He + dominance in the plasmasphere during geomagnetically disturbed periods: 1. Observational results

Abstract. Observations made by the DMSP F10 satellite during the recovery phase from geomagnetic disturbances in June 1991 show regions of He + dominance around 830 km altitude at 09:00 MLT. These regions are co-located with a trough in ionisation observed around 55° in the winter hemisphere. Plasma temperature and concentration observations made during the severe geomagnetic storm of 24 March 1991 are used as a case study to determine the effects of geomagnetic disturbances along the orbit of the F10 satellite. Previous explanations for He + dominance in this trough region relate to the part of the respective flux tubes that is in darkness. Such conditions are not relevant for this study, since the whole of the respective flux tubes are sunlit. A new mechanism is proposed to explain the He + dominance in the trough region. This mechanism is based on plasma transport and chemical reaction effects in the F-region and topside ionosphere, and on the time scales for such chemical reactions. Flux tubes previously depleted by geomagnetic storm effects refill during the recovery phase from the ionosphere as a result of pressure differences along the flux tubes. Following a geomagnetic disturbance, the He + ion recovers quickly via the rapid photoionisation of neutral helium, in the F-region and the topside. The recovery of the O + and H + ions is less rapid. This is proposed as a result of the respective charge exchange reactions with neutral atomic hydrogen and oxygen. Preliminary model calculations support the proposed mechanism. Key words. Magnetospheric physics (storms and sub-storms, plasmasphere)


Introduction
Study of singly ionised helium within the plasmasphere began over forty years ago (Nicolet, 1961;Hanson, 1962;Bordeau et al., 1962;Taylor et al., 1963).Since then, observa-Correspondence to: M. H. Denton (mick.denton@aber.ac.uk) tional and theoretical work has quantified the expected distribution and behaviour of He + in the plasmasphere (e.g.Taylor et al., 1970;Paresce et al., 1974;Murphy et al., 1979;Naghmoosh and Murphy, 1983;Chandler and Chappell, 1986;Newberry et al., 1989;Moffett et al., 1989;Bailey and Sellek, 1990;Heelis et al., 1990;Richards et al., 1991;Bailey and Sellek, 1992;Gonzalez and Sulzer, 1996), and the high-latitude region (e.g.Hoffman et al., 1974;Raitt et al., 1978;Heelis et al., 1981;Quegan et al., 1984).Theoretical progress was made by Quegan et al. (1981) who extended the transport equations first derived by Schunk (1975) by providing the mathematical formulation which allowed He + to be included as a major ion in a fully-ionised, four-component plasma (electrons and the O + , H + and He + ions).Model results by Quegan et al. (1984) showed that regions of He + dominance can occur in the high-latitude topside ionosphere, and that the behaviour of He + in this region is largely determined by plasma convection.
Little previous discussion has been made of the role of He + during geomagnetically disturbed periods.Horwitz et al. (1984) presented results from the DE-1 satellite data for the storm of 12-13 November 1981.After the time of maximum disturbance, He + is observed to rival H + as the dominant ion close to an L-shell of 3.5 and at an altitude between 1.5 and 2.8 R E .The concentrations of the other ion species measured by the satellite (O + , He ++ and O ++ ) fall in the region of the mid-latitude trough (see Horwitz et al., 1984, Fig. 2, Panel B) leaving the H + and He + ions dominant.A more complete description of the thermal plasma concentration and structure within the plasmapause region using DE-1 and DE-2 data is given by Horwitz et al. (1986).
The concentration of He + within the plasmasphere is particularly crucial to the development of electromagnetic ion cyclotron (EMIC) waves, a process that can occur in a H + /He + plasma (Norris et al., 1983;Young et al., 1981;Roux et al., 1984).In the presence of He + ions, an EMIC wave may trap thermal electrons and heat them to suprathermal energies between 3 and 20 eV (Roux et al., 1984); determination of the concentration and behaviour of He + ions is particularly important for understanding the heating mechanisms within the plasmasphere.
The depletion in electron concentration, known as the midlatitude trough, is located in the vicinity of the plasmapause and, although these two features are likely to be linked, there are significant differences between them.Extensive reviews of the mid-latitude trough, and ionisation troughs in general, have been carried out by Moffett and Quegan (1983) and Rodger et al. (1992).
The work presented here is an investigation of features observed in the DMSP F10 data set during geomagnetically disturbed periods.The 24 March 1991 storm is used as a case study for the temperature and concentration changes that occur during a storm.Following this, data from the disturbed periods in June 1991 are presented and the observed dominance of the He + ion at 830 km altitude during the storm time recovery phase is discussed.A mechanism, based on chemical and plasma transport effects, is proposed to explain the dominance of the He + ion at this altitude.

