Scott M. Bailey, LWS Workshop March 24, 2004
The Observed Response of the Lower Thermosphere to Solar Energetic
Inputs
Scott M. Bailey, Erica M. Rodgers, Justin Yonker
Geophysical Institute
University of Alaska
Charles A. Barth, Daniel N. Baker
Laboratory for Atmospheric and Space Physics
University of Colorado
Scott M. Bailey, LWS Workshop March 24, 2004
Abstract
The production of nitric oxide is a key response of the upper atmosphere to solar energy deposition. NO plays a strong role in the thermospheric energy balance as it emits efficiently in the infrared, it is the terminal ion in the lower ionosphere, and if transported to lower altitudes will catalytically destroy ozone. NO is primarily produced through the reaction of excited atomic nitrogen with molecular oxygen. One of the primary loss mechanisms of NO is photo-dissociation by solar ultraviolet irradiance. In order to produce the excited atomic nitrogen atom, the strong N2 molecular bond must be broken. At low latitudes, solar soft X-ray irradiance is the energy source that leads to NO. At high latitudes, auroral electrons and the energetic secondary electrons provide the source of energy that leads to the large amounts of NO observed there. Coupling between latitude regions may occur as high latitude NO is transported by winds to lower latitude.
In this talk we describe observations of NO from the Student Nitric Oxide Explorer (SNOE). SNOE obtained global observations of lower thermospheric NO from February 1998 through December 2003. We will present case studies of the observed response to large auroral storms. The SNOE observations show that auroral energy deposition produces a significant global effect on the upper atmosphere.
Scott M. Bailey, LWS Workshop March 24, 2004
Nitric Oxide — Why it is important?
Present in the thermosphere - maximum density near 110 km:• Abundance — several times 10-4 mixing ratio at 130 km• Highly variable — factor of ten — 27 day and 11 year variation• Always larger in the auroral region (max at 65° geomagnetic
latitude)
Present in the mesosphere - minimum density near 75 km:• Abundance — several times 10-9 mixing ratio at 70 km• Transport downward from the lower thermosphere into the
mesosphere— Particularly during the winter polar night
Odd nitrogen reacts with odd oxygen: NO + O3 NO2 + O2
NO2 + O NO + O2
Odd nitrogen controls the composition of the lower Ionosphere:NO + O2
+ NO+ + O2
N + O2+ NO+ + O
NO+ + e N + O
Nitric Oxide is the most important cooling mechanism in the lower thermosphere:
• Heteronuclear molecule has a permanent electric dipole moment
— Infrared cooling in the 5.33 m band— Controls temperature in the critical 120 km region
Scott M. Bailey, LWS Workshop March 24, 2004
Production of Nitric Oxide
NO is primarily created through the reaction of excited atomic nitrogen with molecular oxygen:
N(2D) + O2 → NO + O
A major source of excited atomic nitrogen is produced through energetic electron impact with molecular nitrogen:
e* + N2 → N(2D) + N + e*
Destruction of Nitric Oxide
NO is primarily destroyed through the reaction with ground state atomic nitrogen:
NO + N(4S) → N2 + O
NO is also destroyed through photodissociation:NO + h → N(4S) + O
Note that this reaction is doubly effective since it creates a ground state N atom which can also destroy NO.
The effective lifetime of an NO molecule is about 1 day under sunlit conditions.
Scott M. Bailey, LWS Workshop March 24, 2004
So where do the energetic electrons come from?
Two sources:• Photoelectrons – solar soft X-ray irradiance, < 10 nm• Precipitating auroral electrons
Scott M. Bailey, LWS Workshop March 24, 2004
SNOE obtains global observations of nitric oxide
Polar Orbit – constant local time near 11AM/PM
15 orbits per day - observations are obtained at all latitudes and 15 longitudes (same local time) each day
Spinning satellite – altitude profiles from 0 to 200 km, NO densities are obtained from 95 to 150 km
SNOE UVS observes 215, 237 nm fluorescently scattered solar radiance – NO is only measured at locations which are illuminated by the sun.
