Method for inverting ozone concentration profile through airglow radiation of oxygen atmospheric zone and near-infrared atmospheric zone

Abstract

The invention belongs to the technical field of space atmospheric optical remote sensing, and particularly relates to a method for inverting an ozone concentration profile through airglow radiation of an oxygen atmospheric zone and a near-infrared atmospheric zone. According to the method, airglow radiation signals of the O2 atmospheric zone and the near-infrared atmospheric zone are combined, the ozone profile within the near space of 30 km to 130 km is obtained through calculation according to the photochemical reaction principle and the atmospheric radiation transmission model, and compared with a traditional O3 concentration profile inversion method, the method has better accuracy and a larger vertical coverage range.

Description

Technical Field

[0001] The present invention belongs to the technical field of space atmospheric optical remote sensing, and specifically relates to a method for inverting ozone concentration profiles using airglow radiation in an oxygen atmosphere belt and a near-infrared atmosphere belt, and in particular to a method for inverting ozone concentration profiles in a nearby space region using airglow radiation in an oxygen atmosphere belt and a near-infrared atmosphere belt. Background Art

[0002] Ozone is one of the most important trace gases in the Earth's atmosphere. It has active chemical properties and participates in many photochemical reaction processes. Studying the temporal evolution and spatial distribution of ozone concentration in the global near-space is of great significance to the ecological environment and climate change. It can also improve the accuracy of weather forecasts and the safety of aerospace.

[0003] Satellite remote sensing can realize global-scale observations and has the characteristics of high temporal and spatial resolution and wide temporal and spatial continuity. The ozone concentration detection method using satellite remote sensing has gradually become an international research hotspot. At present, the main methods of satellite remote sensing detection of ozone profiles are occultation absorption detection, ultraviolet scattering absorption detection, and infrared thermal radiation detection. Among them, the occultation detection method is to invert the ozone concentration by observing the changes in the atmospheric radiation absorption spectrum of the sun or moon when it rises or sets, so its scanning horizontal resolution and spatial coverage are limited; the ozone concentration inversion method based on ultraviolet scattering absorption spectrum is easily affected by clouds and aerosols, resulting in inaccurate detection results; and the long-wave infrared thermal radiation detection of ozone mostly relies on high-resolution, high-sensitivity optical elements and detectors, which have high requirements for refrigeration conditions, and external environmental factors such as temperature and humidity profile errors will also affect the radiation and ozone weight function, thereby affecting the accuracy of the ozone profile inversion results.

[0004] By detecting oxygen molecules in O2(a 1 Δ g ) band airglow radiation can be indirectly inverted to obtain the vertical profile of ozone. This method has the advantages of high accuracy and strong stability. However, due to the self-absorption effect at low altitudes, the spectrum is polluted, which makes it difficult to use O2(a 1 Δ g ) band is difficult to detect the ozone concentration in the lower area of ​​the nearby space, while the O2(a 1 Δ g ) band has weak airglow radiation and a small signal-to-noise ratio, making it impossible to detect ozone concentration. Summary of the invention

[0005] In order to overcome the problems in the prior art, the present invention proposes a method for inverting ozone concentration profiles from airglow radiation in the oxygen atmospheric belt and the near-infrared atmospheric belt. The method of the present invention combines the airglow radiation signals of the O2 atmospheric belt and the near-infrared atmospheric belt, and uses the principle of photochemical reaction and the atmospheric radiation transmission model to calculate and obtain the ozone profile within 30km-130km in the near space. Compared with the traditional O3 concentration profile inversion method, it has better accuracy and larger vertical coverage.

[0006] The technical solution of the present invention to solve the above technical problems is as follows:

[0007] The present invention provides a method for inverting ozone concentration profiles from airglow radiation in an oxygen atmosphere zone and a near-infrared atmosphere zone, comprising the following steps:

[0008] Step 100: Obtain O2(a 1 Δ g ) band based on standard observation spectrum data of target layer altitude of 2km-90km D a , and O2(b 1 ∑ + g ) band based on standard observation spectrum data of 50km-150km target layer altitude D b ;

[0009] Step 200: The standard observation spectrum data D a And standard observation spectrum data D b Crack layer by layer to obtain O2(a 1 Δ g ) band between 2km and 90km above sea level, and the single-layer airglow radiation spectral intensity value of each layer, as well as O2(b 1 ∑ + g ) The single-layer airglow radiation spectral intensity value of each layer between the altitude of 50km-150km in the band; construct a single-layer observation spectral dataset based on the target layer altitude set H1, and a single-layer observation spectral dataset based on the target layer altitude set H2;

[0010] Step 300: Establish a geometric model for observing the edge along the line of sight based on the spherically symmetric structure, and calculate O2(a 1 Δ g ) band self-absorption effect correction term, O2(b 1 ∑ + g ) band self-absorption effect correction term; and calculate the O2(a 1 Δ g ) band self-absorption effect correction of single-layer airglow radiation spectrum intensity value and O2(b 1 ∑ +g ) band self-absorption effect to correct the single-layer airglow radiation spectrum intensity value;

[0011] Step 400: Based on O2(a 1 Δ g ) band self-absorption effect to correct the single-layer airglow radiation spectrum intensity value, and based on the kinetic photochemical model, construct the O2(a 1 Δ g ) band ozone concentration calculation model, based on the target layer altitude set H1 O2 (a 1 Δ g ) band with ozone concentration collection of observed spectral data considering self-absorption effect;

[0012] Step 500: Construct O2(a) based on kinetic photochemical model 1 Δ g ) band and O2(b 1 ∑ + g ) bands jointly calculate the ozone concentration relationship model, and obtain the O2(b 1 ∑ + g ) band with ozone concentration collection of observed spectral data considering self-absorption effect;

[0013] Step 600: Based on O2(a 1 Δ g ) band considering the self-absorption effect of the observed spectral data of ozone concentration and O2(b 1 ∑ + g ) band, and jointly invert the ozone concentration profile of the observed spectral data within the target layer altitude of 30km-130km.