The Defense Meteorological Satellite Program
Data used in the current study are from the F10 satellite of the current DMSP series.Its orbit is sun-synchronous and approximately in the 09:00/21:00 MLT orbital plane at an altitude close to 830 km.The orbital period is around 101 min, giving just over 14 orbits a day, each separated in longitude by around 25 • (Venkatraman and Heelis, 1999).
Each satellite in the DMSP series carries instrumentation to measure several geophysical parameters along the satellite's orbit.The "Special Sensor -Ions, Electrons and Scintillation" (SSIES) package on board the DMSP satellites consists of four instruments: Langmuir Probe (LP), Retarding Potential Analyser (RPA), Ion Drift Meter (DM) and Scintillation Meter (SM).The operation of the SSIES instrumentation and DMSP data reduction are covered in detail by Heelis et al. (1978) and Greenspan (1994).In this current study, the electron temperature data are obtained from the LP instrument.Measurements of the ion temperature and concentration, and the individual O + , H + and He + concentrations are obtained from the RPA instrument.The individual ion concentrations can be determined when their respective concentrations exceed 5% of the total ion concentration (Venkatraman and Heelis, 1999).
3 The 24 March 1991 storm: a case study

Introduction
The severe magnetic storm which began on 24 March 1991 was observed by the DMSP F10 satellite from storm commencement around 03:00 UT through the recovery phase which lasted in excess of seven days.The progress of the storm can be seen by examining the Dst plot for the duration of the storm which is shown in Fig. 1.The maximum Dst excursion occurs late on 24 March.Rapid recovery occurs for a period of around one day, followed by a much slower recovery over the following week.During the day preceding the storm, Dst was slightly negative and broadly constant.At storm commencement, the increase in solar wind pressure caused Dst to increase sharply to an index of approximately +60 nT.During the storm main phase, Dst dropped to a minimum of around −300 nT, approximately 21 h after the initial storm commencement.The recovery period, which lasted more than seven days, was interspersed with further bursts of activity, causing more fluctuations in the Dst index.Continued disturbances in the Dst index were observed following the recovery period, which continued up to and after 30 March.

