Ion distributions in the vicinity of Mars: Signatures of heating and acceleration processes
© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. 2012
Received: 9 February 2011
Accepted: 28 April 2011
Published: 8 March 2012
More than three years of data from the ASPERA-3 instrument on-board Mars Express has been used to compile average distribution functions of ions in and around the Mars induced magnetosphere. We present samples of average distribution functions, as well as average flux patterns based on the average distribution functions, all suitable for detailed comparison with models of the near-Mars space environment. The average heavy ion distributions close to the planet form thermal populations with a temperature of 3 to 10 eV. The distribution functions in the tail consist of two populations, one cold which is an extension of the low altitude population, and one accelerated population of ionospheric origin ions. All significant fluxes of heavy ions in the tail are tailward. The heavy ions in the magnetosheath form a plume with the flow aligned with the bow shock, and a more radial flow direction than the solar wind origin flow. Summarizing the escape processes, ionospheric ions are heated close to the planet, presumably through wave-particle interaction. These heated populations are accelerated in the tailward direction in a restricted region. Another significant escape path is through the magnetosheath. A part of the ionospheric population is likely accelerated in the radial direction, out into the magnetosheath, although pick up of an oxygen exosphere may also be a viable source for this escape. Increased energy input from the solar wind during CIR events appear to mainly increase the number flux of escaping particles, the average energy of the escaping particles is not strongly affected. Heavy ions on the dayside may precipitate and cause sputtering of the atmosphere, though fluxes are likely lower than 0.4 × 1023 s−1.
Key wordsMars solar wind interaction ion escape
Mars is the smallest of the three terrestrial planets with atmospheres, with the weakest gravity and the thinnest atmosphere. The difference in solar wind interaction between Earth and Mars (as well as Venus) is primarily the presence of a strong internal magnetic field at Earth, which can balance the pressure of the solar wind at a distance of about 10RE. Mars does not have a significant internal magnetic field, but some significant crustal magnetic fields which does play a local role in the solar wind-atmosphere interaction (Acuña et al., 1998; Connerney et al., 2001; Brain et al., 2005; Edberg et al., 2008).
At the unmagnetized planets a pressure balance is formed between the dynamic pressure of the solar wind and the ionosphere supported by induced magnetic fields caused by ionospheric currents. The pressure balance occurs through the intermediary of the piled-up magnetic field in the mag-netosheath, see for example Luhmann (1990) for a tutorial. For Mars the ionosphere balances the external pressure at an altitude of a few 100 km (200–800 km with median 380 km for Mars, Mitchell et al. (2000)). The atmospheres of Earth and Mars are also very different, but this appears to play less role from a plasma dynamics point of view. In a denser atmosphere the ionosphere forms at a higher altitude, in a less dense atmosphere at lower altitude, but the area of the ionosphere as seen from above is not significantly affected, as the altitude of the ionosphere is small compared to the planetary radius. Atmospheric and exospheric scale height, as well as exobase and homopause levels will influence both details of the interaction and possibly the relative loss of different atmospheric species. For details on solar wind influence on the evolution of atmospheres we refer to Lammer et al. (2008) and references therein.
There is some evidence that Mars was once rather similar to Earth, with oceans and a denser atmosphere. Much of the evidence comes from geological features indicating outbursts of liquid water, as well as in situ samples of sedimentary rocks (Squyres et al., 2004). Some studies have questioned the picture of a wet and warm early Mars, e.g. Hoffman (2000). Measurements of planetary origin ion escape from Mars due to solar wind interaction has been made during high solar activity with the ASPERA instrument onboard the Phobos-2 spacecraft. These measurements indicated that a substantial amount of the ancient Mars atmosphere and oceans, if the denser atmosphere and oceans ever existed, could have been removed by solar wind interaction (Lundin et al., 1989; Verigin et al., 1991). Low solar activity loss rates based on ASPERA-3 measurements are of the order of 1024 s−1 (Lundin et al., 2008b; Nilsson et al., 2011), an order of magnitude less than the Phobos-2 high solar activity results, and thus not a significant contribution to the total escape.
In order to generalize the results obtained at present day Mars, so that they can be applied to the early solar system and exoplanets, we must investigate the details of the ion escape processes, not just present escape rates. The higher escape rates measured with Phobos-2 indicates a substantial dependence on the solar cycle. Such a dependence can come from enhanced production of ions and increased atmospheric/ionospheric scale height due to increased solar EUV, i.e. a change of the ionospheric source, as well as from more energy available for removal of atmospheric particles. The response to changing solar wind and EUV conditions during the declining phase of a solar maximum and solar minimum have been studied by Lundin et al. (2008a) and Nilsson et al. (2010). The response of the ion escape and the shape of the induced magnetosphere to changing solar wind flux and solar EUV could be qualitatively described for current conditions. Edberg et al. (2010) and Nilsson et al. (2011) looked at times when co-rotating interaction regions (CIR) arrived at Mars, and found that the outflow increased by a factor of on average 2.5 during a CIR, significantly less than the enhancement for solar maximum implied by the Phobos 2 measurements. The influence of magnetic anomalies on ion distributions have also been studied, e.g. Lundin et al. (2011) and Nilsson et al. (2006a, 2011), finding that the magnetic anomalies does affect the ion fluxes in the vicinity of the planet, but does not cause a hemispheric asymmetry of the escape inside the nominal IMB. The escape from the dayside ionosphere and/or pick up ion fluxes are larger from the northern hemisphere, which have less magnetic anomalies. In this study we will present average distribution functions of ions, obtained using almost 4 years of data, to study in detail the ion distribution, flow and acceleration in the vicinity of Mars. These results can be compared with model results, to elucidate topics such as the source of the escaping ions (ionosphere or exosphere), the location and nature of acceleration regions, and the response of the escape to increased energy input into the atmosphere system of Mars.
2. Instrument and Data
We use data from the Ion Mass Analyzer (IMA) of the ASPERA-3 instrument package on Mars Express (Barabash and the ASPERA-3 team, 2006). Mars Express is placed in an elliptical orbit with a epitasis altitude of about 275 km, an apoapsis altitude of about 10 000 km and a period of 6.75 h. IMA has an energy coverage of 10 eV to 36 keV. The lower energy limit of the measured source population is affected by spacecraft velocity (ram-effect) and spacecraft potential. The instrument has an energy resolution of 7% and steps through 96 energy levels in 12 s. Before May 2007 the instrument did in practice not measure below 30 eV. Between May 2007 and mid November 2009 an energy table going down to 10 eV was used. After that an improved table going down as close as possible to zero is in use. We have used data from May 2007 until February 2011.
