The energization and subsequent vertical transport of H⁺, He⁺, and O⁺ ions from the high latitude ionosphere to the terrestrial magnetosphere has been an active area of research in the last several decades (Schunk and Raitt, 1980; Mukai et al., 1994; Schunk and Sojka, 1997; Daglis et al., 1999; Winglee et al., 2002; Nosé et al., 2005; Barakat and Schunk, 2006; Glocer et al., 2009; Garcia et al., 2010; Ilie et al., 2013; Ilie et al., 2015). However, the energization, circulation, and redistribution of N⁺, in addition to that of O⁺, has received less attention, even though several direct and indirect measurements (Bashir and Ilie, 2018; Bashir and Ilie, 2021) have confirmed that N⁺ plays a crucial role in the near-Earth plasma dynamics.

The first ionospheric measurements of upflowing nitrogen ions were reported as early as 1961 by the Sputnik III mission. The existing observational record spans six solar cycles and consists of measurements spanning a wide range of altitudes, from ∼ 200 km from the Sputnik III to millions of km from the WIND mission. Figure 1 compiles the temporal and spatial coverage of these measurements, along with the reported N⁺ to O⁺ ratio. These observations indicate vast variations in the N⁺ to O⁺ ratio, ranging from less than 0.1 to supra-unitary. Albeit limited (and likely inconclusive), observational studies based on high-altitude measurements report on larger N⁺ to O⁺ ratio, as seen in Figure 1.

However, the N⁺ to O⁺ density ratio has been reported to vary not only with the solar cycle but also with the season, geomagnetic activity, latitude, magnetic local time (MLT), and time of day. These variations imply that N ⁺ and O ⁺ obey different chemical and energization processes as they are lofted from the ionosphere and possibly follow different paths of energization as they convect and drift throughout the magnetosphere. Therefore, their differential transport and circulation depend not only on the external drivers but also on the local atmospheric conditions.

Instruments onboard most space missions could not reliably separate the N⁺ from O⁺, and relatively few currently active ion spectrometers in space have the appropriate mass resolution to distinguish between these two ion species. Therefore, the separate observational record of N⁺ has been overlooked. These satellite-borne ion composition observations reveal several essential features attributable to “non-classical” acceleration mechanisms, i.e., centrifugal acceleration due to field line convection and curvature changes, transverse heating of ions as a result of wave-particle interactions, ponderomotive forces of Alfvén waves or Field Aligned Currents (FACs) driving the parallel electric field, and low altitude frictional heating Peterson et al. (1994); Yau et al. (2007). Therefore, questions regarding the relative contribution of the different sources of the high-altitude ionospheric outflow remain unanswered. In this letter, we review the most notable observations of nitrogen ions in the ionosphere-magnetosphere system to provide the reader with the context of these observations while emphasizing the need to develop instrumentation capable of distinguishing between O⁺ and N⁺ ions.

There are several possible mechanisms responsible for producing N⁺ in the sunlit ionosphere: dissociative ionization of N₂ by photons or photo-electrons, charge transfer reactions between N 2 + and N, and dissociative charge transfer reactions between He⁺ and N₂. On the other hand, nitrogen ions are lost through interactions with atomic and molecular oxygen (Lin et al., 2020). It is important to note that the dissociation energy of N₂ is different from that of O₂ (9.8 eV vs. 5.2 eV binding energy). Also, the ionization energies of nitrogen and oxygen (15.581 eV vs. 12.069 eV) are different. These differences dictate independent photo-chemical processes responsible for producing and losing N⁺ and O⁺, but also distinct escape scenarios.