Data analysis and results
The RPA and LP instruments on board the F10 satellite were in constant operation during the storm period.Changes in the electron and ion temperatures and the ion concentrations are evident from the storm onset, and the data from three consecutive orbits during the storm period are shown in Fig. 2 (denoted PRE-STORM, STORM 1 and STORM 2, respectively).
Before storm commencement (PRE-STORM), the electron and ion temperatures were fairly constant with respect to magnetic latitude, with values close to 3000 K and 2500 K, respectively.The O + ion was the dominant ion, with a minimum in concentration centred around the magnetic equator.The total ion concentration was almost constant at around 1×10 5 cm −3 .The H + and He + ion concentrations had maximum values close to the magnetic equator.The He + ion had a maximum concentration of around 3 × 10 4 cm −3 .The H + ion concentration was below this value, and both the H + and He + ions were close to the limit of detectability by the RPA instrument.In the high-latitude regions, the H + and He + concentrations were so low that they were undetectable by the RPA.Since the initial storm onset occurred during the nighttime section of the DMSP orbit, i.e. between the PRE-STORM and STORM 1 data sets, the STORM 1 data corresponds to that orbit which began approximately 30 min after the storm commencement, defined as the first increase in Dst which occurred close to 2:00 UT on 24 March.
The major difference between the PRE-STORM and STORM 1 temperature profiles is the sharp rise in electron temperature, T e , that occurs in the mid-to high-latitude regions.This is caused by the sudden increase in local heating due to enhanced high-latitude particle precipitation.The US-Air Force Research Laboratory Auroral Boundary Index (ABI), calculated from the SSJ-4 instrument on the DMSP satellites, gives the equatorward boundary of precipitation for this orbit at close to 55 • magnetic latitude (figure not shown).This is consistent with the peaks in electron temperature of 5700 K which occurred at around ±55 • magnetic latitude.The low-latitude electron temperature also rose to around 4000 K at latitudes close to the magnetic equator.
During the STORM 2 orbit, the peak in T e reaches almost 6000 K.In contrast, the ion temperature, T i , only rises slightly in the mid-latitude region, to a peak just above 3000 K.However, during further orbits on the same day, T i reaches a peak of almost 5000 K (figure not shown).This is the result of heat transfer between the electron and ion gases, and especially between the ion and neutral gases.Joule heat-ing increases the temperature of the neutrals in the highlatitude region.Enhanced equatorward thermospheric winds may then drive such neutrals to lower latitudes, where ionneutral coupling boosts the low-latitude ion temperature (e.g.Fuller-Rowell et al., 1994, 1996).In addition, since the ion thermal conductivity is much less than the electron thermal conductivity, the energy input to the ion gas that occurs in the D-, E-and F-regions of the ionosphere takes longer to be transferred to the topside than the corresponding energy input to the electron gas.
Another dramatic change occurs in the total ion concentration, N i , between the PRE-STORM and STORM 1/STORM 2 orbits.Peaks in N i occur in the Northern and Southern Hemispheres (with maxima around 1.5×10 5 cm −3 ), initially centred at around ±50 • magnetic latitude.This is also due to the increase in particle precipitation that accompanies the storm, and the corresponding increase in ionisation in the high-latitude region.It should be noted that the peaks in maximum ion concentration move equatorward to around ±30 • magnetic latitude during the subsequent 24 h (figure not shown).Changes in the individual ion concentrations and their relative abundances also occur between the PRE-STORM and STORM1/STORM2 orbits.Before the storm, O + is the dominant ion, while H + and He + are minor ions.During the storm, the trough in O + concentration close to the equator initially deepens (STORM1) and the He + ion concentration approaches that of O + at around 3×10 4 cm −3 .As the storm progresses (STORM2), this situation changes and the O + concentration close to the magnetic equator increases to around 1×10 5 cm −3 .Peaks in the O + concentration occur in the mid-to high-latitude region, again due to particle precipitation.
Figure 3 shows DMSP data from three consecutive orbits that took place during the recovery period of the storm (27 March).By this time, the high-latitude heating has diminished considerably and the peak electron temperature has dropped to below 4000 K at magnetic latitudes close to ±50 • .This is a result of the poleward "relaxation" of the magnetospheric convective electric field.The plasmasphere has expanded and the auroral heating regions have moved poleward.The ion temperature remains fairly constant with respect to magnetic latitude at around 2500 K, but evidence of localised heating remains present in the high-latitude region.The total ion concentration during these orbits is fairly constant equatorward of around ±50 • .On the RECOVERY 3 orbit, the He + ion concentration again approaches that of the O + ion at around 4×10 4 cm −3 .This behaviour is clearly the result of a depletion (or trough) in the O + concentration, coupled with an enhancement in the light ion concentration.Such depletions allow the He + concentration to approach that of O + at numerous periods, both during the storm and throughout the recovery period.A mechanism for this observation will be discussed later.

Introduction
The geomagnetic activity for June 1991, as determined by the Dst index, is shown in Fig. 4. As can be seen from the variation of this index, the entire month was disturbed.Three X-class solar flares occurred in early June and sudden storm commencements were observed on 4, 8, 9, and 10 of the month (Pavlov et al., 1999).The period between 4-11 June has been considered as a single storm interval and has been the subject of previous experimental and theoretical investigations. (Pavlov et al., 1999).the Dst index).These features are found to occur at all longitudes, and during periods when the entire flux tube is sunlit, in comparison with the results presented by Hoffman et al. (1974), which showed regions of He + dominance for partially lit flux tubes.Figure 5 shows examples of orbits during June 1991 where He + is the dominant ion, or is close to being the dominant ion.Due to the summer-to-winter hemisphere directed neutral wind, the F-region is elevated in the summer hemisphere and depressed in the winter hemisphere and, at 830 km altitude, this has the effect of increasing the O + concentration in the Northern Hemisphere and reducing its concentration in the Southern Hemisphere.Thermal expansion also causes a relative increase in ion concentration in the summer hemisphere.It is clear from Fig. 5 that the regions where He + dominance occur are co-located with the trough in the O + concentration.Such regions are seen in the winter (southern) hemisphere during June 1991 and are observed between approximately 20 • and 55 • magnetic latitude throughout this month.
The increased depletion of O + that occurs during disturbed periods is due to erosion of the plasmasphere.At a constant altitude of 830 km, the relative O + concentration falls in the winter hemisphere, as the F-region is depressed by the neutral wind.However, further depletion of O + occurs as flux tubes that were previously co-rotating, and "filled" with ions of ionospheric origin, become affected by the magnetospheric convective electric field during storm times.Such flux tubes may cease co-rotating and follow convection paths where conditions will significantly reduce tube concentration, e.g. the tubes may move into darkness or partial darkness for long periods of time.

