Model results for the midlatitude daytime E  region: EUV ionization rate and a (NO⁺ ) relationship

A. V. Mikhailov

Institute of Terrestrial Magnetism, Ionosphere and Radio Wave Propagation, Russian Academy of Sciences, Troitsk, Moscow Region, Russia

Received February 22, 2000

Contents

Abstract

1. Introduction

Midlatitude ionospheric E layer has been studded for many years, nevertheless there are still problems with its description. While existing empirical N_mE models like IRI [Bilitza, 1990] reproduce regular N_mE variations with a sufficient accuracy, a theoretical approach based on modern EUV solar flux models and commonly accepted dissociative recombination rate constants for NO⁺ and O₂⁺ ions usually underestimates N_mE by 30-40% [Buonsanto et al., 1995; Titheridge, 1997]. Because of the square-law loss process this 40% deficit in N_mE implies a 100% increase in the ionization rate at the E -layer peak (105-110 km). Some approaches have been proposed to overcome this problem. Ivanov-Kholodny and Nusinov [1979] used low a( NO⁺) value by Mul and McGowan [1979] along with [O₂] scale height strong seasonal variations in the 100-110 km height range. Antonova et al. [1996] took into account vibrationally excited NO⁺ and O₂⁺ ions and this allowed them to explain N_mE and h_mE seasonal variations. Titheridge [1996, 1997] using a full allowance for secondary ionization with EUV radiations down to 25 Å and a 33% additional increase of the radiation with l< 150 Å in the EUVAC model [Richards et al., 1994 could describe the observed N_mE values. Although there is large uncertainty with EUV fluxes in this spectrum range, such an increase of the EUV flux in the 50-150 Å range seems unjustified as it will be shown below. The fluxes in this spectrum range have already been tripled in the EUVAC model [Richards et al., 1994] compared to the reference spectrum F74113 measured on April 23, 1974 (F_10.7=74), and this factor is kept in the model for all levels of solar activity.

Calculated NO⁺/ O₂⁺ ratio is another problem with the E region theoretical modeling [Buonsanto et al., 1995; Titheridge, 1997]. Usually the calculated NO⁺/ O₂⁺ ratio is less compared to rocket observations in the E region [Danilov, 1994; Danilov and Semenov, 1978; Danilov and Smirnova, 1995, and references therein]. Buonsanto et al. [1995] and Titheridge [1997] analyzing this problem suggest that our understanding of the NO⁺ chemistry may be incomplete.

The aim of the paper is to compare E region calculations with the Millstone Hill N_e(h) observations given by Buonsanto et al. [1995] and make a conclusion on EUV model fluxes and a( NO⁺) dissociative recombination rate coefficient necessary to obtain the observed N_mE for different levels of solar activity. A possible way to get NO concentrations providing the observed NO ⁺/ O₂⁺ ratio in model calculations is proposed as well.

2. Ionospheric Model

Midlatitude regular ionospheric E layer is known to be controlled by photochemical processes. A two-component model by Nusinov [Bruevich and Nusinov, 1984; Nusinov, 1984, 1992] with further corrections by Nusinov et al. [1999] is used to calculate EUV fluxes in 48 wavelength intervals with 8 l 1050 Å. The intensity of the EUV fluxes in this model depend on slowly varying F_bg emission at 10.7 cm wavelength and on radio emission from active areas on the Sun, F_10.7 - F_bg [Nusinov, 1984]. The background F_bg emission varies from F_bg = 60-65 (in 10^-22 W m^-2 Hz^-1 ) at solar minimum to F_bg 120 at solar maximum. The X range ( l< 100 Å) includes 13 wavelength bins. Ionization by a strong Lya line ( l=1216  Å) is taken into account in accordance with the model by Katjushina et al. [1991]. Although this emission gives only around 1% of the total ionization rate at the E layer peak it becomes important at lower heights. For further discussion Table 1 gives fluxes in accordance with the Nusinov and EUVAC models in the same wavelength bins as used in the EUVAC model. Solar minimum of April 23, 1974 ( F_10.7=74, F_bg=67) when the F74113 reference spectrum was measured and solar maximum conditions with F_10.7=200, F_bg=100 corresponding to the EUVAC model for P=200 are compared in Table 1. Parameter P = (FA_10.7+F_10.7)/2 is used as the proxy in the EUVAC model [Richards et al., 1994], FA_10.7 being an 81-day average of the daily F_10.7 index.