This section presents the altitude profiles of production and loss processes for N⁺ ions from 200 to 2,500 km altitude in the polar ionosphere. These are derived from hybrid simulations using the Seven Ion Polar Wind Outflow Model (7iPWOM) (Lin et al., 2020), and the solution is based on the combined hydrodynamic approximation below 1,000 km altitude and particle-in-cell approach above 1,000 km altitude. Since solar activity is known to alter the density profiles of atmospheric neutrals, as well as the photo- and secondary electron spectra (Solomon et al., 1988), we present here the steady-state simulation results for summer solstice, both for Solar Maximum conditions (F10.7 = 180 × 10⁻²² WHz/m²), as well as for Solar Minimum (F10.7 = 80 × 10⁻²² WHz/m²), as shown in Figure 2. For both cases, the solution is based on a steady-state numerical simulation for which the magnetic field lines originated at 80° latitude and 12 MLT in the northern hemisphere. The neutral densities are obtained from NRLMSISE-00 empirical model (Picone et al., 2002), while neutral NO, NO(²D), N(²D), and N(⁴S) densities are retrieved from the Global Ionosphere Thermosphere Model (GITM) (Ridley et al., 2006). It is important to note that the neutral densities, in particular the density of neutral hydrogen, are of great importance for determining the global fluence of ionospheric outflow as the ionosphere and thermosphere are strongly coupled through the resonant charge exchange reactions between ionospheric ions and the colocated neutral hydrogen population. For instance, the supply of H⁺ to the ionosphere is limited by the local distribution of hydrogen density. However, there is controversy regarding the available supply of neutral hydrogen; studies report that the predicted neutral H density by the NRLMSISE-00 model is either overestimated by as much as ∼36%–67% (Waldrop and Paxton, 2013) or underestimated by as much as a factor of two (Nossal et al., 2012; Kotov et al., 2018). Furthermore, the density of hydrogen in the upper thermosphere is reported to vary with the solar cycle and is reported to be larger during solar minimum conditions as compared to solar maximum (Qian et al., 2018). Therefore, the production and loss rates presented in Figure 2 are only intended to provide context for the chemistry involving N⁺ ions in the high-latitude terrestrial ionosphere and are not representative of all conditions.

The top panel in Figure 2 lists the chemical reactions contributing to the production and loss of N⁺ ions, based on the reaction rates published in Lin et al. (2020). Each of the ion species involved in the ion-neutral-electron collisions is shown in colored text: O⁺ (blue), N⁺ (orange), He⁺ (dark green), H⁺ (light green), N 2 + (dark red), NO⁺ (purple), and O 2 + (brown). e* and hν denote the suprathermal electrons (SE) and photons that produce N⁺ ions. The orange arrows represent the production of N⁺ ions through chemical reactions, while the grey arrows denote reactions through which N⁺ is being lost. The thickness of these arrows indicates the efficiency of the reaction to produce or lose N⁺ ions, i.e., thicker arrows indicate chemical reactions that are most efficient to produce or lose this species, as derived from the specific reaction rate. The middle and bottom panels of Figure 2 show the production (orange lines) and loss profiles (grey lines) of N⁺ ions during Solar Maximum (center panel) and Solar Minimum (bottom panel) conditions.

The Suprathermal Electron(SE) production (solid orange line) and the charge exchange between neutral N(²D) species (orange + symbol line) dominate the production of N⁺ ions at altitudes between 200 and 2,500 km. In contrast, N⁺ ions are lost via charge exchange reactions with neutral NO (grey Y symbol line) and neutral O (grey + symbol line) in the low-altitude F2 region, while the dissociative recombination with electrons (solid grey line) and charge exchange with neutral H species (grey triangle line) take over the loss of N⁺ ions in the high-altitude region. In addition, the production and loss profiles indicate that the interplay between O⁺, N⁺, and molecular ions via ionospheric chemistry is critical to determining the budget of heavy ions in the low-altitude region. The production rates of molecular N 2 + and NO⁺ ions via charge exchange between N⁺ and neutral NO (grey Y symbol line) are comparable with that of N⁺ production via SE (solid orange line) below 1,000 km altitude. This implies that the abundances of N⁺ ions in the ionosphere are regulated by those of N 2 + and NO⁺ in the low-altitude region.

