficient to exclude a possibility that they can be attributed to measuring errors. We can note that a relative number of these crossings increases toward the flanks with no apparent dawndusk asymmetry. For this reason, we combine data from dawn and dusk sectors in further analysis.

FIGURE 1

FIGURE 1. Left—Projections of observed magnetopause crossings onto the X–Y plane. Colors indicate a division of crossings into particular subsets (subsolar—yellow, near flank—green, distant flank—red). The crossings exhibiting B_MSH > B_MSP are shown as blue crosses. Right—Distributions of differences between observed R_obs and modeled R_mod (Lin et al., 2010) magnetopause stand-off distances for the subsets of crossings with B_MSH/B_MSP < 1 (green) and B_MSH/B_MSP > 1 (red). Bottom—Dependence of the B_MSH/B_MSP ratio on the angle α between the radius vector of a particular crossing and the X-axis.

A portion of events exhibiting an inverse magnetic gradient is illustrated in the bottom panel of Figure 1, where the B_MSH/B_MSP ratio is plotted as a function of α. The gray crosses stand for individual crossings, and the red bars show medians in the angle bins. We can see that this median is about constant and equal to $\approx 0.65$ in the subsolar region and then starts to increase toward unity at flanks, but it does not reach the blue dashed line standing for B_MSH/B_MSP = 1. These observations are quantified in Table 1. The first row in the table presents the number of events in |α| subsets that decrease toward the flank because an apogee of the THEMIS A, D, and E spacecraft is insufficient to cross the flank magnetopause when the solar wind pressure is low. On the other hand, the number of crossings satisfying a condition of B_MSH > B_MSP increases with increasing α and reaches 25% of all crossings in the far flank region.

TABLE 1

TABLE 1. Longitudinal distribution of the magnetopause crossings projected onto the equatorial plane.

The top right-hand panel in Figure 1 shows the distribution of differences between observed and modeled magnetopause stand-off distances. We have checked several empirical magnetopause models, but we decide to use the Lin et al. (2010) model because it explicitly contains the effect of the IMF strength on the magnetopause location. The histograms are plotted for B_MSH < B_MSP (green) and B_MSH > B_MSP (red) events separately. One can note that B_MSH > B_MSP events are generally located closer to the Earth than the “standard” events with a larger magnetic field on the magnetospheric side. We also plotted similar histograms for our subsets and fitted them with Gaussian distributions. The parameters of distributions (full width at half maximum (FWHM) and center) are surveyed in Table 2.

TABLE 2

TABLE 2. Distributions of differences between observed R_obs and modeled R_mod magnetopause stand-off distances. Parameters of Gaussian fits (center and FWHM) are given for three magnetopause regions.

Table 2 shows that the Lin et al. (2010) model describes the position of the magnetopause rather well, and the deviations of model locations from observations are lower than 0.2 R_E with an exception of the near-flank region. The shift of crossings with B_MSH/B_MSP > 1 toward the Earth by about 0.2 R_E can be observed in all regions. Since B_MSH is actually IMF compressed at the bow shock and the IMF strength is included in the model, it indicates that the effect of the IMF strength on the magnetopause location is not limited by the pressure but influences the whole interaction process. On the other hand, we can see only a slight enlargement of the prediction uncertainty described by FWHM for the crossings with B_MSH/B_MSP > 1, but we are operating with a small number of events (Table 1) for an ultimate conclusion.

3.1 Upstream Conditions

The previous section has shown that the observations of an inverse magnetic gradient across the magnetopause are rather frequent; the probability of its observations increases with the distance from the subsolar point and reaches nearly 25% at the terminator. In search for the conditions favorable for its formation, we started with an analysis of upstream conditions. We have plotted distributions of the ion density, velocity, and dynamic pressure separately for events with B_MSH > B_MSP and B_MSH < B_MSP, but we did not find any systematic difference among them, thus we are not showing these plots. The only clear dependence of B_MSH/B_MSP on upstream conditions was found for the IMF strength and IMF cone angle (the angle between the IMF and solar wind velocity vectors) as Figure 2 demonstrates.