The intrinsic field-of-view of IMA is 4.5° × 360° in the spacecraft X–Z plane, divided into 16 azimuthal sectors of 22.5° (see Barabash and the ASPERA-3 team, 2006) their figure 37 or Nilsson et al. (2006a) their figure 1 for a schematic description of the IMA field-of-view as well as a definition of the spacecraft coordinate system). Mars Express is a three-axis stabilized instrument platform. In order to obtain a limited three-dimensional field-of-view IMA utilizes an electrostatic entrance deflection system to bring particles in from about ±45° from the viewing plane of the instrument. The entrance deflection is stepped through 16 different elevation angles with an angular spacing close to 5.625° to obtain a total angular coverage of 90° out of the instrument viewing plane. Part of the three-dimensional field-of-view is blocked by the spacecraft body and the solar panels. Throughout our work we use only data from viewing directions which are not affected by spacecraft blocking. We use a conservative approximation of the blocking due to the moveable solar panels, rather removing too much than too little data. At energies below 50 eV the entrance deflection system has insufficient resolution to obtain the desired angles of deflection, and therefore the entrance deflection system is set to a value as close to zero deflection as possible. This means that below 50 eV the measurements are two-dimensional.
The mass per charge of observed ions is determined through a magnetic deflection system and a micro-channel plate based position detection system. Ions are distributed over 32 mass anodes, and a given ion mass will give counts spread around a given mass anode for a given energy. Through fitting of theoretical response curves for the major heavy planetary origin ions, assumed to be O+, and , these can be separately determined. The separation is better at low energy, below a few 100 eV, where the relative trajectory difference in the magnetic field at a given energy is larger, facilitating mass separation. Nominal positions for protons and alpha particles are always well separated from the heavier ions. The mass resolution of IMA is discussed in more detail in Carlsson et al. (2006).
The data used in this study has been treated by a noise removal process which removes counts with all zero neighbors in the nearest mass end energy channels. Elevated background counts, caused by solar EUV which may enter for certain conditions, or high energy particles, are automatically removed. Proton fluxes may for certain conditions, especially for intense fluxes at energies below 1 keV, contaminate mass channels corresponding to other ion species. This gives rise to a characteristic signal which is detected and accounted for in the data used in this study. Such data is not just removed, it is used to estimate the proton flux. The automatic algorithm detects more than 90% of the spread out protons, and essentially all cases with fairly strong proton fluxes. For weaker proton fluxes the spread out proton signal is not as wide as usual, but concentrated in a spot in the middle of the detector range. This coincides fairly well with where the O2+ mass peak is located for such energies. We calculate the flux in the mass channels corresponding to O2+, and increased fluxes in this mass range in the magnetosheath at energies typical for proton contamination can be used as a signature of insufficient removal of proton contamination. If the heavy ion flux is not much larger than the flux at the O2+ mass peak we discard the heavy ion data, in order to ascertain that we have a local maximum at the heavy ion mass channels, and thus remove the remaining contamination from protons. Such data is not used to reconstruct the proton fluxes. Sample energy spectra with background noise and proton contamination were shown and discussed in Franz et al. (2006).
A final aspect of our data treatment is cross-talk between different view directions (sectors) of the instrument. This appears to occur only for rather strong fluxes in some sectors, in which case a weak signal may be detected in all azimuthal sectors at the same energy as the original signal. In average distribution functions obtained over many years a rather clear but quite weak ring is seen at the same energy as the strongest signal. Real ring distributions, due to classical pick-up of ions in the solar wind, would not occur at the same energy for all viewing directions in the spacecraft reference frame. We have in our data subtracted the 25th percentile of the flux in the different angular directions for each energy level above 100 eV. This lessens the visual impact of the rings in the plots of the average distribution functions, but does not otherwise have a significant impact on any of our obtained results. Below 100 eV this type of rings are not discernible, and the measured fluxes have a wider angular spread so that this method is not necessary.
3. Data Analysis Method
The IMA angular coverage is not only limited, it is potentially strongly biased as the orientation of the three-axis stabilized platform is determined by the needs of the on-board cameras and other instruments designed to study the surface and atmosphere of Mars. The orientation is therefore neither evenly nor randomly distributed. The directional sampling problem is further emphasized by the low energy ion data, below 50 eV, which does not have entrance deflection scanning and is thus two-dimensional. Things are further complicated by the fact that the space environment around Mars is not symmetric, it shows clear asymmetry relative to the direction of the solar wind electric field (Dubinin et al., 2006; Fedorov et al., 2006; Barabash et al., 2007; Nilsson et al., 2010). The crustal fields have a very uneven distribution between the hemispheres (Acuna et al., 1998; Connerney et al., 2001), which may also bias data if these are important for the ion distributions around Mars and the ion outflow.
We have chosen to deal with this problem by binning the IMA data into angular bins as well as spatial bins. Our spatial binning is based on the Mars Solar Orbit coordinate system, with Xmso pointing from the center of Mars towards the sun. Ymso is the component of the sun velocity relative to Mars orthogonal to Xmso, i.e. in the orbit plane, pointed towards dusk. Zmso completes a right handed system, with +Zmso towards north. This basic coordinate system has been transformed to a two dimensional cylindrical coordinate system with the coordinates Xmso and .
For each spatial position we have binned the data after the angle of arrival of measured ions. The angle of arrival is measured relative to the +XMSO direction. The three-dimensional solid angle contributing to each angular bin is the solid angle of a cone-section with the angular width of the two-dimensional angular bin. The angle relative to XMSO, i.e. the sun direction, is given a sign such that it is positive along the RMSO vector, i.e. outward from the cylinder center. The solid angle for each angular bin thus corresponds to half a solid angle cone, one in for each hemisphere in the R direction. The solid angle contributing to each angular bin is used in the calculation of the total three-dimensional flux.
We therefore get average distribution functions for different spatial positions around the planet. Each angular direction bin and spatial bin have a different amount of samples. The average is calculated separately for each direction, thereby taking into account uneven angular sampling. Finally we calculate the energy shift due to the spacecraft motion for each individual looking direction of the instrument. This will at times move the measurable ions down to lower energies, more so for heavier ions. The ram velocity shifted data is interpolated to an energy table which consists of the energy table used between May 2007 and mid-November 2009, which goes down to 10 eV energy, with 10 equally spaced extra energy levels 1 eV apart below 10 eV. We do not take the spacecraft electric charge into account. The spacecraft charge is likely to be positive for a sunlit spacecraft in a tenuous plasma and likely negative in a dense plasma. For directional fluxes with a drift energy well above the energy corresponding to a spacecraft charge the flux estimates will not be affected, the ions will be slowed down/accelerated but the flux will remain constant. Similarly, cold plasma accelerated into the instrument by a negative charge will to a first order approximation not affect the net directional flux measured by the spacecraft, as the extra contribution will be the same from all directions. The spacecraft charge can sometimes be estimated using observations of photoelectron peaks of known energy, e.g. Franz et al. (2006). For ionospheric measurements the spacecraft potential is typically in the range —10 to 0 V.
The average distribution functions have been calculated for three heavy ion species, O+, and . The mass separation works well for low energy ions, which is where the separation is most needed, in order to compensate for the spacecraft motion. Apart from that effect, the estimate of the number flux is not dependent on the assumed ion mass. For high energy the mass separation is less reliable, so we present all data as the sum of the flux of all heavy ions. The average distribution functions at low energy, i.e. mostly close to the planet, can be well fitted by a drifting Maxwellian. We have done so for the low energy data, thereby extrapolating to lower energies than those observed.