Although the primary reactions to produce and lose N⁺ ions are similar between Solar Maximum and Minimum conditions, the relative contributions of these reactions change under different solar activities, especially the SE production rate. For example, the loss rate of N⁺ ions via charge exchange with neutral H is larger than the production rates of N⁺ via SE production above 1,500 km altitude during Solar Maximum. However, this transition occurs at around 1,000 km altitude during Solar Minimum conditions. These variations in the production and loss altitude profiles hint at a dynamic interplay between all ionospheric species at lower altitudes, significantly altering the peak production rates for N⁺ for various conditions. In addition, the abundances of N⁺ ions in the polar ionosphere are mainly controlled by the SE production rate, therefore hinting at a possible connection between N⁺ density and solar driving via the F10.7 index. Furthermore, the N⁺ production rates during Solar Minimum conditions dominate up to 1,000 km altitude. In contrast, during Solar Maximum conditions, the SE production and the charge exchange between neutral N(²D) species are most effective below 500 km altitude. This suggests that N⁺ ions might have extended lifetimes during Solar Minimum compared to Solar Maximum conditions.

The first direct measurements of ionic composition in the topside ionosphere came from the Bennett type Radio Frequency (RF) quadrupole mass spectrometer onboard the Soviet Sputnik III satellite (Istomin, 1961). Sputnik III was launched on 15 May 1958, to study the upper atmosphere and the near-Earth space, on an orbit with 65.18° inclination, spanning space from 217 km to 1,864 km altitude, and re-entered the atmosphere in 1960. The mass spectrometer it carried provided measurements of ions with masses between 6 and 48 atomic mass units. Figure 3 shows the first measurements of N⁺ and N 2 + ions up to 500 km.

These measurements indicated that at lower altitudes, below 150 km, the abundance of N⁺ is somewhat small, with N⁺ densities being less than 10² cm⁻³; however, as the altitude increases, the N⁺ density increases rapidly by 2–3 orders of magnitude. While the abundances of N 2 + ions are a small fraction compared with those of the N⁺ component of the ionosphere, N 2 + plays a crucial role in the overall ionization balance of the ionosphere (Istomin, 1961). This is because O⁺ is primarily produced from atomic oxygen, while N⁺ is formed via N 2 + dissociation, based on the different chemical binding energies of O₂ and N₂.

The first U.S.-led detailed experimental study of atmospheric composition was based on data from the R.F. ion spectrometer onboard Polar Orbiting Geophysical Observatory (OGO 2), designed to measure thermal ions in the mass range of 1–45 amu. Figure 4 shows the concentrations of H⁺, He⁺, N⁺, and O⁺ ions as a function of dipole latitude and altitude (Taylor et al., 1968), as measured by OGO 2 on 15 October 1965 (quiet time, Dst ∈ [0, 2] nT) at dawn (panel a) and dusk (panel b). These measurements show that heavy ions dominate the atmospheric composition in the high latitude regions, while lighter ions prevail in the equatorial region. Furthermore, ion concentrations exhibit these high latitude variabilities both at dawn and at dusk local times. However, these observations not only showed evidence of latitudinal variation in the exospheric ion composition but also that N⁺ ions become significantly important at high latitudes, in the polar and auroral regions, where they can exceed the He⁺ abundances, and sometimes even the H⁺ (Brinton et al., 1968) density. Panel c) shows the N⁺ to O⁺ ratio, also as a function of dipole latitude and altitude. During the dusk pass, spacecraft measurements indicate that the N ⁺/O ⁺ is significantly higher than during the dawn pass, showing over one order of magnitude difference between the two data sets. This is mainly due to the different sampling altitudes between dusk (∼1,300–2,000 km) vs. dawn (∼400–900 km). Furthermore, during the dusk pass (at a sampling altitude between ∼1,300–1,700 km), above 60° latitude in the northern hemisphere, the N ⁺/O ⁺ ∈ [0.2, 0.6], while measurements taken during the dusk pass (at a sampling altitude between ∼600–800 km) yield a N ⁺/O ⁺ around 0.1.