FIGURE 2

FIGURE 2. B_MSH/B_MSP ratio as a function of the IMF strength (left) and IMF cone angle (right). The gray points mark all MP crossings, and the color bars stand for median values of B_MSH/B_MSP in particular subsets of crossings. Color coding is explained in the top left corners.

The gray points stand for values corresponding to individual crossings, and color bars show medians in IMF or cone angle bins for the subsolar (yellow), near flank (green), and distant (red) flank. Consistently with the bottom panel in Figure 1, the median B_MSH/B_MSP ratio increases with the distance from the subsolar point, but the left panel shows that it also increases with an increasing IMF strength (left panel) in a monotonic way, and it exceeds unity even in the subsolar region if the IMF strength is sufficiently high. We should note that we made plots like those in Figure 2 for the IMF B_Y and B_Z components, and the results were similar to the B_MSH/B_MSP dependence on the IMF strength.

The clear increase of B_MSH/B_MSP with the cone angle (right panel) starts at about 30° in all magnetopause segments. It is hard to say whether a little larger median ratio observed for a nearly radial field is the real physical effect or a product of limited statistics in this cone angle bin. Nevertheless, it is observed in all three magnetopause regions. The number of points above the blue dashed line (events exhibiting the inverse gradient) increases with the cone angle, but the medians are below unity in all magnetopause segments.

A larger value of the B_MSH/B_MSP can be caused either by too large B_MSH or too low B_MSP. Let us first check B_MSH that is actually a compressed IMF. The left-hand panel in Figure 3 shows B_MSH as a function of the IMF strength. The format and color coding are the same as in the previous figures; the full colored bars are medians in IMF bins, and the dotted colored bars present medians computed for events with B_MSH > B_MSP. All individual points as well as all medians roughly correspond to a compression factor of about 4 that is consistent with IMF compression at the supercritical quasi-perpendicular bow shock (Spreiter and Stahara, 1980). Since the red medians in each IMF bin are the lowest, we can conclude that the compression factor decreases with the distance from the subsolar point that is consistent with early magnetosheath models (Spreiter and Stahara, 1980). Comparing the medians computed from all data (full lines) and medians corresponding to events with B_MSH > B_MSP (dotted lines), we can note that both medians are about equal at the distant flank (red). It means that 1) the number of events with B_MSH > B_MSP prevails and 2) the inverse gradient is not connected with an enhanced IMF compression in this region. The same is true for the near-flank (green) events with an exception of IMF below 5 nT, and thus, we can conclude that the formation of an enlarged magnetic gradient across the flank magnetopause is not connected with larger than usual IMF compression at the bow shock.

FIGURE 3

FIGURE 3. Left—The magnetic field in the magnetosheath as a function of the IMF strength; right—the relation between observed B_MSP at the magnetopause and modeled magnetic field according to T89 at the same location. The color-coding follows Figure 2; the blue crosses stand for crossings with B_MSH/B_MSP > 1; the straight line in the right-hand panel signifies an identity of both fields.

In order to check the conditions in the magnetosphere, we have applied the Tsyganenko (1989) model (T89 model) of the magnetic field that takes into account variations of the geomagnetic activity and computed a prediction of the magnetic field strength at the point of each magnetopause crossing. The model is parameterized with the Kp index that covers geomagnetic activity in a broad range of latitudes, and thus, it would reflect the influence of the ring current as well as auroral electrojects on the magnetospheric magnetic field. A comparison of observed and predicted magnetic fields is shown in the right-hand panel in Figure 3. Since the model is relatively simple and does not include the influence of upstream conditions on the magnetospheric field, the spread of points is rather large, but the medians shown by colored bars lie approximately on the black line that signifies the identity of the predicted and measured magnetic fields. It is especially true at the small fields at flanks (green and red bars) where a great majority of events with B_MSH > B_MSP (blue crosses) were observed.