[0014] Furthermore, in step 100,

[0015] For O2(a 1 Δ g ) band out-of-band radiation i a The linear fitting calculation results show that the background interference noise N of the airglow-free radiation signal at an altitude of 2km-90km is obtained. a , where out-of-band radiation i a is the observed spectral data I a 2-90 Spectral data in the wavelength range of 1210nm-1240nm, 1300nm-1340nm, O2(a 1 Δ g ) band observation spectrum data I a2-90 Eliminate background interference noise of non-airglow radiation signal N a , obtain standard spectrum data D a ;

[0016] For O2(b 1 ∑ + g ) band out-of-band radiation i b Linear fitting calculation of background interference noise N of airglow-free radiation signal at altitudes of 50km-150km b , where out-of-band radiation i b O2(b 1 ∑ + g ) band observation spectrum data I b 50-150 Spectral data in the wavelength range of 750nm-759nm and 767nm-781nm; for the observed spectral data I b 50-150 The spectral signal at an altitude of 130km-150km is averaged to obtain the scattered light interference noise d b ; O2(b 1 ∑ + g ) band observed spectral data I b 50-150 Eliminate the background interference noise of the airglow radiation signal N b , and scattered light interference noise d b Then, the standard spectrum data D is obtained. b .

[0017] Furthermore, in step 200, based on the single-layer observed spectral data set of the target layer altitude set H1

[0018]

[0019] Single-layer observation spectral dataset based on target layer altitude set H2

[0020]

[0021] in, is the single-layer airglow radiation spectral intensity value at any h1 altitude in the target layer altitude set H1, is the single-layer airglow radiation spectrum intensity value at any h2 height in the target layer altitude set H2; a O2(a 1 Δ g ) band single-layer airglow radiation spectrum intensity value corresponding to the observation wavelength; λ bO2(b 1 ∑ + g ) band single-layer airglow radiation spectrum intensity value corresponding to the observation wavelength; 30km≤H1≤90km, 70km≤H2≤130km, h1∈H1, h2∈H2, 1210nm≤λ a ≤1340nm, 750nm≤λ b ≤790nm.

[0022] Furthermore, the step 300 includes:

[0023] Step 310: Establish a geometric model for observing the edge of the line of sight based on the spherically symmetric structure, and based on the absorption coefficient σ h1 Calculate O2(a 1 Δ g ) band self-absorption effect correction term A h1 And based on the absorption coefficient σ h2 Calculate O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 ;

[0024] Step 320: The calculated O2(a 1 Δ g ) band self-absorption effect correction term A h1 The reciprocal of the single-layer airglow radiation spectrum intensity value Multiply them and calculate O2(a 1 Δ g ) band target layer altitude h1 self-absorption effect correction single layer airglow radiation spectrum intensity value The calculated O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 The reciprocal of the single-layer airglow radiation spectrum intensity value Multiply them and calculate O2(b 1 ∑ + g ) band target layer altitude h2 self-absorption effect correction single layer airglow radiation spectrum intensity value

[0025] Furthermore, the step 300 includes:

[0026] Step 3101: Establish a geometric model for observation along the line of sight edge based on the spherically symmetric structure, record the atmospheric layer number l from the outside to the inside and from the near satellite end to the far satellite end, and use the absorption coefficient σ h1 Calculate O2(a 1 Δ g) band self-absorption effect correction term A h1 :

[0027]

[0028] Where i is the number of the limb sight line, j is the number of the spherically symmetric structure layer, j′ is the number of the spherically symmetric structure layer j one layer forward from the satellite end, is the single-layer airglow radiation spectrum intensity value of the corresponding layer number at the target layer altitude h1 observed along the limb line of sight for the spherically symmetric structure, σ h1 (j′) is According to the spherically symmetric structure, the absorption coefficient of one layer moving toward the satellite end;

[0029] Step 3102: Using the absorption coefficient σ h2 Calculate O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 :

[0030]

[0031] in, is the single-layer airglow radiation spectrum intensity value of the corresponding layer number at the target layer altitude h2 observed along the limb line of sight for the spherically symmetric structure, σ h2 (j′) is The absorption coefficient of one layer moving toward the satellite end according to the spherically symmetric structure.

[0032] Furthermore, the step 400 includes:

[0033] Step 410: O2(a 1 Δ g ) band self-absorption effect correction of single-layer airglow radiation spectrum intensity value According to the observation wavelength λ a Perform integral operation to obtain O2(a 1 Δ g ) band target layer airglow concentration at altitude h1

[0034]

[0035] Among them, E a O2(a 1 Δ g ) band Einstein transition probability constant, λ is the wavelength integral variable;

[0036] Step 420: Based on the kinetic photochemical model, construct O2(a 1 Δ g) band to calculate the ozone concentration relationship equation, and calculate the ozone concentration at the target layer altitude h1

[0037]

[0038] Where η is the energy absorbed by O2 to produce O( 3 P) and O( 1 D) quantum yield constant, J H is the constant of the photolysis coefficient of ozone in the Hartley band, A1 is O( 1 D) finally releases energy in the form of photons and transfers back to the ground electron state. The inverse constant of the photochemical lifetime is k1, which is O( 1 D) eventually releases energy in the form of photons and transfers back to the ground state rate constant, g IRA is the resonance absorption coefficient of ground state molecular oxygen in the IRA band, is responsible for the electronic excited state O( 1 D) collision quenching molecular concentration constant coefficient, Responsible for the photoexcitation to produce O2(a 1 Δ g ) oxygen molecule concentration constant coefficient within the height range of h1;

[0039] Step 430: Correct the single-layer observed spectral dataset V using the inverse of the self-absorption effect correction term a 30-90 , calculate O2(a 1 Δ g ) band self-absorption effect correction single layer observation spectrum dataset U a 30-90 , and the ozone concentration at all altitudes in the target layer altitude set H1 Construct O2(a 1 Δ g ) band target layer altitude ozone concentration set C a 30-90 .

[0040] Furthermore, the step 500 includes:

[0041] Step 510: O2(b 1 ∑ + g ) band self-absorption effect correction of single-layer airglow radiation spectrum intensity value According to the observation wavelength λ b Perform integration operation to obtain O2(b 1 ∑ + g ) band target layer airglow concentration at altitude h2

[0042]

[0043] Among them, E b O2(b 1 ∑ + g ) band Einstein transition probability constant;

[0044] Step 520: Construct O2(a) based on the kinetic photochemical model 1 Δ g ) band and O2(b 1 ∑ + g ) bands to jointly calculate the ozone concentration relationship equation, adding O2(b 1 ∑ + g ) The concentration of the target layer at the altitude h2 of the band The ozone concentration inversion accuracy is improved by calculating the ozone concentration at the target layer altitude h2 in the range of 70km-90km.