These measurements were also confirmed by the mass spectrometer data from the Explorer 31 (DME-A) satellite, which showed that N⁺ is a significant ionospheric constituent, often exceeding He⁺ in concentration (Hoffman, 1967). Figure 5 shows the ion concentration profiles during 15 August 1966 (quiet time), as measured by Explorer 31. N⁺ density was reported to vary between 5% and 30% of that of O⁺, while H⁺ abundances were reported to be only 5% of the O⁺ concentration at these altitudes. These observational data sets suggest that, even during solar minimum conditions and geomagnetically quiet times, N⁺ ions are the second most abundant ion species found in the Earth’s ionosphere (Hoffman, 1970), findings aligned and confirmed by earlier measurements (Istomin, 1961; Holmes et al., 1965).

Similarly, Explorer 32 (Atmosphere Explorer-B or AE-B), launched on 25 May 1966, was designed to measure temperatures, composition, densities, and pressures in the topside ionosphere. The spacecraft carried a Bennett RF ion spectrometer, which measured the abundances of thermal positive ions of 1–4 and 12–19 amu. Based on measurements collected during the 10-month-long lifespan of the spacecraft, a global study of the diurnal variation of the atmosphere revealed substantial altitude variations of ion composition between 58° and 71° geomagnetic latitude. In addition, measurements at altitudes between 500 and 1,500 km and during geomagnetically active times reported that the abundances of O⁺ and N⁺ ions were a factor of ∼2.5 higher than during geomagnetically quiet times (Brinton et al., 1971).

The second satellite launched under the NASA International Satellite for Ionospheric Studies (ISIS) program, ISIS-2, was deployed on 1 April 1971, into an 88.1° prograde orbit with apogee and perigee of 1,440 and 1,360 km, respectively. ISIS-2 carried out an Ion Mass Spectrometer (IMS) experiment designed to measure the composition and distribution of positive ions in the terrestrial ionosphere in the mass range of 1–64 amu (Hoffman, 1970). The first measurements from the IMS instrument (Hoffman et al., 1974) showed significant variations in ion composition, particularly in the night-side equatorial region and in the daytime poleward of the plasmapause region. It was recorded that during daytime (summer conditions), above 20° latitude, the O⁺ ion is the dominant species, and its abundance remains constant to the pole. The density of N⁺ ions consistently varies together with the density of O⁺ at roughly one order of magnitude lower concentration, except at mid to low latitudes, where the ratio of O⁺/N⁺ is ∼20. It is noted that the same ratio approaches ∼3 on each side of the equatorial maximum abundance of O⁺ on the night-side. These features seem typical during undisturbed conditions (Hoffman et al., 1974) and in line with previous measurements.

During geomagnetically active times, the picture changes significantly. Figure 6 shows the ionic concentrations based on IMS observations during the double-dip geomagnetic storm of 4 August 1972, which recorded a minimum Dst of −125 nT and a Kp = 9. Measurements during the times when the Kp index reached the maximum value show that the N⁺ ion becomes the dominant outflowing species at 1,400 km, from 55° latitude towards the pole (Hoffman et al., 1974). In addition, large concentrations ( ∼ 1 0 3 cm⁻³) of molecular ion species, such as N 2 + , NO⁺, and O 2 + , are also observed at these times. During a similar event, measurements reported significant enhancements of N₂ at high altitudes, which could potentially provide the source of N⁺ and N 2 + , and therefore leading to the enhancement in their concentrations. The increase in the densities of molecular ion species during geomagnetically active times suggests that additional electrodynamic processes are required to explain the energization of these heavy ions, which under quiet conditions might go undetected (Wilson and Craven, 1998).

Furthermore, the Akebono spacecraft (launched on 22 February 1989) carried the Suprathermal Ion Mass Spectrometer (SMS) (Whalen et al., 1990), which sampled the two-dimensional thermal (0–25.5 eV) and suprathermal (55 eV/q-4.1 keV/q) ion energy distributions in the satellite spin plane. SMS measurements (Whalen et al., 1990) also confirmed the presence of N⁺ above the ionosphere. Spin averaged data taken on 7 November 1989, when the satellite was at 5,000 km in the southern hemisphere auroral zone near local noon, revealed the existence of a peak near m/q = 16 with a noticeable shoulder on the lower mass side. Inspection of the high-resolution data indicated that in fact both N⁺ and O⁺ ions were present at this time and with a O⁺/N⁺ density ratio of ∼ 2 .