3.2 Geomagnetic Activity

A combination of conclusions following from the previous figures with the fact that the magnetopause is only slightly compressed (Figure 1) suggests that the excess of the magnetic pressure on the magnetosheath side would be compensated by the plasma pressure on the magnetospheric side and thus a link with the geomagnetic activity. In order to check it, the B_MSH/B_MSP ratio as a function of two basic geomagnetic indices, SYM-H and AE, is shown in Figure 4.

FIGURE 4

FIGURE 4. B_MSH/B_MSP ratio as a function of SYM-H (left) and AE (right) indices of the geomagnetic activity. The color bars follow the coding in Figure 2.

Since the THEMIS orbits cover predominantly the low-latitude magnetopause, SYM-H seems to be more appropriate, and the medians shown by color bars in the left panel reveal that the B_MSH/B_MSP ratio is about constant and does not depend on a value of the index if the magnetosphere is quiet (SYM-H $>-30nT$), but it increases with increasing geomagnetic activity. The same conclusion follows from the right-hand panel that presents a dependence of B_MSH/B_MSP on the AE index. It is interesting to note that although THEMIS moves basically in the low-latitude magnetopause, the correlation of the AE index describing the auroral activity with the B_MSH/B_MSP ratio is slightly larger (0.17) than that with SYM-H index (0.12) that is predominantly affected by ring current changes, thus processes at low latitudes.

A combination of Figures 2–4 suggests that the conditions for the creation of an inverse magnetic gradient across the flank magnetopause are large IMF dominated by perpendicular (B_Y and B_Z) components and/or enhanced geomagnetic activity. An additional analysis has shown that the correlation of the B_MSH/B_MSP ratio with IMF B_Z is 0.43 while it is only 0.30 for IMF B_Y, and thus, we focus on SYM-H, AE, and IMF B_Z. To find which of these factors are more important, Figure 5 combines these parameters.

FIGURE 5

FIGURE 5. B_MSH/B_MSP ratio in bins of IMF B_Z and SYM-H (left) or AE (right) indices. The color scale shows median values of the ratio in a particular bin, and a number of events in a particular bin are given inside the bin. Note that only crossings of the flank magnetopause (green and red sectors in Figure 1) are used.

We binned data into 2 nT wide bins of IMF B_Z and then into 25 nT wide bins of SYM-H (left panel) and 200 nT wide bins of AE (right panel), respectively. For each of these bins, we counted the number of events, and if it exceeded 5, we further calculated the median of the B_MSH/B_MSP ratio. The number of events is given in each bin, and the value of the B_MSH/B_MSP median is shown by color. To be more illustrative, we use discrete colors instead of a continuous color palette. The scale is shown on the right-hand side of each panel, and numbers stand for rounded medians.

A brief look at the panels of Figure 5 reveals that low B_MSH/B_MSP medians (blue color) require a combination of small IMF B_Z, regardless of its polarity, and a low geomagnetic activity. On the other hand, B_MSH/B_MSP > 1.1 (orange and red colors) can be observed nearly exceptionally during intervals of strong ($<-4$) negative IMF B_Z and enhanced geomagnetic activity. There are several exceptions from these rules in our statistics, but all of them are connected with a small number of events in the bins, and thus, their statistical significance is low. Although the analysis covers predominantly the magnetopause at low geomagnetic latitudes, it seems that auroral activity (AE index) is an important factor for the creation of an inverse magnetic gradient because it is observed always if AE > 1000.