In the final analysis presented in this paper we used spatial bins of size 0.2 × 0.2R m in our XMSO-RMSO coordinate system. The angular bin size was 20°, approximately matching the resolution of the instrument.
3.1 Fitting of distribution functions to low energy data
4.1 Average flow around the planet
Before we present the average distribution functions we will present the average flow around the planet calculated from these average distribution functions. The net flux in the X and R directions are calculated as for standard moment calculations (e.g. Franz et al, 2006). The flux in the higher energy part is thus calculated by integrating the average distribution function, while the flux in the lower energy part is estimated using the fitting procedure described in the previous section. The flux in the two energy domains are added. What is obtained is therefore a net flux in the X and R directions, an isotropic distribution centered on zero would yield zero flux. Furthermore the 3D solid angle corresponding to each angular bin is used to calculate the flux, so it is a three-dimensional flux value which is obtained. Figure 2 shows the average flux of protons (panel a), alpha particles (panel b) and heavy ions (panel c) in cylindrical coordinates. Mars is indicated with a red-orange circle, units are Martian radii (R m , 3393 km). White arrows indicate the flow direction, the colour scale shows the logarithm of the particle flux in units of m−2 s−1. The proton and alpha particles have been integrated for energies above 50 eV, for heavy ions we have integrated above 50 eV and used a fitted Maxwellian below 50 eV. Black numbers indicate the position of the sample distribution functions (see next section). Zero flux is indicated with a low number, to distinguish it from no data which is shown as white. All spatial bins with less than 104 energy spectrograms of data are treated as no data in Fig. 2. Each spatial bin contains 18 angular bins, which will have uneven sampling. With 104 spectrograms there is on average of the order of 103 spectrograms contributing to each angular bin which assures that we have good statistics. Lowering the threshold even down to 102 just adds a few spatial bins and does not significantly change any results. The complete data coverage was shown in Nilsson et al. (2011).
A model induced magnetosphere boundary (IMB) and bow shock (Trotignon et al., 2006), derived using Phobos 2 and MGS data, is shown as a black line. It is known that the position of the induced magnetosphere boundary is highly variable (Brain et al., 2005; Trotignon et al., 2006; Edberg et al., 2009), so the average flux of protons and alpha particles should gradually decrease around the average induced magnetosphere boundary when moving closer to the planet. The opposite is true for planetary origin heavy ions. This is indeed what is seen in Fig. 2, the model is a good description of the dayside IMB, at least for the rather limited resolution we are using here. In the outer tail, beyond about 2RM tailward, and at a radial distance of about 1.5RM and outward, we see large fluxes of protons inside the model IMB. The planetary origin ions, while clearly present in the same region inside the IMB, has significantly smaller flux than closer to the center of the tail. To some extent this is because we show the flux density (m−2 s−1) in Fig. 2, which decreases at larger radial distances as the ion flow is spread out over a larger area.
The flow direction of the solar wind ions is around the obstacle as can be expected. There is a significant amount of heavy ions outside the nominal induced magnetosphere boundary on the dayside of the planet. The flow direction of these ions is more in the RMSO direction, with a relatively smaller component in the anti-sunward direction, as compared to the solar wind origin fluxes. The bow shock can be clearly seen in the H+ and alpha particle data, as the region where the flux start to deviate around the obstacle. Two features are noteworthy concerning the magnetosheath flow. One is that the apparent bow shock, defined as the region where the flow start to deviate around the obstacle, is somewhat closer to the planet than the average bow shock position determined from wave data (Phobos 2) and electron and magnetic field data (MGS), i.e. as described in Trotignon et al. (2006). The difference is about one bin of 0.2RM and is likely due to the different phase of the solar cycle for model and data. The flow direction of the heavy ion fluxes in the magnetosheath are well aligned with the model bow shock.
The other noteworthy feature of the magnetosheath ion flow is the distribution of alpha particles within the mag-netosheath, which appears to be somewhat different from that of the protons. The alpha particle flux appears to be strongest in a plume along and just inside the bow shock, though the flow direction is not clearly aligned along the bow shock the way it is for the heavy ions.
Finally we note that the low proton fluxes in the solar wind, in the upper corner of the first panel of Fig. 2, may be due to poor statistics, but may also be due to an instrumental effect where narrow beams may be severely underestimated. This does not affect any of the conclusions drawn in the paper so we will not investigate this further.
4.2 Average distribution functions
At point 1, in the deep tail, we see no solar wind origin ions and most heavy ions have energies between 100 and 1000 eV. The heavy ions have a clear peak in their distribution for anti-sunward flow with only small fluxes in the sunward direction. Considering the long integration time the heavy ions mainly form tailward flowing beams with some deviations in the direction, consistent with previous reports Carlsson et al. (2006).
At point 2, somewhat closer to the planet and further away from the center of the tail, we see an added component of colder heavy ions, with only small fluxes of solar wind origin ions. The lower energy ions are mainly drifting tailward as well. Note that the unit used in the plot is flux, not phase space density. The distribution function is close to a tailward drifting Maxwellian. A detailed sample was discussed in Section 3.1. The temperature of the fitted Maxwellian distribution is 5 eV. The more energetic ions above about 100 eV form tailward flowing beams. We do see some low energy ions at about 10 eV energy in the alpha channel. Previous reports have attributed such low energy ions to ions (Lundin et al., 2009) rather than alpha particles.
Point 3 is located at a relatively low altitude in the night-side tail of Mars. We see more intense fluxes of low energy heavy ions, reaching down to almost 0 eV (measured through ram-shift of the measured ions, the lowest energies are reached for the heaviest ions). Statistics are relatively poor for the lowest energies which can only be reached through the spacecraft ram energy shift, but still exhibits a quite smooth curve from 1 up to about 100 eV. The fitted temperature is 4 eV. The low energy component of the heavy ions is now dominating, but some accelerated ions are seen already here, with a rather random angular distribution. The flux of low energy ions detected in the alpha channel (mass per charge, m/q, of 2) is more intense than further tailward. Some of these particles are detected at more magnetosheath-like energies (best seen in Fig. 4). Whether these are ions that have been accelerated or intruding magnetosheath alpha particles cannot be directly resolved from the observations alone. However one should note that the more energetic part of these m/q 2 ions (>50 eV) are the ones used to obtain Fig. 2, and these are flowing inward in the tail, as opposite to the heavy ions which are flowing straight anti-sunward or somewhat outward. This seems to indicate that the more energetic component in the alpha mass channel is indeed due to solar wind origin alpha particles penetrating into the tail. The flux of protons at magnetosheath energies is low.