[0045]

[0046] Among them, k Σ O2(b 1 Σ g + ) eventually releases energy in the form of photons and transfers back to the ground state rate constant, is responsible for the electronic excited state O2(b 1 Σ g + ) is the collision quenching molecular concentration constant coefficient, O2(a 1 Δ g ) The airglow concentration in the target layer of the band h1 within the range of 70km-90km, Responsible for the photoexcitation to produce O2(a 1 Δ g ) oxygen molecule concentration constant coefficient within the height range of h2;

[0047] Step 530: Construct O2(b 1 ∑ + g ) band to calculate the ozone concentration relationship equation, and calculate the ozone concentration in the target layer altitude h2 within the range of 90km-130km

[0048]

[0049] Among them, A2 is O2 (a 1 Δ g ) band eventually releases energy in the form of photons and transfers back to the ground electron state, the inverse constant of the photochemical lifetime, g A is the resonance absorption coefficient of ground state molecular oxygen at 762nm in the A band, g B is the resonance absorption coefficient of ground state molecular oxygen at 688nm in the B band;

[0050] Step 540: Based on O2(a 1 Δ g ) band airglow concentration and O2(b 1 ∑ + g ) band airglow concentration Traverse all altitude values ​​in the target layer altitude H2 and calculate the ozone concentration at all altitudes in the target layer altitude set H2 Then, construct O2(a 1 Δ g ) band target layer altitude ozone concentration set

[0051]

[0052] Compared with the prior art, the present invention has the following technical effects:

[0053] (1) In the present invention, by adding O2 (a 1 Δ g )、O2(b 1 ∑ + g ) band self-absorption term is used to calculate the low-altitude ozone concentration profile, and the corrected single-layer airglow radiation spectrum intensity value is substituted into the kinetic photochemical model to obtain the low-altitude ozone concentration profile after self-absorption effect correction; the present invention takes into account O2 (a 1 Δ g )、O2(b 1 ∑ + g ) band self-absorption effect correction, optimize the airglow radiation spectral intensity of each target layer, eliminate the spectral pollution caused by the self-absorption effect, and calculate a more accurate low-altitude atmospheric ozone profile.

[0054] (2) In the present invention, O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) band airglow radiation intensity model, O2(b 1 ∑ +g ) band is used to calculate the high-altitude ozone concentration. The high-altitude ozone concentration is calculated using the kinetic O2 (b 1 ∑ + g ) band photochemical model instead of O2(a 1 Δ g ) band photochemical model to obtain a more accurate high-altitude ozone profile and calculate the complete near-space atmospheric ozone profile, which not only ensures the expansion of the ozone profile inversion range, but also further guarantees the accuracy of the calculated ozone profile.

[0055] (3) In the present invention, O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) band joint calculation model, according to the kinetic photochemical model, O2 (b 1 ∑ + g ) band to ozone concentration, a more accurate mid- and low-altitude ozone profile is obtained; the present invention takes O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) bands, optimize the kinetic photochemical ozone concentration model, reduce the ozone concentration inversion error, and calculate a more accurate mid- and high-altitude atmospheric ozone profile. BRIEF DESCRIPTION OF THE DRAWINGS

[0056] In order to more clearly illustrate the technical solutions and advantages in the embodiments of the present invention or the prior art, the drawings required for use in the embodiments or the prior art descriptions are briefly introduced below. Obviously, the drawings described below are only some embodiments of the present invention. For ordinary technicians in this field, other drawings can be obtained based on these drawings without paying creative work.

[0057] Figure 1 It is a schematic diagram of the process of the present invention;

[0058] Figure 2 is the radiation intensity image of the spectral data observed in the limb observation mode of SCIAMACHY, where Figure 2 (a) is O2(a 1 Δ g ) band 57km, 67km, 77km, 87km four different altitude observation spectral data radiation intensity image, Figure 2 (b) is O2(b 1 ∑ +g ) Radiation intensity images of spectrum data observed at four different altitudes: 77km, 87km, 107km, and 137km;

[0059] Figure 3 It is the radiation intensity image of the standard spectrum data of airglow observation after removing the background interference noise of the airglow radiation signal in the limb observation mode of SCIAMACHY, where: Figure 3 (a) is O2(a 1 Δ g ) band observation of standard spectral data of airglow radiation intensity image, Figure 3 (b) is O2(b 1 ∑ + g ) band observation of standard spectral data of airglow radiation intensity image;

[0060] Figure 4 It is O2(b 1 ∑ + g ) band after removing the scattered light interference noise, the radiation intensity image of the standard spectrum data of airglow observation with zero out-of-band radiation intensity;

[0061] Figure 5 This is the radiation intensity image of the airglow observation spectral intensity data after the SCIAMACHY limb observation mode completes the "onion peeling" algorithm, where Figure 5 (a) is O2(a 1 Δ g ) band airglow observation spectral intensity data radiation intensity image, Figure 5 (b) is O2(b 1 ∑ + g ) band airglow observation spectral intensity data radiation intensity image;

[0062] Figure 6 It is O2(a 1 Δ g ) band after self-absorption effect correction single-layer airglow radiation spectrum intensity image;

[0063] Figure 7 is a comparison of multi-day ozone concentration profiles with MIPAS satellite data products and traditional direct methods, where: Figure 7 (b), (d), (f), and (h) are relative deviations from the official MIPAS data; Figure 7 The dates corresponding to (a), (c), (e), and (g) are March 2, 2011, June 1, 2011, September 12, 2011, and November 22, 2011, respectively. DETAILED DESCRIPTION

[0064] In order to further explain the technical means and effects taken by the present invention to achieve the predetermined invention purpose, the specific implementation methods, structures, features and effects of the technical solutions proposed by the present invention are described in detail below in conjunction with the accompanying drawings and preferred embodiments. The specific features, structures or characteristics in one or more embodiments may be combined in any suitable form. Unless otherwise defined, all technical and scientific terms used in the present invention have the same meaning as those commonly understood by technicians in the technical field of the present invention.

[0065] Since the traditional kinetic photochemical model is used to detect ozone concentration, only O2 (a 1 Δ g ) band as a tracer of ozone concentration, resulting in poor accuracy of ozone concentration profiles at low, medium and high altitudes. 1 Δ g ) band in the Hartley band ozone ultraviolet photolysis photochemical model and O2(b 1 ∑ + g ) band light excitation induced photochemical model, the present invention is based on the effect of ozone concentration changes on O2 (a 1 Δ g ) band and O2(b 1 ∑ + g ) band concentration, optimize the near-space ozone profile inversion accuracy by spatial region, and propose for the first time the O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) band airglow radiation intensity is combined to calculate the near-space ozone profile, including the low-altitude O2(b 1 ∑ + g ) band self-absorption term, mid-high altitude region O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) bands to jointly calculate the ozone concentration profile, high-altitude area O2(b 1 ∑ + g ) band as a new tracer for inverting the ozone concentration profile, and finally obtain a more accurate near-space ozone profile based on the observed spectral data of the target layer altitude through inversion. Simulation verification shows that under the same conditions, the present invention is superior to the traditional O2(a 1 Δ g ) band inversion ozone concentration profile model relative deviation is significantly reduced, the spatial coverage is significantly increased, and it is basically close to the actual near-space ozone profile.