Our usual model calculations (a standard mode) are based on the photoionization and photoabsorption cross sections mostly from Torr et al. [1979]. Photoionization cross section for O⁺(⁴S), O⁺(²P) and O⁺(²D) production were taken in accordance with Richards and Torr [1988] with allowance for secondary ionization for l< 250 Å in accordance with Ivanov-Kholodny and Nikoljsky [1969]. Their approach is based on the experimental fact that each act of ionization by short-wave UV or X ray emission requires e amount of energy. This e = 32 eV for the emission with l 200 Å. Then the effective ionization cross sections is defined as

(1)

where E is the energy of the initial photon, and s_iph is the photoionization cross section, l is in Å. For a comparison the same calculations were made with cross sections given by Fennely and Torr [1992] with taking into account secondary ionization for l< 400 Å as proposed by Titheridge [1996].

The list of chemical reactions used in the model is given in Table 2. Reaction rates were used as in Buonsanto et al. [1992], McEwan and Phillips [1975], Oppenheimer et al. [1977], Torr and Torr [1979], and McFarland et al. [1973].

Neutral composition (O, O₂, N₂, N) and temperature T_n were used from MSIS 86 thermospheric model [Hedin, 1987]. Nitric oxide, NO is very important for E layer chemistry. It was found by fitting the calculated NO⁺/ N_e and O₂+/N_e ratios in the 100-120 km height range to the ion composition model by Danilov and Smirnova [1995] which is based on rocket measurements. An effective scale height of the [NO] height distribution inferred at 115 km was used to extrapolate the [NO] profile above 120 km.

Millstone Hill daytime observations for three winter days February 5, 1992, November 10, 1988, and January 15, 1985 as they are given in Buonsanto et al. [1995] were used for a comparison with our model calculations. These days represent quiet time E region for solar minimum (January 15, 1985, F_S=74.7 ), middle (November 10, 1988, F_S=175.3 ), and high solar activity (February 5, 1992, F_S=207 ) conditions, F_S being a three month average F_10.7.

3. Calculations

Three types of model calculations were made for two sets (see above) of photoionization and photoabsorption cross sections: (i) with standard EUV fluxes from Nusinov model and T_e=T_n in the E region; (ii) with increased by 4 times fluxes in the 50-100 Å wavelength bin and T_e=T_n, and (iii) with standard model fluxes, but T_e=2.5T_n in the E layer peak around 110 km. An increase of T_e over T_n with T_e/T_n=3 - 5 is observed by probe measurements in the daytime E region [Duhau and Azpiazu, 1985]. As the dissociative recombination rate coefficients for NO⁺ and O₂⁺ ions depend on T_e this effect may be important. In accordance with Duhau and Azpiazu [1985] a gaussian type dependence was used to specify the T_e/T_n height distribution with the peak at 110 km. Calculations in comparison with Millstone Hill observations are given in Figure 1 for high solar activity (February 5, 1992). The standard calculations give N_mE by 40% lower than the observed one similar to FLIP (around a 50% deficiency) and Millstone Hill photochemical model results [Buonsanto et al., 1995]. The 50-100 Å flux increased by a factor of 4 does provide the observed N_mE, although h_mE is shifted to higher altitudes. Close results but with a more realistic h_mE may be obtained with the standard EUV model fluxes and T_e/T_n=2.5 at 110 km.

Calculations with cross sections by Fennelly and Torr [1992] and Titheridge [1996] (Figure 1 middle box) give the results which are very close to our standard model calculations (Figure 1, top) although our approach of taking into account the secondary ionization effects in accordance with the Ivanov-Kholodny and Nikoljsky [1969] approach is much simpler than the Titheridge [1996] one. The 50-100 Å flux increased by 4 times shifts h_mE to higher altitudes as in Figure 1 (top) and the valley is not developed in this case. Contrary, the N_e(h) profile calculated with T_e/T_n=2.5 demonstrates a well defined valley.

Relative ion composition (NO⁺/N_e and O₂+/N_e ratios) fitted to the Danilov and Smirnova [1995] model by varying [NO] are shown in Figure 1 (bottom). It is interesting to note that [NO⁺] is higher than [O₂⁺] above 105 km, but the ratio is inverse at lower heights. This crossing point shifts to lower heights as the solar activity declines (see Figures 2-3). The reason for such variations is out of the scope of this paper, but the corresponding [NO] height profiles are discussed below.

Similar results are obtained for middle solar activity (Figure 2). Although a factor of 4 for the 50-100 Å flux provides the observed N_e around 110 km, the N_e(h) profile is uplifted as a whole and the valley is not well developed with the Fennelly, Torr, and Titheridge cross sections (Figure 2, middle box). Calculations with T_e/T_n=2.5 look as more realistic with both sets of cross sections (Figure 2, top and middle boxes). The [NO⁺] ions dominate over [O₂⁺] in the 100-120 km height range in accordance with the Danilov and Smirnova model.