At point 4, located quite far downstream, but well away from the center of the tail, we see tailward flowing solar wind origin ions at the same time as heavy ions. The heavy ions are observed at energies from a few eV up to a few keV. The fitted temperature is 8 eV. The flux in the higher energy part (above 100 eV) dominates, note that we show differential flux per eV in Fig. 4 and use a logarithmic scale for the energy. The heavy ions have a clear peak in their distribution for the tailward flow direction. The protons have a somewhat narrower energy distribution as compared to further upstream in the magnetosheath (point 5).
Point 5 is located outside the nominal induced magnetosphere boundary (IMB), somewhat sunward of the terminator. As expected we see tailward flowing solar wind origin ions of magnetosheath-like character, with energies between 100 eV up to almost 10 keV. There are no significant heavy ion fluxes at the lowest measurable energies and the fluxes are relatively low below 100 eV. The heavy ions show a peak in their distribution in the radially outward direction. Energies of heavy ions reach a few keV, much less than the highest energies of the solar wind origin ions. The shape of the average energy spectra are otherwise rather similar.
Point 6 is located at the terminator and just inside the nominal IMB. We do see magnetosheath-like fluxes of solar wind origin ions here, though the protons show weaker peak fluxes, as can be expected inside the nominal IMB. The heavy ions show much enhanced densities of a heated thermal population, i.e. fairly symmetric in angular space. The temperature of the fitted distribution is 5 eV. At energies above 100 eV there is an enhancement of the fluxes in the tailward, radially outward direction. The alpha particle energy of the main, magnetosheath origin population extends down below 100 eV, whereas we once again see a clear local peak at about 10 eV, likely representing .
Point 7 is located in the front-side magnetosheath at a significant radial distance from the subsolar point and just outside the nominal IMB. This is a region where the integrated flow of the heavy ions is more radial than the flow direction of the solar wind origin ions (Fig. 2). The distribution of the heavy ions have a peak in the radially outward direction, close to perpendicular to the sun-planet line. The peak of the proton and alpha distributions are flowing around the planetary obstacle, having a mean flux with an angle of about 45° outward from the anti-sunward direction. Low energy heavy ions are also observed this close to the nominal IMB, with a fitted temperature of 7 eV. Part of the heavy ion flow is directed towards the planet and could cause heavy ion sputter of the atmosphere of Mars. We have therefore made a first rough estimate of the flux in the lowest altitude dayside bins which is directed towards the atmosphere (taken as ±60° from the tailward direction summed over the lowest altitude dayside bins with radial position RMSO < 1 RM). This flux is 0.4 · 1023 s−1 for our average solar wind conditions.
4.3 Co-occurrence of heavy and solar wind origin ions
With the average distribution functions it is not possible to tell if solar wind and planetary origin ions are present in the same statistical bin at the same time. This can be done using ordinary moment data, even though these may suffer from biased and limited sampling. Using moment data when at least either heavy ion flux or proton flux was nonzero, we can see how often the two populations are non-zero simultaneously in the same spatial bin. We have investigated the outer tail boundary which may be a superposition of a flapping tail, or show a region of real plasma mixing. We have done the same investigation for the magnetosheath, where we have investigated the region outside the nominal IMB sunward of X = − 1.
For the outer tail region, inside the nominal IMB at ( XMSO < -2, 1.5 < RMSO < IMB) the heavy ion flux and proton flux were non-zero simultaneously in 32% of the cases, only heavy ions were present in 23% of the cases, and only protons in 45% of the cases. In the nominal magnetosheath, sunward of XMSO = − 1, the heavy ion flux and the proton flux were non-zero in 37% of the cases, only heavy ions were present in 5% of the cases and only protons in 57% of the cases. Almost the same result is obtained for the nominal magnetosheath tailward of XMSO = − 1. One should note that the final step of the data cleaning procedure, checking for apparent O2+ fluxes in the magnetosheath, was performed at the moment data level in this case. The time resolution of the moment calculation is only 192 s. This is a coarser method than the one used otherwise in this paper, as it will remove all data at all energies during one time period of 192 s if a part of it is contaminated. Still we get a quite clear picture from the moment data. Heavy ions and protons are observed simultaneously as often in the outer tail region as in the nominal magnetosheath sunward of XMSO = − 1. Thus we cannot really distinguish between tail flapping and a statistical IMB closer to the tail. An average fit in radial coordinates would clearly yield an IMB, based on ion observations, closer to the planet than the nominal IMB we use for comparison. The low occurrence of only heavy ions in the nominal magnetosheath indicates that the IMB model we are using is at least not overestimating the altitude of the IMB for the low solar activity conditions prevailing during our observations. Some observations of heavy ions only should be expected outside the model average IMB, as the IMB is dynamic.
4.4 Acceleration of ions in the tail and the total flux in the tail
The low energy component is estimated from the Maxwellian fit described in Section 3.1. The good continuity with tail distance of the total flux, despite the acceleration of the ions in the tail, thus indicate that our low energy flux estimates at the terminator is a good estimate of the total flux. The expected continuity is based on the assumption that the trans-terminator flow is the main source of ions in the tail, and that the lack of data points in the planet shadow thus does not strongly influence our results. If they did, we should see a significant increase in the tail fluxes as the data coverage improve with tailward distance. This is not the case, though we do see a dip at XMSO = −3. This indicates that most of the tail flux passes through the region we can observe at XMSO = − 1, and that the tailward trans-terminator flux equals the total tail escape flux. The total escape through the tail, and thus the trans-terminator flux, estimated from our data set has been reported by Nilsson et al. (2011). The average tail escape flux inside the nominal IMB is 1.1·1024 s−1, of a total escape of 2±0.2·1024 s−1.
4.5 Acceleration of heavy ions during CIR events
If more energy is put into the Mars ionosphere this may lead to increased escape of planetary ions, as has been shown for our data set by Nilsson et al. (2011). For modeling of the ion escape, it is important to know how much of the increased energy input goes into more escaping particles, and how much goes into further acceleration of particles that would anyway escape. CIR events represents a pronounced increase in the energy flux in the solar wind and are therefore very suitable to study the response of the near Mars space to increased energy input from the solar wind. We have used the same CIR events as in Edberg et al. (2010) to make a data set which can be compared with the average conditions (excluding the CIR events). The CIR data consists of 41 high pressure events observed between July 2007 and September 2008.
The shape of the tail distributions during CIR events and during average conditions are also quite similar, with only a slight shift of the higher energy population in the tail towards higher energy during CIR events.
5.1 Distribution functions
Three features of the average distribution functions are important. The first is that the average low energy populations are close to Maxwellian, and whereas the bulk drift has a tailward component, the distributions show significant fluxes of sunward moving ions as well (i.e. see the sample distribution of Fig. 1 and examples 2, 3 and 6 of Fig. 3 for clear cases). The altitudes where these ions are observed are in the non-collisional regime (the exobase is expected to be at 195–215 km altitude). Gyration in a background magnetic field and wave-particle interaction reasonably give rise to the thermal populations with particles moving in all directions. In the energy range of a few eV gravity may also play a role, as the escape energy for heavy ions at Mars is 2 to 5 eV. Wave-particle interaction at Mars has previously been discussed by Ergun et al. (2006). Our data confirm the importance of heating processes in the upper ionosphere of Mars. Due to lack of wave measurements we cannot directly study the heating mechanism. We do note that in the upper magnetosphere of Earth, where background magnetic fields are of the same order of magnitude as in the induced magnetosphere of Mars, out flowing heavy ions are effectively heated by what appear to be Alfvén waves (Nilsson et al., 2006b; Slapak et al, 2011; Waara et al., 2011).