Discussion
Observations made during the geomagnetically disturbed month of June 1991 show regions close to the 830 km altitude at 09:00 LT, where ionised helium is at a higher concentration than either ionised oxygen or ionised hydrogen.This feature is only observed in the winter (southern) hemisphere between approximately 20 • and 55 • magnetic latitude and occurs during periods when recovery from geomagnetic storm conditions is thought to be occurring.Hoffman et al. (1974) presented results using the ISIS-2 satellite data taken close to the 1400 km altitude.He + was found to be the dominant ion in the winter hemisphere trough region at around 55 • latitude for a evening satellite pass at 17:13-18:10 LT (see Fig. 4 of Hoffman et al., 1974).This was explained to be the result of part of the ionosphere at this latitude residing in darkness, thus suppressing ion production.However, the ISIS-2 satellite was in a sunlit region and thus, ionised helium continued to be produced above F-region altitudes via photoionisation.The Hoffman et al. (1974) results are, at first glance, very similar to the DMSP F10 observations.However, during the DMSP orbits, the F-region of the ionosphere and the satellite orbital path are both constantly sunlit and thus, production of O + via photoionisation in the ionosphere occurs.Thus, the mechanism which produced the He + dominance noted by Hoffman et al. (1974) and the mechanism responsible for the He + dominance in the DMSP observations must be different.
Previous studies have examined the causes of He + dominance in the topside ionosphere.Quegan et al. (1981) were the first to provide the mathematical formulation which allowed He + to be included in a fully-ionised four-component plasma.Model results by Quegan et al. (1984) showed that regions of He + dominance can occur in the high-latitude topside ionosphere and the behaviour of He + in this region is largely determined by plasma convection.The authors postulated four conditions that lead to regions of He + dominance.Although these conditions were deduced for the high-latitude topside region, they are reproduced below, since they are useful for comparison with the regions and conditions examined in the current study.
(i) Both O + and H + must be depleted.This implies a lack of exposure of the F-region to sunlight and any other cause of ionisation.
(ii) There must be sunlight on the topside ionosphere region of the upper atmosphere, acting either to maintain He + concentrations or to cause a rapid enhancement in He + .
(iii) Transit through a region satisfying condition (ii) must not be too fast, so that He + has enough time to increase, while O + and H + are still at low abundances or decaying.
(iv) The decay region for O + and H + and the region of He + dominance need not be in the same place.Depleted plasma convecting into a region satisfying condition (ii) can produce a region of He + dominance.
These conditions will henceforth be referred to as the "He + dominance conditions".

A mechanism for He + dominance within the plasmasphere
The mechanism proposed to explain the regions of He + dominance in the current study is a combination of chemical and plasma transport effects.The flux tubes, both F-regions, and the DMSP satellite altitudes, are constantly sunlit.Refilling of storm-depleted flux tubes proceeds via ion upflow from the ionosphere.In addition, the concentration of the O + and H + ions is largely controlled by the charge exchange reaction between them During the main phase of a geomagnetic storm, the plasmapause moves equatorwards and the "size" of the plasmasphere is reduced.This is caused by the flux tubes becoming involved in magnetospheric convection, resulting in ion outflow to the outer magnetosphere, known as "erosion of the plasmasphere".During the recovery phase, the equator-ward boundary of convection moves poleward, and the previously depleted flux tubes refill from the ionosphere.The electron concentration drop across the plasmapause boundary may approach a factor of 100 (e.g.Carpenter, 1963;Carpenter and Park, 1973).
During sunlit hours, the flux tubes refill due to photoionisation that occurs primarily in the F-region.Pressure differences along the flux tube then lead to plasma transport of the ionisation into the topside.The main reactions which influence topside ion concentrations are shown in Table 1.He + production proceeds directly via photoionisation.The loss reactions for He + are of primary importance only during the nighttime, when plasma flows down the flux tubes to regions of increased chemical complexity.During the daytime, the chemical loss of He + is negligible.Production of O + ions, which populate the topside ionosphere, proceeds primarily through photoionisation of neutral oxygen, at F-region altitudes.However, the only significant source (and sink) for H + in the ionosphere is the charge exchange reaction with neutral and ionised oxygen (Eq.1).Direct photoionisation of neutral hydrogen is negligible, but during refilling of the flux tubes, the equilibrium reaction between O + and H + for the topside, (Hanson and Ortenburger, 1961) is maintained.In effect, this reaction means that the photoionisation of neutral oxygen is the ultimate source for both O + and H + .It is proposed that the consequence of the above equilibrium condition is to "suppress" the recovery of O + and H + and permit regions of He + dominance to arise.