General conclusions on the results for solar minimum (Figure 3) are the same as above. The only difference is that a factor of 4 for the 50-100 Å flux is not sufficient to get the observed N_e around 110 km, while a factor of 2.5 for T_e/T_n may be too high and should be decreased. Such a decrease of T_e/T_n ratio does take place at low solar activity [Duhau and Azpiazu, 1985]. It should be stressed that the Danilov and Smirnova [1995] model does not show any relative ion composition variations around 110 km (cf. Figures 1-3, bottom boxes) in the course of solar cycle (around 55% for NO⁺/N_e and 45% for O₂+/N_e). This implies a corresponding small [NO] variations with solar activity in the E layer maximum (see below).

The other possibility to decrease the NO⁺ ion recombination rate and solve the problem with low calculated N_mE is to use low dissociative recombination rate coefficient a( NO⁺)=2.3 10^-7 (300/T_e)^0.5 by Mul and McGowan [1979]. Calculations with this rate coefficient provide the observed N_e around 110 km with T_e=1.5T_n and standard model 50-100 Å fluxes. The results are very close to those obtained with a( NO⁺)=4.5 10^-7 (300/Te)^0.83, T_e/T_n=2.5 at 110 km. Both curves are given for a comparison in Figure 4 for three days considered. A well defined h_mE at 107-110 km and a valley at 120-125 km may be obtained in this case. The standard set of cross sections was used in these calculations.

Each set of calculations was made with [NO] fitted to provide the Danilov and Smirnova [1995] model NO ⁺/N_e and O ₂⁺/N_e values in the 100-120 km height range. Above 120 km [NO] was extrapolated with an effective scale height found at 115 km. The calculated [NO] distributions are given in Figure 5 for three days in question. Only calculations which provide N_e at 110 km close to the IS observations are shown in Figure 5. The calculated [NO] height variation is seen to be a Chapman type layer with the peak around 107 km and a scale height of 10 2 km. A dependence of [NO] _max on solar activity is seen with [NO] _max on February 5, 1992 being higher than on January 15, 1985.

4. Discussion

There are two ways to overcome the problem with low calculated N_mE : either to increase the photoionization rate in the E layer peak or to decrease the recombination rate for NO ⁺ being the major ion in the E region.

Let us consider the first possibility. For the classic daytime Chapman E layer the photoionization rate in its peak may be written as

(2)

(2) To increase q_max one may increase I (the ionization flux) or decrease H (the scale height of the ionized atmospheric neutral species). In their earlier monograph Ivanov-Kholodny and Nusinov [1979] proposed to consider strong seasonal variations of molecular oxygen scale height in the E region with small winter H(O₂ ) values. Along with this they used low a( NO⁺ ) by Mul and McGowan [1979]. This approach allowed them to explain many morphological features of the E layer. Unfortunately low winter H(O₂ ) results in lower winter h_mE compared to summer one. On one hand this contradicts to incoherent scatter observations made in Kharkov (49.43^o N, 36.92^o E) and presented in the monograph by Antonova et al. [1996] where winter h_mE values are higher than summer ones. On the other hand according to MSIS 86 thermospheric model [Hedin, 1987] the concentration of major neutral (O₂, N₂, O) species is higher in winter at midlatitudes in the E region and this should result in higher winter h_mE values.

The other possibility is to increase I in (2). The ionization rate should be doubled at the E layer peak if the Nusinov [1992] EUV model is used (Figures 1-3, T_e=T_n ). This cannot be done for two UV lines with l=977 Å (CIII) and 1026 Å ( HLyb ) producing the main ionization in the E region as the present day accuracy of measurements in the UV range of spectrum is high enough [Woods et al., 1998]. On the other hand there is large uncertainty with EUV fluxes for l< 150 Å. Initial fluxes have been tripled for the l = 50-150 Å interval in the EUVAC model [Richards et al., 1994], but an additional increase up to factor of 4 is required to get the experimental N_mE values [Titheridge, 1997]. The same increase of fluxes with l = 50-100 Å by a factor of 4 is necessary for the Nusinov model to obtain the observed N_mE (Figures 1-3). Such an increase of the soft X ray radiation changes in favor of X ray the proportion between UV and X ray contributions to the E layer ionization rate. According to [Titheridge, 1997] about 66% of the E region ionization is produced by radiation with l< 150 Å. The X ray contribution will be even larger if to use the required factor of 4 for this wavelength interval in the EUVAC model. In case of the Nusinov EUV model such a 4 times increase would give a 55% X ray contribution to the total ionization rate at 110 km. It is possible to show that such an increase of the X ray contribution to the E layer ionization rate leads to a contradiction with ionospheric observations.