The outflowing ions at Mars are accelerated to form tail-ward flowing beams, apparently at least in part by the solar wind motional electric field (Dubinin et al, 2006; Fedorov et al., 2006; Nilsson et al., 2010). The second important feature of the average distribution functions is that the tail-ward flowing beams show a distinct distribution in energy space, in most of the tail well separated in energy from the low energy ions. See Fig. 5 for a clear distinction between the two energy populations, see sample distributions 1, 2 and 4 of Fig. 3 for two-dimensional samples. Further tailward, the flux in the average low energy population decreases and the flux in the average high energy population increases. The general increase of the higher energy population with distance from the terminator implies that acceleration occur throughout the tail. Tailward of XMSO = − 1RM the two populations show rather small variations in the average shape of their energy distributions and seem to remain distinct from each other. This suggests that acceleration occur quickly in a relatively confined region. If acceleration is fast/confined in space, ions are more likely observed before or after acceleration. The further tailward, the more likely that the ions have already been accelerated at the time of observation. Our conclusion is that acceleration occur throughout the tail, but in a confined region in the YMSO-ZMSO plane. Different types of acceleration in the Martian tail was discussed by Fedorov et al. (2006), where acceleration by the solar wind electric field and j × B tension forces are likely alternatives. Heating and subsequent tail-ward acceleration by the mirror force can also be a viable explanation depending on the geometry of the draped field-lines.
The third important feature relates to the heavy ions observed in the magnetosheath. These have a stronger RMSO component than the solar wind origin flow. They also have a rather low energy as compared to classical solar wind pick up ions, at or below the energy of the solar wind origin specie. Finally, they do not form torus or shell distributions. Pick up ions will upon creation move in the direction of the magnetosheath electric field which is consistent with the radial flow direction. In due time, in a constant background magnetic field, the picked up ions will gyrate and come back to near the starting point. If the ions could form a proper ring distribution this should yield a rather small net radial flow, consistent with the background magnetosheath flow. The gyro radius of energized heavy ions in the magnetosheath of Mars is on the order of a few hundred to a few thousand km. A possible explanation for the observed near radial bulk flow is that the gyro radii of the ions we observe are of the same order of magnitude as the thickness of the magnetosheath close to the planet. Therefore the ions do not form well behaved torus distributions. Furthermore the electric and magnetic fields in the magnetosheath are variable on the time scale of a heavy ion gyration period which is of the order of 10 to 100 s. A plume of ions extending in the solar wind electric field direction is a feature of a number of simulations (see Brain et al. (2010) for a summary and comparison of most recent Mars models). For the data set we are using here, taken after the operations of the Mars Global Surveyor spacecraft ceased, there is no local (Mars orbit) proxy available for the solar wind electric field direction. We can confirm the presence of a plume of heavy ions extending into the magnetosheath, but cannot investigate the dependence on the solar wind electric field direction. Previous work by Dubinin et al. (2006) have shown how ionospheric ions can be gradually accelerated by what appear to be a penetrating solar wind electric field. This means that the ions must have a significant motion in the direction of the electric field when they are accelerated. Our data is thus consistent with an ionospheric origin also for the magnetosheath heavy ions. It is therefore not clear from our data wether the magnetosheath heavy ions were created within the magnetosheath (pick up ions) or if they represent another escape path of ionospheric origin plasma. A careful examination of the mass of the escaping magnetosheath heavy ions could be used to distinguish between these possibilities, as exosphere pick up should be dominated by O+. It is noteworthy that the range of energies observed and the shape of the angular distribution (but not direction) are very similar for the accelerated magnetosheath and the accelerated tail heavy ion fluxes. The range of mass channels covered by the heavy ion species in the magnetosheath and tail are quite similar, suggesting an ionospheric origin for both populations. As noted earlier mass separation is less reliable at the energies observed in the magnetosheath, so we leave a more careful composition analysis for a future study.
We can confirm the presence of anti-sunward moving heavy ions in the dayside Mars magnetosheath and magnetosphere, which may precipitate and cause ion sputtering of the ionosphere. Sample data was shown in Fig. 3, sample 7. A rough estimate gives an approximate anti-sunward flux of 0.4 ∙ 1023 s−1 for our average solar wind conditions (see description at the end of Section 4.2). This must be considered as an upper limit, as higher resolution measurements, preferably binned in altitude and solar zenith angle, should be used to get a more reliable estimate of how much flux will really reach the exobase. We are currently working on such a data set.
Finally one may note the lack of significant sunward flowing ions in the magnetotail. Some models have predicted rather different distributions in the magnetotail of Mars, e.g. Fang et al. (2008). At our sample point 3 the rather weak accelerated fluxes seen could in part be made up of picked up ions that have moved back into the tail, so the phenomenon discussed by Fang et al. (2008) may indeed exist, but with a very different spatial distribution as compared to their model results. Modelling distribution functions, which can be compared with the observations presented here, will be an important step forward in understanding the ion dynamics at Mars.
5.2 Dynamics and mixing of ion populations
In Section 4.3 we showed that the outer tail region, inside the nominal IMB but with significant fluxes of solar wind origin ions, had somewhat lower co-occurrence of heavy and solar wind origin ions than the magnetosheath. Occurrence of O+ only, without any solar wind origin ions, was much more common than outside the nominal IMB, as can be expected. This support the picture of a moving tail boundary as an explanation for the outer tail region with mixed ion populations, as opposite to a region with mixing of the two regions as a result of boundary instabilities. In the latter case we would expect higher co-occurrence of heavy and solar wind ions in the mixing region as compared to in the magnetosheath.
It is noteworthy that significant fluxes of solar wind origin ions were present inside the nominal IMB in the outer tail, tailward of X = −2, in the majority of all cases. Solar wind origin ions were present in 77% of the cases, with solar wind origin ions only in 45% of the cases. Therefore the nominal IMB of the Trotignon et al. (2006) model appears incorrect tailward of X = −2 for solar minimum conditions. With solar wind origin ion fluxes going from low at R = 1.6 to high at R = 2, putting the average tail boundary at R = 1.8 would give a better estimate than the IMB model we have been using. Agreement is better with the fit of MGS data provided by Vignes et al. (2000) which have an approximately constant radial distance of the tail IMB tailward of X = −2.
We suggest that the tail IMB should be studied based on ion data using boundary identifications on an orbit by orbit basis in order to improve these initial results.
