Positive ion composition in the lower ionosphere at high latitudes during MAP/WINE

Krankowsky, D.; Lämmerzahl, P.; Götzelmann, A.; Friedrich, Martin; Torkar, K.

doi:10.1016/0021-9169(87)90020-1

Cited by 15 publications

(2 citation statements)

References 35 publications

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“…The NO + ion has been found to be the most abundant ion in this altitude range by rocket-borne mass spectrometers (e.g. Bragin and Shamakhov, 1982;Krankowsky et al, 1987). Negative ions are negligible at these altitudes (e.g.…”

Section: Channels 1+ and 1− Ion And Electron Densitiesmentioning

confidence: 99%

Mass analysis of charged aerosol particles in NLC and PMSE during the ECOMA/MASS campaign

et al. 2009

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Abstract. MASS (Mesospheric Aerosol Sampling Spectrometer) is a multichannel mass spectrometer for charged aerosol particles, which was flown from the Andøya Rocket Range, Norway, through NLC and PMSE on 3 August 2007 and through PMSE on 6 August 2007. The eight-channel analyzers provided for the first time simultaneous measurements of the charge density residing on aerosol particles in four mass ranges, corresponding to ice particles with radii <0.5 nm (including ions), 0.5-1 nm, 1-2 nm, and >3 nm (approximately). Positive and negative particles were recorded on separate channels. Faraday rotation measurements provided electron density and a means of checking charge density measurements made by the spectrometer. Additional complementary measurements were made by rocket-borne dust impact detectors, electric field booms, a photometer and ground-based radar and lidar. The MASS data from the first flight showed negative charge number densities of 1500-3000 cm −3 for particles with radii >3 nm from 83-88 km approximately coincident with PMSE observed by the ALWIN radar and NLC observed by the ALOMAR lidar. For particles in the 1-2 nm range, number densities of positive and negative charge were similar in magnitude (∼2000 cm −3 ) and for smaller particles, 0.5-1 nm in radius, positive charge was dominant. The occurrence of positive charge on the aerosol particles of the smallest size and predominately negative charge on the particles of largest size suggests that nucleCorrespondence to: S. Knappmiller (knappmil@colorado.edu) ation occurs on positive condensation nuclei and is followed by collection of negative charge during subsequent growth to larger size. Faraday rotation measurements show a bite-out in electron density that increases the time for positive aerosol particles to be neutralized and charged negatively. The larger particles (>3 nm) are observed throughout the NLC region, 83-88 km, and the smaller particles are observed primarily at the high end of the range, 86-88 km. The second flight into PMSE alone at 84-88 km, found only small number densities (∼500 cm −3 ) of particles >3 nm in a narrow altitude range, 86.5-87.5 km. Both positive (∼2000 cm −3 ) and negative (∼4500 cm −3 ) particles with radii 1-2 nm were detected from 85-87.5 km.

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Section: Channels 1+ and 1− Ion And Electron Densitiesmentioning

confidence: 99%

Mass analysis of charged aerosol particles in NLC and PMSE during the ECOMA/MASS campaign

et al. 2009

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“…The applied model describes and explains (Danilov and Smirnova, 1993, 1994 changes in the f + parameter, the transit height, h f +=1 , and α eff caused by strong ionisation sources and calculated from measurements in various geophysical situations (Johannessen and Krankowsky, 1972;Arnold, 1980;Kopp et al, 1985;Krankowsky et al, 1987;Nacisi et al, 1971;Derblom and Laddel, 1973;Brekke et al, 1985). Smirnova (1982Smirnova ( , 1983a chemical scheme.…”

Section: Barabash Et Al: Influence Of Water Vapour On the Height mentioning

confidence: 99%

Influence of water vapour on the height distribution of positive ions, effective recombination coefficient and ionisation balance in the quiet lower ionosphere

2014

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Abstract. Mesospheric water vapour concentration effects on the ion composition and electron density in the lower ionosphere under quiet geophysical conditions were examined. Water vapour is an important compound in the mesosphere and the lower thermosphere that affects ion composition due to hydrogen radical production and consequently modifies the electron number density. Recent lowerionosphere investigations have primarily concentrated on the geomagnetic disturbance periods. Meanwhile, studies on the electron density under quiet conditions are quite rare. The goal of this study is to contribute to a better understanding of the ionospheric parameter responses to water vapour variability in the quiet lower ionosphere. By applying a numerical D region ion chemistry model, we evaluated efficiencies for the channels forming hydrated cluster ions from the NO + and O + 2 primary ions (i.e. NO + .H 2 O and O + 2 .H 2 O, respectively), and the channel forming H + (H 2 O) n proton hydrates from water clusters at different altitudes using profiles with low and high water vapour concentrations. Profiles for positive ions, effective recombination coefficients and electrons were modelled for three particular cases using electron density measurements obtained during rocket campaigns. It was found that the water vapour concentration variations in the mesosphere affect the position of both the Cl + 2 proton hydrate layer upper border, comprising the NO + (H 2 O) n and O + 2 (H 2 O) n hydrated cluster ions, and the Cl + 1 hydrate cluster layer lower border, comprising the H + (H 2 O) n pure proton hydrates, as well as the numerical cluster densities. The water variations caused large changes in the effective recombination coefficient and electron density between altitudes of 75 and 87 km. However, the effective recombination coefficient, α eff , and electron number density did not respond even to large water vapour concentration variations occurring at other altitudes in the mesosphere. We determined the water vapour concentration upper limit at altitudes between 75 and 87 km, beyond which the water vapour concentration ceases to influence the numerical densities of Cl + 2 and Cl + 1 , the effective recombination coefficient and the electron number density in the summer ionosphere. This water vapour concentration limit corresponds to values found in the H 2 O-1 profile that was observed in the summer mesosphere by the Upper Atmosphere Research Satellite (UARS). The electron density modelled using the H 2 O-1 profile agreed well with the electron density measured in the summer ionosphere when the measured profiles did not have sharp gradients. For sharp gradients in electron and positive ion number densities, a water profile that can reproduce the characteristic behaviour of the ionospheric parameters should have an inhomogeneous height distribution of water vapour.

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Photochemistry of Ions at D-region Altitudes of the Ionosphere: A Review

Павлов

2013

Surv Geophys

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Positive ion composition in the lower ionosphere at high latitudes during MAP/WINE

Cited by 15 publications

References 35 publications

Mass analysis of charged aerosol particles in NLC and PMSE during the ECOMA/MASS campaign

Mass analysis of charged aerosol particles in NLC and PMSE during the ECOMA/MASS campaign

Influence of water vapour on the height distribution of positive ions, effective recombination coefficient and ionisation balance in the quiet lower ionosphere

Photochemistry of Ions at D-region Altitudes of the Ionosphere: A Review

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