[0066] In one embodiment of the present invention, a method for inverting ozone concentration profiles from airglow radiation in an oxygen atmosphere zone and a near-infrared atmosphere zone is provided, comprising the following steps:

[0067] Step 100: Obtain O2(a 1 Δ g ) band based on standard observation spectrum data of target layer altitude of 2km-90km D a , and O2(b 1 ∑ + g ) band based on standard observation spectrum data of 50km-150km target layer altitude D b ;

[0068] Step 200: The standard observation spectrum data D a And standard observation spectrum data D b Crack layer by layer to obtain O2(a 1 Δ g ) band between 2km and 90km above sea level, and the single-layer airglow radiation spectral intensity value of each layer, as well as O2(b 1 ∑ + g ) The single-layer airglow radiation spectral intensity value of each layer between the altitude of 50km-150km in the band; construct a single-layer observation spectral dataset based on the target layer altitude set H1, and a single-layer observation spectral dataset based on the target layer altitude set H2;

[0069] Step 300: Establish a geometric model for observing the edge along the line of sight based on the spherically symmetric structure, and calculate O2(a 1 Δ g ) band self-absorption effect correction term A h1 、O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 ; and calculate O2(a 1 Δ g ) band self-absorption effect correction of single-layer airglow radiation spectrum intensity value and O2(b 1 ∑ + g ) band self-absorption effect to correct the single-layer airglow radiation spectrum intensity value;

[0070] Step 400: Based on O2(a 1 Δ g ) band self-absorption effect to correct the single-layer airglow radiation spectrum intensity value, and based on the kinetic photochemical model, construct the O2(a 1 Δg ) band ozone concentration calculation model, based on the target layer altitude set H1 O2 (a 1 Δ g ) band with ozone concentration collection of observed spectral data considering self-absorption effect;

[0071] Step 500: Based on the kinetic photochemical model, construct O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) bands jointly calculate the ozone concentration relationship model, and obtain the O2(b 1 ∑ + g ) band with ozone concentration collection of observed spectral data considering self-absorption effect;

[0072] Step 600: Based on O2(a 1 Δ g ) band considering the self-absorption effect of the observed spectral data of ozone concentration and O2(b 1 ∑ + g ) band, and jointly invert the ozone concentration profile of the observed spectral data within the target layer altitude of 30km-130km.

[0073] The following is a detailed explanation of each of the above steps:

[0074] Step 100: Obtain the O2(a) at an altitude of 2km-90km 1 Δ g ) band original observed spectral data I a 2-90 , and obtain the O2(b 1 ∑ + g ) band original observed spectral data I b 50-150 , the original observed spectral data I a 2-90 and I b 50-150 Preprocessing was performed to eliminate background fitting noise interference and obtain O2(a 1 Δ g ) band based on standard observation spectrum data of target layer altitude of 2km-90km D a , and O2(b 1 ∑ + g) band based on standard observation spectrum data of 50km-150km target layer altitude D b .

[0075] Specifically: Obtain SCIAMACHY observation data from the Envisat official website (ftp: / / scia-ftp-ds.eo.esa.int) and download satellite remote sensing observation data. Read the satellite remote sensing observation data in the 6th spectral channel (990nm-1750nm) and the 4th spectral channel (597nm-789nm) in the limb observation mode on April 7, 2011 in the SCIAMACHY instrument data package, and obtain the corresponding observation wavelength λ a , b The complete information of oxygen molecule airglow radiation spectrum is obtained, and the O2(a 1 Δ g ) band original observed spectral data I a 2-90 , and O2(b 1 ∑ + g ) band original observed spectral data I b 50-150 , and obtain O2(a 1 Δ g ) band observation spectral data such as Figure 2 As shown in (a) and O2 (b 1 ∑ + g ) band observation spectral data image such as Figure 2 Middle (b).

[0076] The background interference noise N without airglow radiation signal is obtained by linear fitting methods such as least squares method, spline method and maximum likelihood estimation method. a 、N b .

[0077] For O2(a 1 Δ g ) band out-of-band radiation i a The linear fitting calculation results show that the background interference noise N of the airglow-free radiation signal at an altitude of 2km-90km is obtained. a , where out-of-band radiation i a is the observed spectral data I a 2-90 The spectrum data of the wavelength range is 1210nm-1240nm, 1300nm-1340nm, then, O2(a 1 Δ g ) band observation spectrum data I a 2-90Eliminated background interference noise N of airglow-free radiation signal a , obtain standard spectrum data D a ,like Figure 3 Middle (a).

[0078] For O2(b 1 ∑ + g ) band out-of-band radiation i b Linear fitting calculation of background interference noise N of airglow-free radiation signal at altitudes of 50km-150km b , where out-of-band radiation i b O2(b 1 ∑ + g ) band observation spectrum data I b 50-150 Spectral data in the wavelength range of 750nm-759nm and 767nm-781nm; for the observed spectral data I b 50-150 The spectral signal at an altitude of 130km-150km is averaged to obtain the scattered light interference noise d b ; Then, O2(b 1 ∑ + g ) band observed spectral data I b 50 -150 Eliminate the background interference noise of the airglow radiation signal N b like Figure 3 (b), and scattered light interference noise d b Then, the standard spectrum data D is obtained. b like Figure 4 , so that its out-of-band radiation matches the out-of-band radiation of the limb spectrum to be corrected, to ensure that the out-of-band radiation intensity is zero after correction.