Preliminary model results
Model results using the Sheffield University Plasmasphere Ionosphere Model (SUPIM) are now used to examine whether or not regions of He + dominance occur following a "model" storm.SUPIM has been developed over 30 years by members of the Space and Atmosphere Research Group at the University of Sheffield.The model solves coupled time-dependent equations of continuity, momentum and energy balance along closed flux tubes, from a base altitude of around 130 km in the Northern and Southern Hemispheres.These equations describe the physical and chemical processes that occur along the flux tube, and are solved for the O + , H + , He + , N + 2 , O + 2 and NO + ions and the electrons.Inputs to the model include the neutral atmosphere composition and horizontal wind, the solar EUV flux and the vertical plasma drift.Outputs include the plasma temperatures, concentrations and field-aligned fluxes.A full description of the model and its evolution have been given by Bailey and Sellek (1990), Bailey and Balan (1996) and Bailey et al. (1997).
The model results presented here are based on the refilling of flux tubes following a "model" geomagnetic storm.This first study merely concentrates on the changes in flux tube concentration during a storm.As such, the concentrations of the major ions during the modelled storm are reduced to 1% of their pre-storm value.This fall in concentration is typical of the reduction in electron concentration across the plasmapause boundary (e.g.Carpenter, 1963;Carpenter and Park, 1973), but the value is obviously much greater than any drop in the concentration that occurs at the plasmapause boundary at the altitude of the DMSP orbits (see Figs. 2 and 3).However, the current modelling study is meant to demonstrate that depletion and refilling of a flux tube can produce the conditions where He + dominance can occur; the study is not intended as a direct comparison with the DMSP data.
Following the initial depletion, the flux tube is left to recover via photoionisation of the neutral components, chemical and transport effects.Calculations were performed for a flux tube with apex altitude of 8000 km for the model day (21 June 1991).The F10.7 and Ap inputs to the model were 220 and 99, respectively.A simple axial-centred dipole approximation to the Earth's magnetic field was employed (Bailey and Balan, 1996).The reduction in ion concentration was imposed at 12:00 LT.
Figure 6 shows the modelled concentrations of the O + , H + and He + ions at 15 min intervals from 11:30 LT until 13:45 LT for a single flux tube, from a base altitude in the Northern and Southern Hemisphere of 130 km up to the apex altitude of 8000 km at the equator (L=2.26-invariant latitude 48.26 • ).The magnetic latitude of the flux tube corresponding to the F10 satellite altitude of 830 km is approximately ±44 • .The storm onset is taken to occur at 12:00 LT.Regions of He + dominance occur throughout all profiles following the storm onset and are particularly evident during the first 30 min after the storm commencement.The O + and H + ion concentrations recover much more slowly than the He + ion concentration.The model calculations show that such regions of He + dominance are expected both at and above the 830 km altitude of the DMSP F10 orbit.
The modelled regions of He + dominance are greater in latitudinal extent in the winter hemisphere than in the summer hemisphere.In addition, the regions of He + dominance in the model simulation occur slightly above the satellite altitude, and extend further in altitude into the topside.It should be noted that the He + concentration in the SUPIM model will be strongly affected by the concentration of neutral helium, and by the neutral wind.Values for these parameters are taken from the MSIS 86 (Hedin, 1987) and HWM 90 (Hedin et al., 1991) models, respectively.During disturbed periods, both the concentration of the neutral constituents and the neutral air wind are expected to change rapidly (Rishbeth et al., 1987;Fuller-Rowell et al., 1996), and the values provided by empirical models, such as MSIS 86 and HWM 90, may be inaccurate.In addition, during the current modelling study, the neutral atmosphere and wind taken from these empirical models were not time-dependent.
Despite the difference in altitude of the regions of He + Fig. 6.Examples of periods when the He + ion is dominant, or comparable with the O + ion in the trough region.These plots show data from the period when the plasmasphere is either disturbed, or recovering from disturbed conditions (4, 22, and 29 June, respectively).Such examples are typical of He + dominance in the trough region which occurs during the recovery period throughout the month of June.
dominance between the DMSP observations and the model results, the simulation shows that He + is expected to be the dominant ion in regions of the topside during the immediate recovery from a geomagnetic storm.The results appear to indicate that the DMSP observations are the "bottom-side edge" of a region of He + dominance that extends upwards of the 830 km altitude.
Despite the simplicity of these first model calculations, it has been shown that regions of He + dominance are to be expected during refilling of flux tubes.These results form part of an ongoing study to produce an enhanced simulation of a geomagnetic storm using the SUPIM model.Results from this study will be reported in a future paper.