Scott M. Bailey, LWS Workshop March 24, 2004
SNOE observations show that NO responds to varying solar activity as expected.
Low latitude profiles sorted by F10.7
High latitude profiles sorted by AP
Note that larger concentrations of NO are observed at the high latitudes.
Scott M. Bailey, LWS Workshop March 24, 2004
SNOE observations show significantly larger amounts of NO at high latitudes.
Scott M. Bailey, LWS Workshop March 24, 2004
Even if data for days of low auroral activity are considered, SNOE observations show larger amounts of NO at high latitudes.
Scott M. Bailey, LWS Workshop March 24, 2004
A one-dimensional chemical model reproduces observed equatorial altitude profiles
Model Incorporates:• Solar soft X-ray irradiance, < 20 nm, measured by SNOE• Relevant photochemistry, 35 reactions• Vertical diffusion• MSIS neutral atmosphere, GLOW energetic electron transport
code
Scott M. Bailey, LWS Workshop March 24, 2004
The chemical model reproduces observed equatorial NO densities for 935 days
SNOE ObservationsModel Predictions
Scott M. Bailey, LWS Workshop March 24, 2004
Northern WinterSouthern Summer
Solstice
Northern WinterSouthern Summer
Solstice
SNOE observations for 935 days show large amounts of NO near polar regions and sporadic enhancements at all latitudes.
Geo
grap
hic
Latit
ude
Scott M. Bailey, LWS Workshop March 24, 2004
Northern WinterSouthern Summer
Solstice
Northern WinterSouthern Summer
Solstice
The photochemical model can be used to calculate the global distribution of NO produced by solar soft x-rays.
Geo
grap
hic
Latit
ude
Scott M. Bailey, LWS Workshop March 24, 2004
Geo
grap
hic
Latit
ude
Geo
grap
hic
Latit
ude
Scott M. Bailey, LWS Workshop March 24, 2004
Northern WinterSouthern Summer
Solstice
Northern WinterSouthern Summer
Solstice
By subtracting the calculated NO produced by solar soft x-rays from the observations, we determine the global distribution of NO produced by auroral energy.
Note that the auroral energy routinely reaches middle latitudes and occasionally reaches the equator. This excursion to lower latitudes must be caused by winds. NO transported to lower latitudes will lead to enhanced cooling as well as modification of the temperature structure and D/E region composition there.
Geo
grap
hic
Latit
ude
Scott M. Bailey, LWS Workshop March 24, 2004
Northern WinterSouthern Summer
Solstice
Northern WinterSouthern Summer
Solstice
Smoothing by 30 days reveals a repeatable pattern of winter transport of NO to middle latitudes.
Note that in summer times, there is negligible NO produced by auroral energy.
Geo
grap
hic
Latit
ude
Scott M. Bailey, LWS Workshop March 24, 2004
Northern WinterSouthern Summer
Solstice
Northern WinterSouthern Summer
Solstice
The photochemical model can be iterated with varying auroral inputs to obtain the auroral energy deposition required to reproduce the NO observations.
The resulting energy fluxes show strong seasonal dependence with minima at the summer solstice.
North
Day of Year
Scott M. Bailey, LWS Workshop March 24, 2004
North
South
Day of Year
Day of Year
Scott M. Bailey, LWS Workshop March 24, 2004
Northern WinterSouthern Summer
Solstice
Northern WinterSouthern Summer
Solstice
The ratio of hemispheric energy inputs shows that winter energy deposition is significantly larger than summer energy deposition.
The ratios may also be increasing with solar activity.
Day of Year
Scott M. Bailey, LWS Workshop March 24, 2004
Conclusions:
The production of NO by solar soft X-ray irradiance is well understood.
NO produced by auroral energy is transported by winds to middle latitudes and sometimes to the equator.
Auroral energy deposition varies strongly with season and is at a minimum at summer latitudes. This is consistent with previous studies which have shown that discrete auroral events are suppressed in the summer.
Scott M. Bailey, LWS Workshop March 24, 2004
Scott M. Bailey, LWS Workshop March 24, 2004