[0079] Step 200: Based on the “onion peeling” algorithm, O2(a 1 Δ g ) band based on standard observation spectrum data of target layer altitude of 2km-90km D a 、O2(b 1 ∑ + g ) band based on standard observation spectrum data of 50km-150km target layer altitude D b Crack layer by layer to obtain O2(a 1 Δ g ) band between 2km and 90km above sea level, and the single-layer airglow radiation spectral intensity value of each layer, as well as O2(b 1 ∑ +g ) band between 50km and 150km above sea level, the single-layer airglow radiation spectrum intensity value of each layer; due to O2 (a 1 Δ g The effective target layer altitude set of the band is H1, O2 (b 1 ∑ + g ) band is H2, so a single-layer observation spectral dataset based on the target layer altitude set H1 is constructed. And a single-layer observation spectral dataset based on the target layer altitude set H2 Generate spectral images such as Figure 5 As shown in (a) and (b) in 5;

[0080] Single-layer observation spectral dataset based on target layer altitude set H1

[0081]

[0082] Single-layer observation spectral dataset based on target layer altitude set H2

[0083]

[0084] in, is the single-layer airglow radiation spectral intensity value at any h1 altitude in the target layer altitude set H1, is the single-layer airglow radiation spectrum intensity value at any h2 height in the target layer altitude set H2; a O2(a 1 Δ g ) band single-layer airglow radiation spectrum intensity value corresponding to the observation wavelength; λ b O2(b 1 ∑ + g ) band single-layer airglow radiation spectrum intensity value corresponding to the observation wavelength; 30km≤H1≤90km, 70km≤H2≤130km, h1∈H1, h2∈H2, 1210nm≤λ a ≤1340nm, 750nm≤λ b ≤790nm.

[0085] It is worth mentioning that the "peeling onion" algorithm is an existing mature algorithm. In the satellite payload limb observation mode, the collected signals can be regarded as the numerical integration of the body radiance along the line of sight. These signals show complex geometric characteristics, including contributions from the target layer and the atmosphere at the height of the space above it. Through the "peeling onion" algorithm, the solution is solved layer by layer starting from the top line of sight. The solution of the previous layer is used as the input of the next layer, and the solution is gradually solved downward. Since there is no contribution from other heights above the top layer, the signal strength of the target layer at the top layer height can be directly obtained. Then, the contribution of the top layer height is eliminated from the second layer measurement value, and the signal strength of the second layer target segment can be obtained. According to this idea, the signal strength information of the target layer at each limb height can be obtained step by step.

[0086] Step 300: Establish a geometric model for observing the edge along the line of sight based on the spherically symmetric structure, and calculate O2(a 1 Δ g ) band self-absorption effect correction term A h1 、O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 ; and calculate O2(a 1 Δ g ) band target layer altitude h1 self-absorption effect correction single layer airglow radiation spectrum intensity value and O2(b 1 ∑ + g ) band target layer altitude h2 self-absorption effect correction single layer airglow radiation spectrum intensity value

[0087] Wherein, step 300 includes the following steps:

[0088] Step 310: Establish a geometric model for observing the edge of the line of sight based on the spherically symmetric structure, and based on the absorption coefficient σ h1 Calculate O2(a 1 Δ g ) band self-absorption effect correction term A h1 and O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 .

[0089] As an example, this step may include the following steps:

[0090] Step 3101: Establish a geometric model for observation along the line of sight edge based on the spherically symmetric structure, record the atmospheric layer number l from the outside to the inside and from the near satellite end to the far satellite end, and use the absorption coefficient σ h1 Calculate O2(a1 Δ g ) band self-absorption effect correction term A h1 :

[0091]

[0092] Where i is the number of the limb sight line, j is the number of the spherically symmetric structure layer, j′ is the number of the spherically symmetric structure layer j one layer forward from the satellite end, is the single-layer airglow radiation spectrum intensity value of the corresponding layer number at the target layer altitude h1 observed along the limb line of sight for the spherically symmetric structure, σ h1 (j′) is According to the spherically symmetric structure, the absorption coefficient of one layer moving toward the satellite end;

[0093] Step 3102: Using the absorption coefficient σ h2 Calculate O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 :

[0094]

[0095] in, is the single-layer airglow radiation spectrum intensity value of the corresponding layer number at the target layer altitude h2 observed along the limb line of sight for the spherically symmetric structure, σ h2 (j′) is The absorption coefficient of one layer moving toward the satellite end according to the spherically symmetric structure.

[0096] Step 320: The calculated O2(a 1 Δ g ) band self-absorption effect correction term A h1 The reciprocal of the single-layer airglow radiation spectrum intensity value Multiply them and calculate O2(a 1 Δ g ) band target layer altitude h1 self-absorption effect correction single layer airglow radiation spectrum intensity value The calculated O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 The reciprocal of the single-layer airglow radiation spectrum intensity value Multiply them and calculate O2(b 1 ∑ + g ) band target layer altitude h2 self-absorption effect correction single layer airglow radiation spectrum intensity value

[0097] Step 400: Based on the kinetic photochemical model, construct O2(a 1 Δ g ) band ozone concentration calculation model, based on the target layer altitude set H1 O2 (a 1 Δ g ) band with self-absorption effect.

[0098] It is worth noting that the kinetic photochemical model is an existing mature model, which discusses in detail the O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) band, focusing on the generation and annihilation mechanisms of O2(a 1 Δ g )、O2(b 1 ∑ + g ) The airglow is directly produced by the photolysis of the Hartley band of ozone molecules and the excited state of oxygen atoms O( 1 D) energy transfer process indirectly produces two aspects. In addition, ground state oxygen molecules can absorb solar radiation to produce O2 (a 1 Δ g ) band and O2(b 1 ∑ + g ) band. At night, O2(a 1 Δ g ) and O2(b 1 ∑ + g ) is mainly produced by three-body reaction. The kinetic photochemical model shows the interaction between ozone molecules and O2(a 1 Δ g )、O2(b 1 ∑ + g ) gas glow photochemical model, for the use of O2(a 1 Δ g )、O2(b 1 ∑ + g )It provides a solid theoretical basis for inverting ozone concentration profiles from airglow radiation spectra.

[0099] Wherein, step 400 includes the following steps:

[0100] Step 410: O2(a 1 Δ g ) band self-absorption effect correction of single-layer airglow radiation spectrum intensity value According to the observation wavelength λ a Perform integral operation to obtain O2(a 1 Δ g ) band target layer airglow concentration at altitude h1

[0101]

[0102] Among them, E a O2(a 1 Δ g ) band Einstein transition probability constant, λ is the wavelength integral variable;

[0103] Step 420: Based on the kinetic photochemical model, construct O2(a 1 Δ g ) band to calculate the ozone concentration relationship equation, and calculate the ozone concentration at the target layer altitude h1

[0104]

[0105] Where η is the energy absorbed by O2 to produce O( 3 P) and O( 1 D) quantum yield constant, J H is the photolysis coefficient constant of ozone in the Hartley band (λ<310nm), A1 is O( 1 D) finally releases energy in the form of photons and transfers back to the ground electron state. The inverse constant of the photochemical lifetime is k1, which is O( 1 D) eventually releases energy in the form of photons and transfers back to the ground state rate constant, g IRA is the resonance absorption coefficient of ground state molecular oxygen in the IRA band (1270nm), is responsible for the electronic excited state O( 1 D) collision quenching molecular concentration constant coefficient, Responsible for the photoexcitation to produce O2(a 1 Δ g ) constant coefficient of oxygen molecule concentration in the height range of h1.

