NRLMSIS 2.1: An Empirical Model of Nitric Oxide Incorporated Into MSIS

Emmert, J. T.; Jones, McArthur; Siskind, D. E.; Drob, Douglas P.; Bernath, Peter F.; Stevens, M. H.; Bailey, S. M.; Bender, Stefan; Funke, B.; Hervig, Mark E.; Pérot, Kristell

doi:10.1029/2022ja030896

Cited by 27 publications

(17 citation statements)

References 68 publications

(128 reference statements)

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“…Later development led to the NRLMSISE-00 which improved the total mass density by incorporating more orbital drag and accelerometer data (Picone et al, 2002). Recently, the model was further updated to NRLMSIS2.0 (Emmert et al, 2021) and NRLMSIS2.1 (Emmert et al, 2022). In this 10.1029/2022SW003349 4 of 12 version, extensive new data were incorporated to estimate the profiles of neutral temperature, 8 neutral species densities, and total neutral mass density based on, time, location, solar activity, and geomagnetic activity.…”

Section: Nrlmsis20 Modelmentioning

confidence: 99%

Thermospheric Temperature and Density Variability During 3–4 February 2022 Minor Geomagnetic Storm

et al. 2023

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The Thermosphere-Ionosphere (TI) system of the Earth is externally forced by waves from the lower atmosphere and energy and momentum inputs from the sun through solar irradiance and solar wind energetic particles. The solar irradiance controls the thermospheric background neutral density and temperature through heating by the extreme ultraviolet radiation, one form of solar forcing. Another form of solar forcing comes from solar energetic charged particles from coronal mass ejection, high-speed streams, and corotating interaction regions. These charged particles behave like a plasma and are termed as the solar wind. The solar wind magnetic field, depending on its directionality, reconnects with Earth's magnetic field, transporting the solar wind energetic charged particles into the Earth's magnetosphere. Due to magnetosphere and ionosphere coupling through precipitation and electric fields, currents and resulting joule heating are produced, which perturbs the TI system. These perturbations then spread globally transporting energy and momentum. The transport happens through a high to lower latitude circulation induced by the heating and through Traveling Atmospheric Disturbance, that transports energy into the mid-to low-latitudes (Burns et al., 1995). Depending on the storm strength it can take from ∼3 hr

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Section: Nrlmsis20 Modelmentioning

confidence: 99%

Thermospheric Temperature and Density Variability During 3–4 February 2022 Minor Geomagnetic Storm

et al. 2023

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“…Suppose we want to confirm whether TAD #2 identified in the density perturbation (see TAD #2 Figure 1e) is a GW event or not. The background parameters needed by the function F , such as N B (buoyancy frequency), c s (sound speed),

\mathcal{H}

(density scale height), ν (kinematic viscosity,

\nu =\mu /\overline{\rho }

, where μ is the molecular viscosity), γ (ratio of specific heats), etc., are determined directly or indirectly from the Naval Research Laboratory MSIS (NRLMSIS) 2.1 model (Emmert et al., 2022). This model inputs the time and location for the TAD event.…”

Section: Techniques For Diagnosing Gws From In‐situ Observationsmentioning

confidence: 99%

Quiet Time Thermospheric Gravity Waves Observed by GOCE and CHAMP

Xu,

Vadas,

Yue

2024

JGR Space Physics

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The Gravity Field and Steady‐State Ocean Circulation Explorer (GOCE) and CHAllenging Minisatellite Payload (CHAMP) satellites measure in‐situ thermospheric density and cross‐track wind. When propagating obliquely to the satellite track in a horizontal plane (i.e., not purely along‐track or cross‐track), gravity waves (GWs) can be observed both in the density and cross‐track wind perturbations. We employ the Wavelet Analysis, red noise model, dissipative dispersion and polarization relations for thermospheric GWs, and specific criteria to determine whether a quiet‐time (Kp < 3) thermospheric traveling atmospheric disturbances (TADs) event is a GW or not. The first global morphology of thermospheric GWs instead of TADs is reported. The fast intrinsic horizontal phase speed (cIH > 600 m/s) of most GWs suggests that they are not generated in the lower/middle atmosphere (where cIH < 300 m/s). A second population of GWs with slower speeds (cIH = 50–250 m/s) in GOCE are likely from the lower/middle atmosphere, but they occur much less frequently in CHAMP. GW hotspots occur during the high‐latitude and the winter midlatitude regions. GW amplitudes exhibit semi‐annual and annual variations. These findings suggest that most GOCE and CHAMP GWs are higher‐order GWs from primary GW sources in the lower/middle atmosphere. Finally, the average propagation direction of the CHAMP GWs exhibits a clear diurnal cycle, with clockwise (counterclockwise) occurring in the northern (southern) hemisphere and equatorward propagation occurring at ∼13 LST. This suggests that the predominant GW propagation direction is opposite to the background wind direction.

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“…Note that there exists a newer version of MSIS-series of models, NRLMSIS 2.1, which consists of the addition of nitric oxide (NO), but that retains all other model parameters from NRLMSIS 2.0. (Emmert et al, 2022). The NRLMSIS 2.0 couples thermospheric densities to entire column via an effective mass profile.…”

Section: Mass Spectrometer and Incoherent Scatter Radar Model (Msis)mentioning

confidence: 99%

The Lower Thermospheric Winter‐To‐Summer Meridional Circulation: 2. Impact on Atomic Oxygen

Wang,

Yue,

Wang

et al. 2023

JGR Space Physics

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As a companion study of the Part 1 (J. C. Wang et al., 2022, https://doi.org/10.1029/2022JA030948), the impact of the lower‐thermospheric circulation on atomic oxygen (O) in the mesosphere and lower thermosphere (MLT) region is investigated in this Part 2 using Specified Dynamics Configuration Runs of the Whole Atmosphere Community Climate Model eXtended (SD‐WACCMX) output. The asymmetry of the O profile in the summer and winter MLT region is mainly driven by local vertical advection, which is associated with the lower‐thermospheric winter‐to‐summer circulation and middle‐to‐upper thermospheric summer‐to‐winter circulation. It is found that meridional transport and eddy diffusion only weakly modulate the O budget within this altitude range. The globally and annually averaged transport effect due to the vertical advection is quantitatively estimated. It is shown that the vertical advection is the dominant mechanism in redistributing O at altitudes between 84 and 103 km, suggesting the vertical wind can efficiently transport O between its source and sink region within the vertical column. This study demonstrates that whole atmosphere coupling on seasonal time scales is a complex interaction involving multiple underlying mechanisms within the space‐atmosphere interaction region.

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NRLMSIS 2.1: An Empirical Model of Nitric Oxide Incorporated Into MSIS

Cited by 27 publications

References 68 publications

Thermospheric Temperature and Density Variability During 3–4 February 2022 Minor Geomagnetic Storm

Thermospheric Temperature and Density Variability During 3–4 February 2022 Minor Geomagnetic Storm

Quiet Time Thermospheric Gravity Waves Observed by GOCE and CHAMP

The Lower Thermospheric Winter‐To‐Summer Meridional Circulation: 2. Impact on Atomic Oxygen

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