Furthermore, cold atomic N⁺, and molecular N 2 + and NO⁺ species have been measured by the CASSIOPE Enhanced Polar Outflow Probe (e-POP) mission data (Yau et al., 2009), and these observations suggest that N⁺ can contribute up to 10%–50% to the plasma density at all times, independent of geomagnetic activity (Yau et al., 2019).

The ionosphere and the solar wind constitute the mass and energy source for the terrestrial magnetosphere. At the same time, the ionosphere is the primary supply of cold plasma to the plasmasphere and also a critical source for the plasmasheet population (e.g., Shelley et al., 1972; Cladis, 1988; Horwitz et al., 1990; Seki et al., 2015; Kistler et al., 2016; Welling and Liemohn, 2016), and a sufficient reservoir for the magnetosphere under any geomagnetic condition (Chappell et al., 1987). The first discovery of nitrogen ions (both N⁺ and N⁺⁺) in the magnetosphere was made by the Dynamic Explorer 1 (DE-1) (Chappell et al., 1982) mission, which carried the first mass spectrometer that could resolve masses near O⁺ peak in the mass spectrum, with a projected mass resolution δm/m = 3%. The Retarding Ion Mass Spectrometer (RIMS) Experiment onboard the DE-1 satellite measured ions with a mass between 1 and 32 amu and energies ranging from 0 to 50 eV. During the moderate geomagnetic storm of 30 December 1981 (when the Kp index reached a maximum of 6), the RIMS instrument recorded the presence of N⁺ and N⁺⁺ in the 04 to 16 MLT sector in the magnetosphere. Figure 7, adapted and digitized from (Chappell et al., 1982), shows the mass spectra measured in the high mass channel for two time periods: when the spacecraft was in the plasmasphere (solid line for measurements taken at 10:06 UT) and in the polar cap (dashed line at 07:37 UT). It is noted that the N⁺ and O⁺ peaks are clearly resolved in both cases, while no He⁺ counts are being recorded during both these times. Measurements from 30 December 1981, show cold ( < 30 eV) N⁺ ions outflowing from the polar ionosphere up to 3 R _E altitude in the polar cap (Chappell et al., 1982), with density profiles similar to the ones of O⁺. The recorded fluxes of N⁺ are 5%–10% of those of O⁺, also in agreement with previous measurements and supporting evidence that N⁺ is a constant companion of O⁺ (Craven et al., 1995).

In addition, the largest enhancements on the N⁺ fluxes are seen at the outer edge of the plasmasphere, suggesting the possibility of an existing N⁺ torus, analogous to the previously reported O⁺ torus features (Chappell et al., 1982). Furthermore, based on spacecraft position, peak flux, and flow velocity, it was inferred that these outflowing N⁺ ions could be interpreted as 0.3 eV field aligned N⁺ ion beams with a density of 0.8 cm⁻³, and they present similar characteristics as the low energy O⁺. A possible explanation of these observed enhancements of N⁺ fluxes at the outer edge of the plasmasphere is provided by the fact that the N⁺ undergoes more efficient charge-exchange reactions than O⁺ does and has a shorter average lifetime in the inner magnetosphere primarily due to the difference in charge exchange cross sections between the two species and the ambient neutral hydrogen. These differences imply that O⁺ ions are more likely to be transported inwards, towards lower L-shells, before they charge exchange with the ambient neutral H population, while energetic N⁺ ions have a shorter lifetime in the inner magnetosphere as they lost via charge exchange reaction significantly faster. This prohibits their transport deeper into the inner magnetosphere, and therefore they tend to populate the outer edge of the plasmasphere (Liu et al., 2022).