One of the ways to estimate the X ray contribution to the E layer total ionization rate is to analyze N_mE variations during solar flares [Ivanov-Kholodny et al., 1976, 1977]. According to rocket and satellite observations strong increase of the X ray emission takes place in 1-8, 8-20, 44-60-Å spectrum intervals during solar flares while only small changes of UV radiation were observed [Chubb et al., 1957]. Therefore, we may suppose for our estimates that UV ionization rate does not change during solar flares. The I_x flux in the 8-165 Å spectrum range which ionizes the E region is related to the 8-20 Å flux as I_x (I_8-20)^0.5 [Ivanov-Kholodny et al., 1976]. Regular observations of X ray emission in the ionization chambers on board the satellites are available and published in Solar Geophysical Data. For strong flares analyzed by Ivanov-Kholodny et al. [1977] the I_8-20 emission measured on board the SOLRAD 9 and 10 satellites increased by 5-25 times. Therefore, for our estimates we may take an average factor of 3.6 for the I_x increase during the flare events considered. Then a proposed 4 times increase of X ray emission with a 55-66% (mean 60%) X ray contribution to the total E layer ionization rate results in

(3)

where q₀ and q_f - total E layer ionization rate for quiet and flare conditions, and F_acI_x = 3.6 is an average X ray emission increase. Therefore, we get q_f = 2.56q₀. On the other hand, the observed N_mE variations for the flares considered [Ivanov-Kholodny et al., 1977] give on average q_f= (1.44-1.60)q₀ with lower value for winter and larger one for summer periods. This is much less than a factor of 2.56 obtained for a 4 times increased X ray emission required to get the observed N_mE in model calculations. Thus this proposition should be ruled out. The observed q_f = (1.44 - 1.60)q₀ implies only a 17-23% X ray contribution to the total E  region ionization rate. A 18% of X ray relative contribution was obtained by Ivanov-Kholodny and Nusinov [1979] for medium solar activity. The EUV model by Nusinov provides the required X ray relative contribution while the EUVAC model strongly overestimates it (see Table 1 for the 50-100 Å bin) not to mention an additional increase of the flux in this wavelength bin proposed by Titheridge [1997]. Therefore, there is no way to solve the problem of low calculated N_mE at the expense of the photoionization rate increase. It should be mentioned that according to recent soft X ray (20-100 Å) measurements on board the SNOE satellite [Bailey et al., 1999] the extrapolation of the measured irradiance to the solar minimum gives values which are much less then the EUVAC predictions.

Let us consider the other possibility - a decrease of a( NO⁺). The N_mE observations can be well reproduced in our calculations if T_e > T_n is accepted in the daytime E region in accordance with the probe measurements [Duhau and Azpiazu, 1985]. A moderate T_e/T_n=2.5 ratio is required at the E layer peak (around 110 km) with a conventional a( NO⁺)=4.5 10^-7 (300/T_e)^0.83 to obtain the observed N_mE (Figures 1-3). The required T_e/T_n ratio may be even 1.5 if a small a( NO⁺) = 2.3 10^-7 (300/T_e)^0.5 rate coefficient by Mul and McGowan [1979] is used (Figure 4). Unlike Duhau and Azpiazu [1985] who found strong dependence of T_e/T_n ratio on solar activity, practically an unchanged T_e/T_n is required in our calculations at all levels solar activity. Physical mechanism of such T_e heating at midlatitudes is not clear yet [Duhau and Azpiazu, 1985]. It should be mentioned that no difference between T_e and T_i (which coincides with T_n in the midlatitude E region) is observed by the incoherent scatter method at midlatitudes. Such T_e enhancement over T_i due to the relative electron-ion drift velocity takes place in the auroral zone according to EISCAT observations [Igarashi and Schlegel, 1987]. Nevertheless a possibility of T_e being higher T_n seems very promising in solving the problem with low calculated q/a_eff for the daytime E layer.

Our calculations (Figures 1-3, top boxes) reproduce a reasonable depth of the E-F1 valley. According to the IRI 90 model [Bilitza, 1990] the valley depth ( N_val/N_mE ) is 10-12% for the conditions in question. The valley depth of 13-15% are given by the empirical models [Chasovitin et al., 1983; Fatkullin et al., 1981]. Kharkov incoherent scatter observations [Tkachev, 1981] give the depth of the noon valley of 12-18%. The calculated N_e(h) profiles (Figures 1-3, top boxes, T_e=2.5T_n ) have the valley depth of 10-15%. The profiles calculated with F_acX=4 for the 50-100 Å wavelength interval have show an undeveloped valley. Normal valley with the depth of 10-13% provide the calculations with T_e=1.5T_n, F_acX=1 and a( NO⁺) by Mul and McGowan [1979, (Figure 4)]. Close results are obtained with the Fennelly and Torr [1992], and Titheridge [1996] cross sections (Figures 1-3, middle boxes). Therefore, a proper EUV spectrum is more important for development of a normal valley than different sets of cross sections used in calculations.