[0106] Step 430: Correct the single-layer observed spectral dataset V using the inverse of the self-absorption effect correction term a 30-90 , calculate O2(a 1 Δ g ) band self-absorption effect correction single layer observation spectrum dataset U a 30-90 , and the ozone concentration at all altitudes in the target layer altitude set H1 Construct O2(a 1 Δg ) band target layer altitude ozone concentration set C a 30-90 .

[0107] Since O2(a 1 Δ g ) band self-absorption term characterizes the error degree accumulated by the onion peeling algorithm at the target layer altitude. All altitude values ​​within the target layer altitude H1 are traversed and O2(a) is calculated by the absorption coefficient. 1 Δ g ) band self-absorption effect correction term, according to the target layer altitude value, the single layer observation spectrum data set V is corrected by the inverse of the self-absorption effect correction term a 30-90 , calculate O2(a 1 Δ g ) band self-absorption effect correction single layer observation spectrum dataset Generate a self-absorption effect corrected spectral image such as Figure 6 As shown,

[0108]

[0109] Based on O2(a 1 Δ g ) band self-absorption effect correction single layer observation spectrum dataset Traverse all altitude values ​​in the target layer altitude H1 and calculate the ozone concentration at all altitudes in the target layer altitude set H1 Then, construct O2(a 1 Δ g ) band target layer altitude ozone concentration set

[0110]

[0111] Step 500: Based on the kinetic photochemical model, construct O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) bands jointly calculate the ozone concentration relationship model, and obtain the O2(b 1 ∑ + g ) band with self-absorption effect.

[0112] Based on the kinetic photochemical model, O2(a 1 Δ g ) band and O2(b 1 ∑+ g ) bands jointly calculate the ozone concentration relationship model, not only by 1 ∑ + g ) band to improve the accuracy of ozone profile inversion within the target layer altitude range of 70km-90km, and according to O2(b 1 ∑ + g ) band single-layer observation spectral dataset increases the height range of ozone profile inversion, and obtains the O2(b 1 ∑ + g ) band with self-absorption effect.

[0113] Wherein, step 500 includes the following steps:

[0114] Step 510: O2(b 1 ∑ + g ) band self-absorption effect correction of single-layer airglow radiation spectrum intensity value According to the observation wavelength λ b Perform integral operation to obtain O2(b 1 ∑ + g ) band target layer airglow concentration at altitude h2

[0115]

[0116] Among them, E b O2(b 1 ∑ + g ) band Einstein transition probability constant;

[0117] Step 520: Considering O2(b 1 ∑ + g ) band to the ozone concentration inversion can improve the accuracy of ozone concentration inversion. Based on the kinetic photochemical model, the O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) bands to jointly calculate the ozone concentration relationship equation, adding O2(b 1 ∑ + g ) The concentration of the target layer at the altitude h2 of the band The ozone concentration inversion accuracy is improved by calculating the ozone concentration at the target layer altitude h2 in the range of 70km-90km.

[0118]

[0119] Among them, k Σ O2(b 1 Σ g + ) eventually releases energy in the form of photons and transfers back to the ground state rate constant, is responsible for the electronic excited state O2(b 1 Σ g + ) is the collision quenching molecular concentration constant coefficient, O2(a 1 Δ g ) The airglow concentration in the target layer of the band h1 within the range of 70km-90km, Responsible for the photoexcitation to produce O2(a 1 Δ g ) oxygen molecule concentration constant coefficient within the height range of h2;

[0120] Step 530: Since the target layer is above 90 km above sea level, O2 (a 1 Δ g ) band airglow concentration decreases, the calculated ozone concentration error is large, and O2(b 1 ∑ + g ) band has high airglow concentration, and the calculation accuracy of ozone concentration is high. Based on the kinetic photochemical model, O2(b 1 ∑ + g ) band to calculate the ozone concentration relationship equation, and calculate the ozone concentration in the target layer altitude h2 within the range of 90km-130km

[0121]

[0122] Among them, A2 is O2 (a 1 Δ g ) band eventually releases energy in the form of photons and transfers back to the ground electron state, the inverse constant of the photochemical lifetime, g A is the resonance absorption coefficient of ground state molecular oxygen in the A band (762nm), g B is the resonance absorption coefficient of ground state molecular oxygen in the B band (688nm).

[0123] Step 540: Based on O2(a 1 Δ g) band airglow concentration and O2(b 1 ∑ + g ) band airglow concentration Traverse all altitude values ​​in the target layer altitude H2 and calculate the ozone concentration at all altitudes in the target layer altitude set H2 Then, construct O2(a 1 Δ g ) band target layer altitude ozone concentration set

[0124]

[0125] In the above steps 400 and 500, based on the kinetic photochemical model, the O2 (a 1 Δ g ) band, O2(b 1 ∑ + g ) band to calculate the ozone concentration relationship model, by adding O2(a 1 Δ g ) band, O2(b 1 ∑ + g ) band self-absorption correction item is used to correct the single-layer observed spectral data, reduce the error accumulation caused by the "onion peeling" algorithm layer by layer, and focus on eliminating the error caused by O2 (a 1 Δ g ) band self-absorption effect, and focus on eliminating the spectral pollution caused by O2 (b 1 ∑ + g ) band self-absorption effect, and obtain the ozone concentration set based on the observed spectral data in the target layer altitude sets H1 and H2.

[0126] Step 600: Based on O2(a 1 Δ g ) band considering the self-absorption effect of the observed spectral data of ozone concentration and O2(b 1 ∑ + g ) band, and jointly invert the ozone concentration profile of the observed spectral data within the target layer altitude of 30km-130km.