Discussion
The work presented in this paper has been prompted by features observed in the DMSP F10 database during geomagnetically disturbed periods.The major storm that occurred on 24 March 1991 has formed the basis of a case study of storm effects on plasma temperature and concentration at around the 830 km altitude at 09:00 LT.Features in the data observed during June 1991 led to the investigation of regions of He + dominance, particularly at times of recovery from geomagnetic storms.
For the DMSP data taken during the recovery period, three of the four He + dominance conditions, originally proposed by Quegan et al. (1984), were fulfilled, while the remaining condition, condition (iv), was not applicable to the current study since the depletion and recovery of all three ions was presumed to occur in the same location.(i) Both O + and H + must be depleted.This condition is fulfilled since the O + and H + (and the He + ) concentrations are depleted due to the geomagnetic activity.Previously depleted flux tubes have returned to co-rotation and are refilling from the ionosphere.(ii) The topside ionosphere must be sunlit.This condition is fulfilled since the relevant part of the F10 orbit, and the underlying ionosphere are sunlit throughout the period of study.(iii) He + must have enough time to increase in concentration, while O + and H + remain at low abundances, or are decaying.The recovery of He + occurs very rapidly due to direct photoionisation of neutral helium.The recovery of the O + and H + ions is suppressed due to the charge exchange reaction between them.

Conclusions
This study represents further investigation of the role of He + in the topside during geomagnetically disturbed periods, and complements previous work on He + for the high-latitude ionosphere (Quegan et al., 1984) and periods when flux tubes are only partially sunlit (Hoffman et al., 1974).
The main conclusions of the current study are: 1. Regions of He + dominance occur in the altitude region close to 830 km.These regions are co-located with the trough in O + concentration within the plasmasphere and are observed to occur during the expansion and recovery phases of storms.2. A mechanism is proposed whereby the refilling of He + within previously depleted flux tubes proceeds, via photoionisation, faster than the refilling of O + and H + .The charge exchange reaction between O + and H + suppresses the recovery of these ions.This mechanism is supported by model calculations.3. Further modelling studies are required to confirm this proposed mechanism for He + dominance.Such studies are currently in progress.

Fig. 1 .
Fig. 1.The Dst index from 23 to 31 March 1991.The dashed line indicates the time of maximum Dst, and is defined as the start of the storm.

Fig. 2 .
Fig. 2.Observations of the ion and electron temperatures, and the O + , H + and He + ion concentrations, made close to 09:00 MLT by the RPA and LP instruments on board the DMSP F10 satellite, on three orbits surrounding the storm commencement of 24 March 1991.It should be noted that during parts of the orbits the concentration of H + and He + fell below the level of detectability.The spacecraft longitude (in degrees) and UT (in seconds) are given for the equatorward crossing of each orbit.

Fig. 3 .
Fig. 3.As Fig. 2, except that the orbits are taken from 27 March, a day during the recovery period.

4. 2
DMSP Observations of He + dominance around the 830 km altitude -data analysis and results Regions of He + dominance are observed in the DMSP F10 data set during the storm/recovery periods that occur during June 1991.Typical examples of such features are shown in Fig. 5.Many similar examples are found throughout the month of June, during periods when the magnetosphere is recovering from geomagnetic disturbances (as determined by

Fig. 4 .
Fig. 4. The Dst index for the month of June 1991.Almost the entire month of June is either geomagnetically disturbed, or recovering from geomagnetically disturbed conditions.A particularly large disturbance occurred on 4 June.

Fig. 5 .
Fig. 5. Examples of periods when theHe + ion is dominant, or comparable with the O + ion in the trough region.These plots show data from the period when the plasmasphere is either disturbed, or recovering from disturbed conditions(4, 22, and 29 June,.Such examples are typical of He + dominance in the trough region which occurs during the recovery period throughout the month of June.

Table 1 .
The main production and loss reactions which determine the concentration of O + , H + and He + in the topside ionosphere