Problems with calculated NO⁺/ O₂⁺ ratio [Buonsanto et al., 1995; Titheridge, 1997] which contradicts to rocket measurements in the E region mostly is related with a correct specification of the [NO] distribution. In our approach we make a self-consistent [NO] fitting to get NO⁺/N_e and O₂⁺/N_e ratios as in the Danilov and Smirnova [1995] model which is based on rocket observations. The calculated [NO] profiles (Figure 5) demonstrate small variations with solar activity, the [NO] peak density at 107 km being larger only by 40% at high solar activity. This is much less than solar cycle variations (4-5 times for winter) used by Titheridge [1997] in his analysis. The other difference is in the NO peak density which is by 10-2.5 times less in his model when we pass from low to high solar activity. On the other hand a theoretical model by Gerard et al. [1997] gives the NO peak values which are much closer to our results. Close NO values were observed by SNOE satellite at geomagnetic latitudes of Millstone Hill for a quiet ( Ap=12 ) day following a period of moderate disturbance with Ap=28 [Solomon et al., 1999]. However, it should be stressed that the obtained [NO] solar cycle variation is an estimate based on the model [Danilov and Smirnova, 1995] ion composition which demonstrates very small solar activity variation in the E region.

The effective scale height inferred at 115 km from the calculated [NO] distribution is about 8-12 km depending on the calculation mode. This is close to H( NO)=8- 9 km used by Titheridge [1997, and references therein] but unlike his dependence on solar activity there is a tendency for H( NO ) to be less at solar maximum (Figure 5, top and middle boxes). Similar dependence of H (NO) at 120 km on solar activity may be found in Gerard et al. [1997].

5. Conclusions

The main results of our analysis are following:

1. The observed at Millstone Hill daytime N_mE may be reproduced in model calculations provided the 50-100 Å flux is increased by 4 times in the Nusinov [1992] EUV model. The same increase is required in case of the EUVAC model as was proposed by Titheridge [1997]. But such an increase distorts the proportion between UV and X ray contributions in favor of X ray (around 60%) to the total photoionization rate of the E region. This leads to a contradiction with N_mE observations during solar flares. As was shown by [Ivanov-Kholodny and Nusinov, 1979] the X ray contribution to the E layer total ionization rate for quiet conditions is around 20% depending on solar activity, our analysis gives similar estimate. The EUV model by Nusinov [1992] provides this contribution while the EUVAC model (where the 50-150 Å flux was tripled) does not. Therefore, a proposition to obtain the observed N_mE values in model calculations at the expense of X ray emission increase should be ruled out.

2. The other way to obtain the observed N_mE is to reduce a( NO⁺ ). One of the way to do this is to take into account T_e >T_n in the E region as it follows from probe measurements Duhau and Azpiazu, 1985]. A moderate T_e/T_n=2.5 ratio at the E layer peak (around 110 km) along with a conventional a( NO⁺) and the Nusinov EUV model is required to get the observed daytime N_mE values at different levels of solar activity. The same results may be obtained even with lower T_e/T_n=1.5 ratio and a( NO⁺ ) by Mul and McGowan [1979]. Both calculations reproduce a reasonable depth of the E-F1 valley with N_val/N_mE = 10-15% close to the empirical ionospheric models. But the reality of T_e > T_n in the midlatitude daytime E region is questionable as these probe results are not confirmed by incoherent scatter observations.

3. The E-layer ion composition with [NO⁺] > [O₂⁺] corresponding to rocket observations can be reproduced in model calculations by using an appropriate [NO] height distribution. These [NO] profiles may be obtained by fitting the calculated ion composition in the 100-120 km height range to the model one based on rocket measurements. The calculated [NO] is a Chapman type layer with a peak around 107 km and a scale height of 8-12 km inferred at 115 km. The [NO] peak density varies with solar activity being by 40% larger at F_10.7=207 compared to solar minimum ( F_10.7=75) conditions. The obtained [NO] solar cycle variation should be considered as an estimate based on model [Danilov and Smirnova, 1995] ion composition variations, the latter do not show any solar activity variation at the E layer maximum around 110 km.

Acknowledgments

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