3.3 Relation to Solar Wind Categories

Yermolaev et al. (2009) suggested a scheme for a classification of the solar wind into several categories. They use hourly averaged OMNI solar wind and IMF data and attribute each hour to one of nine solar wind types—slow wind (SLOW), fast wind (FAST), heliospheric current sheet (HCS), co-rotating interaction region (CIR), interplanetary coronal mass ejection that does not exhibit magnetic cloud features (EJECTA), magnetic cloud (MC), and two categories of interplanetary shocks (IS and ISA). Although the authors originally processed the 1976–2000 years, they continue with the classification till present, and a list of intervals attributed to mentioned categories are available at ftp://ftp.iki.rssi.ru/pub/omni/catalog/. Since the statistics presented in Figure 5 suggest a connection of an inverse magnetic gradient with geomagnetic activity, and solar wind geomagnetic effectiveness varies with the category, we have used their classification and checked a possible relation. The results are presented in Table 3. Note that we combined IS and ISA categories because the number of intervals in these categories was too low. Looking at Table 3, we can note that the occurrence rate of the inverse magnetic gradient agrees well with the results in Figure 5. It is not surprising because MCs are typical drivers of large geomagnetic storms, and they often bring a large southward IMF toward the magnetopause. On the other hand, standard upstream conditions (slow or fast solar winds) lead to the inverse gradient only exceptionally.

TABLE 3

TABLE 3. Statistics of inverse gradient observations under different solar wind driving. The first line shows a number of MP crossings under specified conditions, the second line marks a number of crossings exhibiting inverse gradient, and the third line, their ratio.

4 Summary of Statistical Results

We report a statistics of observations of the magnetic gradient across the dayside magnetopause with an emphasis on the situation when the magnetosheath magnetic field magnitude is larger than the field just inbound the magnetopause, i.e., B_MSH > B_MSP. Since this configuration contradicts to a general understanding of the magnetopause formation, we use the term inverse magnetic gradient for briefness. The statistics compare three regions—subsolar, near, and distant flanks. We can summarize our statistical findings as follows:

1. Median magnitudes of the B_MSH/B_MSP ratio are 0.65 at the subsolar region, 0.7 at the near flank, and 0.9 at the distant flank, respectively (Figure 1). The inverse gradient is observed more frequently across the flank magnetopause, and the occurrence rate strongly rises with the departure of the crossing local time from the noon; it is 1.5% in the subsolar region, 7% at the near flank, and 20% at the distant flank (Table 1).

2. A presence of the inverse magnetic gradient across the magnetopause is not exceptional because it is observed at about 9% of all magnetopause crossings. Moreover, the inverse magnetic gradient is a natural continuation of the trends of the B_MSH/B_MSP ratio dependence on factors such as the IMF strength, cone angle (Figure 2), and geomagnetic activity (Figures 4, 5).

3. The magnetosheath magnetic field strength corresponds to its upstream source (Figure 3); the compression ratio does not depend on the B_MSH/B_MSP value (not shown).

4. The magnetopause location is well predicted by the Lin et al. (2010) model; the crossings exhibiting the inverse magnetic gradient are observed slightly closer to the Earth than the model predicts (Figure 1; Table 1).

5. The B_MSH/B_MSP ratio $>1$ is observed for both polarities of IMF B_Z, but the occurrence rate and median values of this ratio are larger for southward IMF (Figure 5).

6. The inverse gradient is observed preferentially during intervals of an enhanced geomagnetic activity described by AE and SYM-H indices (Figure 5).

7. The inverse gradient is not connected with lower than average magnetospheric magnetic field strength just inbound of the magnetopause that is well modeled by the T89 model (Figure 3).

8. Correlation coefficients between the B_MSH/B_MSP ratio and B_MSP are 0.06 only, whereas it is 0.70 for B_MSH.

The preferential observations of the inverse magnetic gradient during enhanced geomagnetic activity are consistent with a classification of corresponding upstream conditions in Table 3—the largest probability of its creation occurs when the magnetosphere is affected by MCs, CMEs, or CIRs, and these structures are responsible for major geomagnetic storms (Richardson et al., 2021). The storm-time magnetosphere is characterized by an enhanced ring current that decreases the magnetic field at the Earth surface (SYM-H index becomes negative) and increases the magnetic field at the magnetopause. The enhancement of eastward and westward auroral electrojects during storm times leads to increase/decrease of the surface magnetic field described by AL/AU indices, and it again would lead to corresponding changes of the magnetic field strength at the magnetopause. Nevertheless, all these effects are implemented in the T89 model, and Figure 3 shows that the distribution of the measured magnetic field around the value predicted by a model does not depend on the B_MSH/B_MSP ratio. Moreover, a comparison of T89 predictions for Kp index 1 and 6 at different locations shows that the storm effect on the magnetic field at the magnetopause can be as large as + 10 nT in the near flank region, but it decreases to + 2 nT at the far flank, and these values cannot explain a presence of the inverse gradient because the storm currents increase B_MSP, but we observe B_MSH > B_MSP. Weigel (2010) argue that the solar wind density amplifies the geomagnetic response to the solar wind activity, but we did not find any notable effect of the upstream density on the formation of the inverse gradient; the correlation of the B_MSH/B_MSP ratio with the upstream density is only 0.08.