As Figure 7 shows, during this time, the highest fluxes of N⁺ are seen in the plasmasphere region as high as 3 R _E and the count rate ratio N⁺/O⁺ is about 0.1. These observations of magnetospheric N⁺ are aligned with the measurements reported in the low altitude ionosphere (Brinton et al., 1971; Hoffman et al., 1974). The low energy N⁺ were reported to exhibit seemingly similar characteristics with the low energy O⁺ and numerical modeling results suggest that, for low energy ions ( < 50 eV), the ratio of N⁺/O⁺ varies between 0.1 and 0.5 for L = 2, and from 0.25 to 1.0 for L = 4 at the equator at noon local time, findings in agreement with measurements from RIMS instrument on board Dynamic Explorer 1 spacecraft (Craven et al., 1993).

Energetic nitrogen ions of above 10 keV have also been detected at higher altitudes in the magnetosphere by the Active Magnetospheric Particle Tracer Explorers (AMPTE) charge-energy-mass (CHEM) instrument (Hamilton et al., 1988). Figure 8 shows the measurements for the energy density at low and high L shells during the first great magnetic storm of 9 February 1986 (with a recorded Dst minimum of −312 nT), after the launch of AMPTE spacecraft. The top panel shows the hourly Dst index throughout the storm, while the following two panels show measurements of the energy density for ring current species, at L = 3–5 and L = 5–7, respectively. While at all L-shells, the bulk of energy density is mostly carried by the H⁺ population, the N⁺ energy density closely follows the trend seen for O⁺. In addition, all ring current species show an increase in density during the storm period, but the relative increase of O⁺ and N⁺ ions is much larger at all distances. At lower L shells, during storm maximum, oxygen ions seem to be the dominant species, with nitrogen ions following closely, while at higher L shells, most of the energy density is carried by the H⁺ population.

Figure 9 shows the energy spectra for H⁺ (light green), He⁺ (dark green), N⁺ (orange) and O⁺ (blue) ions, adapted from (Hamilton et al., 1988). These measurements also show that the fluxes of high energy ring current N⁺ are comparable with those of O⁺ during active times and tend to be at least one order of magnitude higher than those of He⁺ ions. Furthermore, Magnetospheric Multiscale (MMS) observations showed that the high energy population ( > 150 keV) of the middle magnetosphere (beyond 7R _E ) is dominated by heavy ions species, which exist at higher intensities than protons at energies 175 keV, contradicting prior assumptions that protons are the dominant species in this region (Cohen et al., 2017). However, the charge states of these heavy ions hint at a solar wind origin rather than at an ionospheric source.

While solar activity controls the ionic composition of the upper atmosphere (Young et al., 1982; Moore et al., 1999; Cully et al., 2003; Peterson et al., 2006; Brambles et al., 2013; Chappell, 2015), the mass density in the magnetosphere, and hence the abundances of heavy ions of ionospheric origin in the near-Earth plasma are increasing with geomagnetic activity (Daglis, 1997; Nosé et al., 2003). This suggests that throughout the main phase of a magnetic storm, not only O⁺, but also N⁺ ions have the potential to become the dominant ring current ions (Hamilton et al., 1988; Ilie et al., 2021) in terms of energy density.

The Suprathermal Ion Composition Spectrometer (STICS) of the Geotail/EPIC (Energetic Particles and Ion Composition) instrument (Williams et al., 1994) had the capability to measure the mass and mass per charge of energetic ions within the energy range of 9.4–210 keV/e. Therefore, Geotail observations also show that both O⁺ and N⁺ are major constituents of the dayside (11–16 MLT) outer ring current, especially during increased geomagnetic activity (Christon et al., 2002). Furthermore, the density of N⁺ ions is trailing after hydrogen and oxygen ions, even during moderate geomagnetic storms. Figure 10, adapted from (Christon et al., 2002), shows the solar cycle variations of F10.7, Dst, and Kp indices, together with the N⁺/O⁺ ratio, from 1990 to 2002. Tracking the N⁺/O⁺ ratio together with the F10.7 index, a proxy for solar radiation and hence solar activity, reveals an inverse relationship between the N⁺/O⁺ ratio and solar cycle. It can be seen that this ratio ranges between 0.36 and 0.42 during low solar activity and decreases to 0.21–0.27 during times of increased solar activity. Therefore, one can note a drop by a factor of ∼ 2 in the N⁺/O⁺ as the solar cycle transitions from solar minimum to solar maximum. Similar findings are reported based on CRRES/MICS measurements, showing that the N⁺/O⁺ ratio in the ring current (2.5 < L < 6.5) region, even during geomagnetically quiet times during solar maximum is about ∼0.31 (Liu et al., 2005).