The low occurrence of heavy ions only, no solar wind origin ions, in the nominal magnetosheath indicates that the IMB model of Trotignon et al. (2006) is at least not over-estimating the altitude of the IMB sunward of X = −2. Visual inspection of Fig. 2 indicates that the model is accurate for this region within the accuracy of the binning used in our study. The study of Edberg et al. (2009) showed that for the conditions between 2004 and 2009 the IMB (magnetic pile-up boundary when determined from MGS data) at the terminator varied about 0.2RM with solar EUV changes, and a similar amount between no crustal fields and the strongest crustal fields. Not taking crustal magnetic fields into account will thus smear our boundary up to one data bin at the terminator, less in the dayside. A similar smear will occur for position changes due to the changing solar cycle.
Another dynamic region in space around Mars is the bow shock. The average position is clearly seen in our data as a change in the flow direction from anti-sunward to around the planetary obstacle. The significant change of the average flow direction occurs well inside the statistical bow shock crossing determined from plasma waves data (Phobos 2) and magnetic field and electron data (MGS spacecraft). The discrepancy between our bow shock determined using the solar wind origin ion flow direction and the Trotignon et al. (2006) model is likely because our measurements were made during the minimum of a solar cycle (2007–2010), whereas the model is based on data from solar maximum (Phobos) and the increasing phase of a solar cycle. Edberg et al. (2009) have shown that the bow shock position is sensitive to the solar EUV flux which varies with solar cycle. The variation in the average bow shock position at the terminator was 0.4 RM for the range of solar EUV flux obtained between 2004 and 2009. This is consistent with our observed difference between the Trotignon et al. (2006) bow shock position and the deviation of the ion flow from anti-sunward of about 0.2RM.
The flux of heavy ions in the dayside magnetosheath is well aligned with the model bow shock, and significant heavy ion fluxes occur approximately out to the model bow shock. Heavy ion fluxes thus occur somewhat further out than the average position of the bow shock for the solar conditions of the observations. Heavy ion fluxes are thus present in the bow shock region at Mars, and could possibly affect the physics of the bow shock region. Yamauchi et al. (2011) have shown that the bow shock region at Mars is different from that at Venus and Earth. Clearly a study should be made of simultaneous bow shock signatures in electron, solar wind and heavy ion data.
Another feature of our data is that the alpha particle fluxes have a somewhat different distribution than the protons. The alpha particle fluxes are enhanced in a plume along the bow shock. This is a type of signature that could occur in multi species models, and is worthwhile to look for in simulation results.
5.3 Trans-terminator flow
Their 7 cases are not typical. Ionospheric origin ion fluxes are known to show large variations at Mars. These variations may also be spatial, which leads to the second possibility.
The trans-terminator flux is not uniform, as assumed when the single point observations of Franz et al. (2010) are extrapolated to give a total flux. With our method, fluxes may be non-uniform as long as they are sampled in a symmetric fashion. Possible sources of asymmetry which could affect our estimate include uneven sampling of the northern and southern hemisphere, and uneven sampling relative to the direction of the solar wind electric field. In Lundin et al. (2011) it was shown that the tail fluxes show no hemispheric asymmetry, so this would not affect our results. Nilsson et al. (2011) showed that there are flow asymmetries with more escape from the north and dusk as compared to south and dawn. The average result obtained when calculating escape using these for quadrants or ordinary cylinder symmetry was however negligible. The solar wind electric field direction depends on the direction of the solar wind magnetic field, which alternates depending on whether Mars is above or below the heliospheric current sheet. For shorter periods of time, this could be a problem, especially for a few case studies. For almost four years of data the solar wind electric field will have an even distribution, with the positive and negative “electric field hemispheres” sampled equally often.
There is a cold population also in the tail, which is not measured by the particle detector and not well approximated by our Maxwellian fit. Spacecraft charging and limited energy resolution may indeed prevent observations of a low energy population, so this is a possibility. However the continuity of our tail flux estimates with tail distance, despite the increasing dominance of the accelerated population, does indicate that our low energy flux estimates close to the planet yield a good estimate of the average escape flux, consistent with the higher energy measurements obtained deeper into the tail.
We have shown average distribution functions of solar wind origin and heavy ionospheric origin ions in the vicinity of Mars. These show clear evidence of a heated ionospheric ion population as the main source of the escaping ion fluxes in the tail of Mars. Our results show that the gradual increase of the average bulk speed in the tail is primarily due to a shift between a cold population at energies of about 10 eV, which dominates close to the planet, and an accelerated population with energy typically in the range from 100 eV to 2000 eV, which appear to get most of its acceleration in a confined region. No significant fluxes of planet ward moving ions are seen in the tail.
Our data set shows a very good continuity in the estimated total tailward flux inside the IMB. This suggests that the nightside ionosphere, not covered by our measurements is not a strong source (as can be expected). Furthermore this indicates that the average total trans-terminator flux is an order of magnitude lower than the estimates obtained by Franz et al. (2010) based on a few carefully selected and studied events.
The ionosphere may also be the source for the heavy ion fluxes from the dayside and terminator regions through the magnetosheath, although classical pick up of exospheric atoms and molecules ionized inside the magnetosheath may also be a viable source. Careful modeling of the resulting ion distributions should be able to distinguish between these scenarios through comparison with our observations. The heavy ion magnetosheath fluxes form a plume extending from the dayside ionosphere and terminator region, along the bow shock. The flow direction is more radial, approximately along the bow shock, than the solar wind origin ion fluxes in the magnetosheath.
We can confirm the presence of heavy ions moving towards the planet in the dayside magnetosphere and magnetosheath. The total planet ward flux in our lowest altitude bins (covering altitudes from the minimum 275 km up to 0.2RM = 680 km) is 0. 4’ 1023 s−1, which should be considered an upper limit for the flux that actually reaches the exobase.
Our comparison of the average energy spectra during average solar wind conditions and during CIR events indicates that the average ion energy is not strongly affected by the CIR. This means that the increase in available energy is relatively effective in removing ions, as not much energy is wasted in further acceleration of ions that would anyway escape.
Our observations in the outer tail beyond an X distance of — 2RM indicate that the IMB model of Trotignon et al. (2006) is not good for predictions of where to find solar wind origin and ionospheric origin ions for low solar activity. It appears as the average tail IMB should be narrower, a straight line at a radial distance of about 1.8RM seems suitable, although identification of the IMB position on an orbit by orbit basis should be used for an improved tail IMB model based on ion data. Finally we suggest that the heavy ion fluxes in the dayside magnetosheath affect the Martian bow shock. A detailed comparison of the bow shock as determined from electron data (as for the MGS data) and from ion data (as in our data set) should be performed. The bow shock as based on ion data during low solar cycle is closer to the planet than in the Trotignon et al. (2006) model, which is consistent with the solar EUV dependence of the position of the bow shock determined by Edberg et al. (2009).
The work was supported by the Swedish National Space Board. The work of HN and NJTE was supported by the Swedish Research Council. The work of GS was supported by the National Graduate School of Space Technology, Lulea University of Technology.