A common understanding of the pressure balance across the magnetopause is that the sum of magnetic and plasma pressures at the magnetosheath side is balanced by a stronger magnetic field in the magnetosphere, but we are discussing events with an excess of the magnetic pressure on the magnetosheath side. The fact that the magnetopause is approximately at the position predicted by the empirical model (Figure 1) suggests an enhanced contribution of the magnetospheric plasma to the total pressure in a comparison with typical conditions. However, determination of plasma parameters at the magnetopause is difficult because the boundary layers on both sides of the magnetopause often contain a mix of magnetosheath and magnetospheric populations (Němeček et al., 2015), and even low-energy plasma from a plasmasphere (McFadden et al., 2008b) can be observed at the magnetopause during storm-time intervals. For this reason, we will demonstrate the conditions leading to the creation of the inverse gradient for several cases.

5 Supporting Case Study

In accord with the above statistical study, we have chosen three events. First of them occurred during the geomagnetic storm under a strong southward IMF and represents a typical example of the inverse gradient, B_MSH ≈ 2.2 B_MSP. This event is contrasted with another crossing observed under similar conditions but with a standard gradient, B_MSH < B_MSP. The third example is a representative of a group of crossings exhibiting the inverse gradient under a northward IMF. The basic data for these three crossings are shown in three sections of Figure 6.

FIGURE 6

FIGURE 6. Examples of magnetopause crossings. Left—the crossing exhibiting a strong inverse gradient under southward IMF and enhanced geomagnetic activity (SYM-H $\approx -51nT$, AE ≈ 212 nT); right—the crossing with a standard gradient under southward IMF (SYM-H $\approx -6nT$, AE ≈ 162 nT); bottom—the crossing exhibiting an inverse gradient under northward IMF (SYM-H $\approx 3nT$, AE ≈ 30 nT). The panels in each section show from top to bottom: the IMF strength and components propagated from the wind; the magnetic field measured by THEMIS; the energy flux of energetic ions from the SST instrument; the ion energy flux from the ESA instrument; and the total pressure, P_TOT, (black) and its particular components: P_DYN (blue)—the dynamic pressure perpendicular to the model magnetopause surface, P_NKT (green)—a sum of ion and electron thermal pressures, and P_MAG (red)—the magnetic pressure. Note that P_NKT was computed from the ESA ground moments, and the contribution of SST represents less than 1% of the total pressure.

Comparison of the figure sections reveals that both magnetopause crossings observed under southward IMF exhibit relatively thick boundary layer characterized by staircase like (left-hand section) or smooth (right-hand section) transition of the B_Z component from the negative value in the magnetosheath to the positive value on the magnetospheric side and mixed plasma populations on both sides of the magnetopause. On the other hand, the northward IMF (bottom section) leads to a sharp MP crossing with abrupt changes of the ion density and temperature, as it can be seen in the bottom section of the figure. These features distinguish the flank and subsolar magnetopause because Němeček et al. (2015) presented statistically that a thick boundary layer is a consequence of cusp reconnection, and thus, it is formed by northward IMF.