[0127] O2(a 1 Δ g ) band ozone concentration collection Ozone concentration in the middle target layer at an altitude of 30km-69km and O2(a 1 Δ g ) band, O2(b 1 ∑ + g ) band joint calculation of ozone concentration set All ozone concentrations Smooth connection is used to generate the ozone concentration profile of the observed spectral data within the target layer altitude of 30km-130km. Figure 7 Figures (a), (c), (e), and (g) show that the ozone concentration profiles calculated by the present invention are basically consistent with the ozone concentration profiles of the MIPAS official website data at an altitude of 30km-130km in the target layer, and Figure 7 Figures (b), (d), (f), and (h) show that the average relative deviation is small, around 5%, 7%, 8%, and 6%, respectively, and generally remains within 10%. However, the average relative deviation of the ozone concentration profile calculated by the traditional direct method is large and unstable, around 26%, 27%, 34%, and 31%, respectively, and generally fluctuates around 30%.

[0128] Simulation Results Analysis

[0129] The observation data of SCIAMACHY were retrieved, and the simulation was performed using MatlabR2023b software, which was then verified using the temperature data of the MIPAS satellite.

[0130] The SCIAMACHY satellite remote sensing observation data were read by the method of the present invention. The dates involved were March 2, 2011, June 1, 2011, September 12, 2011, and November 22, 2011. The operation results are as follows: Figure 7 As shown: the ozone profile obtained by the calculation method of the present invention is basically consistent with the MIPAS ozone data product, ensuring that the relative deviation is kept within 10%, and can ensure that the ozone profile covering the 30km-130km spatial area is obtained.

[0131] Compared with the traditional methods of directly measuring the ozone radiation absorption characteristics to calculate the ozone concentration profile, such as occultation absorption detection, ultraviolet scattering absorption detection, infrared thermal radiation detection, etc., the present invention measures the O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) band to indirectly calculate the ozone concentration profile. The simulation results of this indirect method are shown in Table 1, which shows that the method of the present invention has significantly lower relative deviation than the traditional direct measurement method, and has the characteristics of fast speed and high inversion accuracy.

[0132] Table 1 Comparison of average relative deviations between the present invention and the traditional direct method

[0133]

[0134] The present invention adopts O2 (a 1 Δ g ) band and O2(b 1 ∑ + g ) band two-band satellite observation data to calculate the ozone concentration profile, compared with the traditional single O2 (a 1 Δ g ) band spectral data to calculate the ozone concentration profile, the relative deviation is significantly reduced, the simulation results are included in Table 1, indicating that the invention has the feature of high inversion accuracy.

[0135] The method of indirectly measuring the atmospheric ozone concentration profile of the present invention not only improves the inversion accuracy of the ozone concentration profile, but also expands the inversion range of the ozone concentration profile. The simulation results are shown in Table 2, indicating that the present invention has a larger inversion spatial range than the traditional direct method of ozone concentration profile inversion, and has the characteristics of high inversion accuracy and large spatial coverage.

[0136] Table 2 Comparison of spatial coverage between the present invention and the traditional direct method

[0137]

[0138]

[0139] The comparison results in Table 2 also show that: when the spatial coverage range of satellite observation spectral data is certain, the ozone concentration profile inverted by the method of the present invention is better than the traditional direct method, and the obtained ozone concentration profile can effectively cover the nearby space area (30km-120km), and the ozone concentration profile in the 30km-130km space area can be stably inverted through satellite spectral data.

[0140] In summary, the near-space ozone profile calculation method based on the O2 atmospheric belt and near-infrared atmospheric belt airglow in the present invention successfully obtains the atmospheric ozone concentration profile in the 30km-130km space area. 1 Δ g ) band joint O2(b 1 ∑ + g ) band airglow radiation intensity model is used to calculate the complete near-space atmospheric ozone concentration profile, which not only broadens the ozone inversion range, but also ensures the accuracy of the calculated ozone profile. At the same time, the present invention overcomes the layer-by-layer accumulation of errors in the traditional "onion peeling" method, and based on the influence of ozone concentration changes on O2 (a1 Δ g ) band and O2(b 1 ∑ + g ) band concentration, the inversion method of near-space ozone profile is optimized by spatial region to improve the inversion accuracy.

[0141] The above embodiments are only used to illustrate the technical solutions of the present invention, rather than to limit the same. Although the present invention has been described in detail with reference to the aforementioned embodiments, those skilled in the art should understand that the technical solutions described in the aforementioned embodiments may still be modified, or some of the technical features may be replaced by equivalents. Such modifications or replacements do not deviate the essence of the corresponding technical solutions from the spirit and scope of the technical solutions of the embodiments of the present invention, and should be included in the protection scope of the present invention.

Claims

1. A method for inverting ozone concentration profiles from airglow radiation in oxygen and near-infrared atmospheric zones, characterized in that: The following steps are involved: Step 100: Obtain O2(a 1 Δ g ) band based on standard observation spectrum data of target layer altitude of 2km-90km D a , and O2(b 1 ∑ + g ) band based on standard observation spectrum data of 50km-150km target layer altitude D b ; Step 200: The standard observation spectrum data D a And standard observation spectrum data D b Crack layer by layer to obtain O2(a 1 Δ g ) band between 2km and 90km above sea level, and the single-layer airglow radiation spectral intensity value of each layer, as well as O2(b 1 ∑ + g ) The single-layer airglow radiation spectral intensity value of each layer between the altitude of 50km-150km in the band; and construct a single-layer observation spectral dataset based on the target layer altitude set H1, and a single-layer observation spectral dataset based on the target layer altitude set H2; Step 300: Establish a geometric model for observing the edge along the line of sight based on the spherically symmetric structure, and calculate O2(a 1 Δ g ) band self-absorption effect correction term, O2(b 1 ∑ + g ) band self-absorption effect correction term; and calculate the O2(a 1 Δ g ) band self-absorption effect correction of single-layer airglow radiation spectrum intensity value and O2(b 1 ∑ + g ) band self-absorption effect to correct the single-layer airglow radiation spectrum intensity value; Step 400: Based on O2(a 1 Δ g ) band self-absorption effect to correct the single-layer airglow radiation spectrum intensity value, and based on the kinetic photochemical model, construct the O2(a 1 Δ g ) band ozone concentration calculation model, based on the target layer altitude set H1 O2 (a 1 Δ g ) band with ozone concentration collection of observed spectral data considering self-absorption effect; Step 500: Based on the kinetic photochemical model, construct O2(a 1 Δ g ) band and O2(b 1 ∑ + g ) bands jointly calculate the ozone concentration relationship model, and obtain the O2(b 1 ∑ + g ) band with ozone concentration collection of observed spectral data considering self-absorption effect; Step 600: Based on O2(a 1 Δ g ) band considering the self-absorption effect of the observed spectral data of ozone concentration and O2(b 1 ∑ + g ) band, and jointly invert the ozone concentration profile of the observed spectral data within the target layer altitude of 30km-130km.