Figure 11, adapted from (Christon et al., 2002), shows histograms of nitrogen and oxygen ion pulse-height analyzed events for different solar and geomagnetic conditions. These measurements, based on 12 years of Geotail data, reveal large variations in the ratio of N⁺/O⁺ in the dayside outer ring current, ranging from 0.14 during active times at solar maximum to larger than unity during quiet times at solar minimum. This ratio is also affected by geomagnetic activity, but to a lesser extent, and it is likely due to the fact that solar activity is the dominant factor in this analysis, as it is responsible for altering the ionospheric source population and means of acceleration for heavy ion outflow. Nevertheless, even during modest geomagnetic storms, N⁺ is generally the third most abundant magnetospheric ion in the 22.7–210 keV/q range, after H⁺ and O⁺ in the dayside outer ring current.

These findings complement measurements based on instrumentation onboard the WIND spacecraft (Mall et al., 2002), which showed that the abundance of nitrogen ions in the magnetosphere displays both a solar cycle and a day-night variation. The N⁺ density has been reported to vary by as much as a factor of 2 with solar activity (Christon et al., 2002). Furthermore, the ratio of N⁺/O⁺ displays a solar cycle relationship with a higher value (0.45) at solar minimum conditions than at solar maximum when it reaches only 0.2 (Mall et al., 2002). Figure 12, adapted from (Mall et al., 2002), shows the variation of N⁺/O⁺ ratio with solar activity in the outer ring current region at 9–15 R _E . The factor of two variations has been linked to the altitude and latitude variations in ionospheric N⁺/O⁺ ratio since at times of enhanced ionospheric outflow, the ratio of magnetospheric N⁺/O⁺ approaches the ratio of N⁺/O⁺ at the topside ionosphere (Christon et al., 2002). In addition, Geotail data shows that oxygen and nitrogen ions are detected together in the outer ring current region nearly continuously, findings that are consistent with previous measurements coming from AMPTE/CCE data (Gloeckler and Hamilton, 1987) and a more recent study by Christon et al. (2020).

More recently, the first observation of the N⁺ band of electromagnetic ion cyclotron (EMIC) (Bashir and Ilie, 2021) waves has been reported by Van Allen probe wave observation during the recovery phase of a geomagnetic storm. The existence of the N⁺ band indirectly suggests the presence of N⁺ ions in the inner magnetosphere, as reported by the past observations (Chappell et al., 1982; Hamilton et al., 1988) and also theoretically inferred N⁺ composition using the indirect method for EMIC waves (Bashir and Ilie, 2018).

These observations reopen the question of ionic composition in the ionosphere-magnetosphere system and the need for caution when interpreting O⁺ measurements. Understanding plasma composition requires ultimately including a variety of ions that are currently known, although less reported, to be present in the low-altitude ionosphere. Table 1 summarizes the N⁺ measuring space missions and relevant details regarding orbits and onboard instrumentation. This review is intended to motivate and guide the development of instrumentation and possibly space missions, capable of measuring abundances and tracking the transport of both O⁺ and N⁺ ions, which are not quantified, nor understood, at this time (Ilie and Liemohn, 2016). Knowledge of the different behavior and paths of energization for O⁺ and N⁺ will provide the context for the interpretation and analysis of data from many currently operating ionospheric and magnetospheric missions.