Guest editor J. S. Halekas thanks two anonymous reviewers for their assistance in evaluating this paper.
- Acuna, M. H., J. E. P. Connerney, P. Wasilewski, R. P. Lin, K. A. Anderson, C. W. Carlson, J. McFadden, D. W. Curtis, D. Mitchell, H. Rème, C. Mazelle, J.-A. Sauvaud, C. d’Uston, S. J. Bauer, P. Cloutier, M. May-hew, D. Winterhalter, and N. F. Ness, Magnetic field and plasma observations at Mars: Initial results of the Mars Global Surevor mission, Science, 279, 1676–1680, doi:10.1126/science.279.5357.1676, 1998.Google Scholar
- Barabash, S. and the ASPERA-3 team, The Analyzer of Space Plasmas and Energetic Atoms (ASPERA-3) for the Mars Express mission, Space Sci. Rev., 126, 113–164, 2006.View ArticleGoogle Scholar
- Barabash, S., A. Fedorov, R. Lundin, and J.-A. Sauvaud, Martian atmospheric erosion rates, Science, 315, 501–503, 2007.View ArticleGoogle Scholar
- Brain, D., J. S. Halekas, R. Lillis, D. Mitchell, R. Lin, and D. Crider, Variability of the altitude of the Martian sheath, Geophys. Res. Lett., 32, doi:10.1029/2005GL023126, 2005.Google Scholar
- Brain, D., S. Barabash, A. Boesswetter, S. Bougher, S. Brecht, G. Chanteur, D. Hurley, E. Dubinin, X. Fang, M. Fraenz, J. Halekas, E. Harnett, M. Holmstrom, E. Kallio, H. Lammer, S. Ledvina, M. Liemohn, K. Liu, J. Luhmann, Y. Ma, R. Modolo, A. Nagy, U. Motschmann, H. Nilsson, H. Shinagawa, S. Simon, and N. Terada, A comparison of global models for the solar wind interaction with Mars, Icarus, 206, 139–151, doi:10.1016/j.icarus.2009.06.030, 2010.View ArticleGoogle Scholar
- Carlsson, E., A. Fedorov, S. Barabash, E. Budnik, A. Grigoriev, H. Gunell, H. Nilsson, J.-A. Sauvaud, R. Lundin, Y. Futaana, H. Holmstrom, H. Andersson, M. Yamauchi, D. Winningham, R. Frahm, J. Sharber, J. Scherrer, A. Coates, D. R. Linder, D. O. Kataria, E. Kallio, H. Koski-nen, T. Säles, P. Riihilä, W. Schmidt, J. Kozyra, J. Luhmann, E. Roelof, D. Williams, S. Livi, C. Curtis, K. C. Hsieh, B. R. Sandel, M. Grande, M. Carter, J.-J. Thocaven, S. McKenna-Lawlor, S. Orsini, R. Cerulli-Irelli, M. Maggi, P. Wurz, P. Bochsler, N. Krupp, J. Woch, M. Fraenz, K. Asamura, and C. Dierker, Mass composition of the escaping plasma at Mars, Icarus, 182, 320–328, 2006.View ArticleGoogle Scholar
- Connerney, J. E. P., M. H. Acuna, P. J. Wasilewski, G. Kletetschka, N. F. Ness, H. Réme, R. P. Lin, and D. L. Mitchell, The global magnetic field of Mars and its implications for crustal evolution, Geophys. Res. Lett., 28, 4015–4018, 2001.View ArticleGoogle Scholar
- Dubinin, E., R. Lundin, M. Franz, J. Woch, S. Barabash, A. Fedorov, D. Winningham, N. Krupp, J.-A. Sauvaud, M. Holmstrom, H. Andersson, and M. Yamauchi, Electric fields within the martian magneto-sphere and ion extraction: ASPERA-3 observations, Icarus, 182, 337–342, 2006.View ArticleGoogle Scholar
- Edberg, N. J. T., M. Lester, S. W. H. Cowley, and A. I. Eriksson, Statistical analysis of the location of the Martian magnetic pileup boundary and bow shock and the influence of crustal magnetic fields, J. Geophys. Res., 113, A08206, doi:10.1029/2008JA013096, 2008.Google Scholar
- Edberg, N. J. T., D. A. Brain, M. Lester, S. W H. Cowley, R. Modolo, M. Franz, and S. Barabash, Plasma boundary variability at Mars as observed by Mars Global Surveyor and Mars Express, Ann. Geophys., 27, 3537–3550, doi:10.5194/angeo-27-3537–2009, 2009.View ArticleGoogle Scholar
- Edberg, N. J. T, H. Nilsson, A. O. Williams, M. Lester, S. E. Milan, S. W. H. Cowley, M. Franz, S. Barabash, and Y. Futaana, Pumping out the atmosphere of Mars through solar wind pressure pulses, Geophys. Res. Lett., 37, L03107, doi:10.1029/2009GL041814, 2010.Google Scholar
- Ergun, R. E., L. Andersson, W K. Peterson, D. Brain, G. T. De-lory, D. L. Mitchell, R. P. Lin, and A. W Yau, Role of plasma waves in Mars’ atmospheric loss, Geophys. Res. Lett., 33, L14103, doi:10.1029/2006GL025785, 2006.View ArticleGoogle Scholar
- Fang, X., M. W Liemohn, A. F Nagy, Y. Ma, D. L. De Zeeuv, J. U. Kozyra, and T. H. Zurbuchen, Pickup oxygen ion velocity space and spatial distribution around Mars, J. Geophys. Res., 113, doi:10.1029/2007JA012736, 2008.Google Scholar
- Fedorov, A., E. Budnik, J.-A. Sauvaud, C. Mazelle, S. Barabash, R. Lundin, M. Acũna, M. Holmström, A. Grigoriev, and M. Yamauchi, Structure of the Martian wake, Icarus, 182, 329–336, 2006.View ArticleGoogle Scholar
- Fränz, M., E. Dubinin, E. Roussos, J. Woch, J. D. Winningham, R. Frahm, A. J. Coates, A. Fedorov, S. Barabash, andR. Lundin, Plasma moments in the Environment of Mars. Mars Express ASPERA-3 observations, Space Sci. Rev., 126, 165–207, doi:10.1007/s11214-006-9115-9, 2006.View ArticleGoogle Scholar
- Fränz, M., E. Dubinin, E. Nielsen, J. Woch, S. Barabash, R. Lundin, and A. Fedorov, Transterminator ion flow in the Martian ionosphere, Planet. Space Sci., 58, 1442–1454, doi:10.1016/j.pss.2010.06.009, 2010.View ArticleGoogle Scholar
- Hoffman, N., White Mars: A new model for Mars’ surface and atmosphere based on CO2, Icarus, 146,326–342, doi:10.1006/icar.2000.6398,2000.View ArticleGoogle Scholar
- Lammer, H., J. F. Kasting, E. Chassefiere, R. E. Johnson, Y. N. Kulikov, and F. Tian, Atmospheric escape and evolution of terrestrial planets and satellites, Space Sci. Rev., 139, 399–436, 2008.View ArticleGoogle Scholar