The formation of the boundary layer at the low-latitude flanks for strong southward IMF is affected by the presence of dayside extension of the plasma sheet that is supplied by intensive reconnection. This reconnection increases cross-tail potential driving magnetospheric current systems that modify the magnetic field at the magnetopause. Enhanced current heats the magnetospheric plasma and brings new charge carriers to the boundary layer. As a result, the magnetospheric plasma pressure is enhanced, balances the magnetosheath magnetic pressure, and keeps the magnetopause in an equilibrium state in the southward events with inverse magnetic gradient. We plot the energy distributions of magnetospheric ions just inbound of the magnetopause in Figure 7 for events shown in Figure 6. The figure shows a merged ion energy flux distribution from ESA and SST analyzers. Although there is an energy gap between the two analyzers, one can see that the maximum of the ion energy flux is above the range of the ESA analyzer ($\approx 30\mathrm{k}\mathrm{e}\mathrm{V}$) for the blue distribution that belongs to the event exhibiting a strong inverse gradient (Figure 6, left-hand section).

FIGURE 7

FIGURE 7. Energetic distributions of the ion energy flux in the magnetosphere just inbound the magnetopause for events in Figure 6. The parts of distributions below 30 keV were determined from the ESA spectrometer and the high-energy parts from the SST detector.

Consequently, we can suppose that the temperature of the ion population is larger than that calculated as the moment of the ESA distribution, and it causes an apparent lack of the magnetospheric pressure demonstrated in the bottom panels in all sections of Figure 6. When the southward IMF is not so strong (right-hand section) of Figure 6, the magnetospheric currents are weaker, and density and temperature in the magnetosphere are lower (green distribution in Figure 7), and we observe a standard magnetic gradient across the magnetopause. This explanation expects a large cross-tail potential for events with the inverse magnetic gradient, and it is consistent with the PCN index being 7 mV/m for the example in the left section of Figure 6, whereas it is only 1.5 mV/m for the event with the standard magnetic gradient shown in the middle section.

The northward crossing (bottom section of Figure 6) exhibits a clear plasma depletion layer at the magnetosheath side (Zwan and Wolf, 1976) characterized by an enhancement of the magnetic field complemented with a density depletion in front of the magnetopause. Nevertheless, the magnetosheath magnetic field outside this layer is still larger than that in the magnetosphere in spite of the fact that the geomagnetic activity is low, and it was low within preceding 12 h. The pressure balance calculated using the plasma moments from the ion spectrometer shows a lack of the pressure in the magnetosphere (last panel), but, similarly to the southward event, the ion density and temperature are underestimated because the maximum of the ion distribution is at the upper edge of the spectrometer energy range (red curve in Figure 7). However, mechanisms leading to such hot and dense plasma in the magnetosphere layer adjacent to the magnetopause should be further investigated.

6 Conclusion

We present a statistical study of the magnetic field gradient across the magnetopause with an emphasis on the flank magnetopause and events when the magnetospheric magnetic field was lower than that in the adjacent magnetosheath. Based on the above discussion, we can believe that we understand the formation of magnetopause layers that can lead to an inverse magnetic gradient across the magnetopause for southward IMF. The intensive reconnection caused by a large southward IMF increases cross-tail potential driving strong magnetospheric currents that overheat the magnetospheric plasma and bring it to the magnetopause. The presence of such plasma leads to a diamagnetic effect (decrease of the magnetospheric magnetic field) and increases the plasma pressure on the magnetospheric side. We have shown that the intensity of these processes increases with the IMF strength, and thus, we can conclude that IMF strength influences the processes in the magnetosphere much more than we expected so far.

Data Availability Statement

Publicly available datasets were analyzed in this study. This data can be found here: http://cdaweb.gsfc.nasa.gov/

Author Contributions

The article is a result of efforts of all authors, and their particular contributions are as follows: Data processing—THEMIS, KG and JS; methodology, ZN; data analysis and interpretation, ZN and JS; software and visualization, KG and JS; original draft preparation, ZN; contribution to data interpretation and enhanced discussion, GP.

Funding

The work was supported by the Czech Science Foundation under Contract 21-26463S.

Conflict of Interest

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Publisher’s Note

All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors, and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.

Acknowledgments

The authors thank the Wind and THEMIS teams for the magnetic field and plasma data available via http://cdaweb.gsfc.nasa.gov/. They also thank professor Vitek for his continuous support.

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