- Luhmann, J. G., The solar wind interaction with unmagnetized planets—A tutorial, in Washington DC American Geophysical Union Geophysical Monograph Series, 58, 401–411, 1990.Google Scholar
- Lundin, R., A. Zakharov, R. Pellinen, B. Hultqvist, H. Borg, E. Dubinin, S. Barabash, N. Pissarenko, H. Koskinen, and I. Liede, First results of the ionospheric plasma escape from Mars, Nature, 341, 609–612, 1989.View ArticleGoogle Scholar
- Lundin, R., S. Barabash, A. Fedorov, M. Holmstrom, H. Nilsson, J.-A. Sauvaud, and M. Yamauchi, Solar forcing and planetary ion escape from Mars, Geophys. Res. Lett., 35, L09203, doi:10.1029/2007GL032884, 2008a.Google Scholar
- Lundin, R., S. Barabash, M. Holmstrom, H. Nilsson, M. Yamauchi, M. Fraenz, and E. M. Dubinin, A comet-like escape of ionospheric plasma from Mars, Geophys. Res. Lett., 35, doi:10.1029/ 2008GL034811, 2008b.Google Scholar
- Lundin, R., S. Barabash, M. Holmstrom, H. Nilsson, M. Yamauchi, E. M. Dubinin, and M. Fraenz, Atmospheric origin of cold ion escape from Mars, Geophys. Res. Lett., 36, L17202, doi:10.1029/2009GL039341, 2009.View ArticleGoogle Scholar
- Lundin, R., S. Barabash, M. Yamauchi, H. Nilsson, and D. Brain, On the relation between plasma escape and the Martian crustal magnetic field, Geophys. Res. Lett., 38, L02102, doi:10.1029/2010GL046019, 2011.View ArticleGoogle Scholar
- Mitchell, D., R. Lin, H. Rème, D. Crider, P. Cloutier, J. Connerney, M. Acuna, and N. Ness, Oxygen Auger electrons observed in Mars ionosphere, Geophys. Res. Lett., 27, 1871–1874, 2000.View ArticleGoogle Scholar
- Nilsson, H., E. Carlsson, H. Gunell, Y. Futaana, S. Barabash, R. Lundin, A. Fedorov, Y Soobiah, A. Coates, M. Fränz, and E. Roussos, Investigation of the influence of magnetic anomalies on ion distributions at Mars, Space Sci. Rev., 126, 355–372, 2006a.View ArticleGoogle Scholar
- Nilsson, H., M. Waara, S. Arvelius, O. Marghitu, M. Bouhram, Y Ho-bara, M. Yamauchi, R. Lundin, H. Reme, J.-A. Sauvaud, I. Dandouras, A. Balogh, L. M. Kistler, B. Klecker, C. W. Carlson, M. B. Bavassano-Cattaneo, and A. Korth, Characteristics of high altitude oxygen ion energization and outflow as observed by Cluster; a statistical study, Ann. Geophys., 24, 1099–1112, 2006b.View ArticleGoogle Scholar
- Nilsson, H., E. Carlsson, D. Brain, M. Yamauchi, M. Holmström, S. Barabash, R. Lundin, and Y Futaana, Ion escape from Mars as a function of solar wind conditions: A statistical study, Icarus, 206, 40–49, doi:10.1016/j.icarus.2009.03.006, 2010.View ArticleGoogle Scholar
- Nilsson, H., N. J. T. Edberg, G. Stenberg, S. Barabash, M. Holmstrom, Y Futaana, R. Lundin, and A. Fedorov, Heavy ion escape from Mars, influence from solar wind conditions and crustal magnetic fields, Icarus, 215, 475–484, doi:10.1016/j.icarus.2011.08.003, 2011.View ArticleGoogle Scholar
- Slapak, R., H. Nilsson, M. Waara, M. André, G. Stenberg, and I. A. Bargh-outhi, O+ heating associated with strong wave activity in the high altitude cusp and mantle, Ann. Geophys., 29, 931–944, doi:10.5194/angeo-29–931–2011, 2011.View ArticleGoogle Scholar
- Squyres, S. W, J. P. Grotzinger, R. E. Arvidson, J. F. Bell, W Calvin, P. R. Christensen, B. C. Clark, J. A. Crisp, W. H. Farrand, K. E. Herkenhoff, J. R. Johnson, G. Klingelhofer, A. H. Knoll, S. M. McLennan, H. Y. McSween, R. V. Morris, J. W. Rice, R. Rieder, and L. A. Soderblom, In situ evidence for an ancient aqueous environment at Meridiani Planum, Mars, Science, 306, 1709–1714, doi:10.1126/science.1104559, 2004.View ArticleGoogle Scholar
- Trotignon, J. G., C. Mazelle, C. Bertucci, and M. H. Acuna, Martian shock and magnetic pile-up boundary positions and shapes determined from the Phobos 2 and Mars Global Surveyor data sets, Planet. Space Sci., 54, 357–369, 2006.View ArticleGoogle Scholar
- Verigin, M. I., N. M. Shutte, A. A. Galeev, K. I. Gringauz, G. A. Kotova, A. P. Remizov, H. Rosenbauer, P. Hemmerich, S. Livi, A. K. Richter, I. Apathy, K. Szego, W. Riedler, K. Schwingenschuh, M. Steller, and Y. G. Yeroshenko, Ions of planetary origin in the Martian magneto-sphere (Phobos 2/TAUS experiment), Planet. Space Sci., 39, 131–137, 1991.View ArticleGoogle Scholar
- Vignes, D., C. Mazelle, H. Reme, M. Acuña, J. Connerney, R. Lin, D. Mitchell, P. Cloutier, D. Crider, and N. Ness, The solar wind interaction with Mars: locations and shapes of the bow shock and magnetic pile-up boundary from the observations of the MAG/ER experiment onboard Mars Global Surveyor, Geophys. Res. Lett., 27, 49–52, 2000.View ArticleGoogle Scholar
- Waara, M., S. Slapak, H. Nilsson, G. Stenberg, M. Andre, and I. A. Barghouthi, Statistical evidence for O+ energization and outflow caused by wave-particle interaction in the high altitude cusp and mantle, Ann. Geophys., 29, 945–954, doi:10.5194/angeo-29-945-2011, 2011.View ArticleGoogle Scholar
- Yamauchi, M., Y. Futaana, A. Fedorov, R. A. Frahm, J. D. Winningham, E. Dubinin, R. Lundin, S. Barabash, M. Holmström, C. Mazelle, J. Sauvaud, T. L. Zhang, W. Baumjohann, A. J. Coates, and M. Fraenz, Comparison of accelerated ion populations observed upstream of the bow shocks at Venus and Mars, Ann. Geophys., 29, 511–528, doi:10.5194/angeo-29-511-2011, 2011.View ArticleGoogle Scholar