2. The method for inverting ozone concentration profiles from airglow radiation in oxygen atmosphere zone and near-infrared atmosphere zone according to claim 1, characterized in that: The step 100 includes: For O2(a 1 Δ g ) band out-of-band radiation i a The linear fitting calculation results show that the background interference noise N of the airglow-free radiation signal at an altitude of 2km-90km is obtained. a , where out-of-band radiation i a is the observed spectral data I a 2-90 Spectral data in the wavelength range of 1210nm-1240nm, 1300nm-1340nm, O2(a 1 Δ g ) band observation spectrum data I a 2-90 Eliminate background interference noise of non-airglow radiation signal N a , obtain standard spectrum data D a ; For O2(b 1 ∑ + g ) band out-of-band radiation i b Linear fitting calculation of background interference noise N of airglow-free radiation signal at altitudes of 50km-150km b , where out-of-band radiation i b O2(b 1 ∑ + g ) band observation spectrum data I b 50-150 Spectral data in the wavelength range of 750nm-759nm, 767nm-781nm; for the observed spectral data I b 50-150 The spectral signal at an altitude of 130km-150km is averaged to obtain the scattered light interference noise d b ; O2(b 1 ∑ + g ) band observed spectral data I b 50-150 Eliminate the background interference noise of the airglow radiation signal N b , and scattered light interference noise d b Then, the standard spectrum data D is obtained. b .

3. The method for inverting ozone concentration profiles from airglow radiation in oxygen atmosphere zone and near-infrared atmosphere zone according to claim 1, characterized in that: In step 200, Single-layer observation spectral dataset based on target layer altitude set H1 Single-layer observation spectral dataset based on target layer altitude set H2 in, is the single-layer airglow radiation spectral intensity value at any h1 altitude in the target layer altitude set H1, is the single-layer airglow radiation spectrum intensity value at any h2 height in the target layer altitude set H2; a O2(a 1 Δ g ) band single-layer airglow radiation spectrum intensity value corresponding to the observation wavelength; λ b O2(b 1 ∑ + g ) band single-layer airglow radiation spectrum intensity value corresponding to the observation wavelength; 30km≤H1≤90km, 70km≤H2≤130km, h1∈H1, h2∈H2, 1210nm≤λ a ≤1340nm, 750nm≤λ b ≤790nm.

4. The method for inverting ozone concentration profiles from airglow radiation in oxygen and near-infrared atmospheric zones according to claim 3, characterized in that: The step 300 includes: Step 310: Establish a geometric model for observing the edge of the line of sight based on the spherically symmetric structure, and based on the absorption coefficient σ h1 Calculate O2(a 1 Δ g ) band self-absorption effect correction term A h1 And based on the absorption coefficient σ h2 Calculate O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 ; Step 320: The calculated O2(a 1 Δ g ) band self-absorption effect correction term A h1 The reciprocal of the single-layer airglow radiation spectrum intensity value Multiply them and calculate O2(a 1 Δ g ) band target layer altitude h1 self-absorption effect correction single layer airglow radiation spectrum intensity value The calculated O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 The reciprocal of the single-layer airglow radiation spectrum intensity value Multiply them and calculate O2(b 1 ∑ + g ) band target layer altitude h2 self-absorption effect correction single layer airglow radiation spectrum intensity value 5. The method for inverting ozone concentration profiles from airglow radiation in oxygen and near-infrared atmospheric zones according to claim 4, characterized in that: The step 300 includes: Step 3101: Establish a geometric model for observation along the line of sight edge based on the spherically symmetric structure, record the atmospheric layer number l from the outside to the inside and from the near satellite end to the far satellite end, and use the absorption coefficient σ h1 Calculate O2(a 1 Δ g ) band self-absorption effect correction term A h1 : Where i is the number of the limb sight line, j is the number of the spherically symmetric structure layer, j′ is the number of the spherically symmetric structure layer number j one layer forward from the satellite end, is the single-layer airglow radiation spectrum intensity value of the corresponding layer number at the target layer altitude h1 observed along the limb line of sight for the spherically symmetric structure, σ h1 (j′) is According to the spherically symmetric structure, the absorption coefficient of one layer moving toward the satellite end; Step 3102: Using the absorption coefficient σ h2 Calculate O2(b 1 ∑ + g ) band self-absorption effect correction term A h2 : in, is the single-layer airglow radiation spectrum intensity value of the corresponding layer number at the target layer altitude h2 observed along the limb line of sight for the spherically symmetric structure, σ h2 (j′) is The absorption coefficient of one layer moving toward the satellite end according to the spherically symmetric structure.

6. The method for inverting ozone concentration profiles from airglow radiation in oxygen atmosphere zone and near-infrared atmosphere zone according to claim 5, characterized in that: The step 400 includes: Step 410: O2(a 1 Δ g ) band self-absorption effect correction of single-layer airglow radiation spectrum intensity value According to the observation wavelength λ a Perform integral operation to obtain O2(a 1 Δ g ) band target layer airglow concentration at altitude h1 Among them, E a O2(a 1 Δ g ) band Einstein transition probability constant, λ is the wavelength integral variable; Step 420: Based on the kinetic photochemical model, construct O2(a 1 Δ g ) band to calculate the ozone concentration relationship equation, and calculate the ozone concentration at the target layer altitude h1 Where η is the energy absorbed by O2 to produce O( 3 P) and O( 1 D) quantum yield constant, J H is the constant of the photolysis coefficient of ozone in the Hartley band, A1 is O( 1 D) finally releases energy in the form of photons and transfers back to the ground electron state. The inverse constant of the photochemical lifetime is k1, which is O( 1 D) eventually releases energy in the form of photons and transfers back to the ground state rate constant, g IRA is the resonance absorption coefficient of ground state molecular oxygen in the IRA band, is responsible for the electronic excited state O( 1 D) collision quenching molecular concentration constant coefficient, Responsible for the photoexcitation to produce O2(a 1 Δ g ) oxygen molecule concentration constant coefficient within the height range of h1; Step 430: Correct the single-layer observed spectral dataset V using the inverse of the self-absorption effect correction term a 30-90 , calculate O2(a 1 Δ g ) band self-absorption effect correction single layer observation spectrum dataset U a 30-90 , and the ozone concentration at all altitudes in the target layer altitude set H1 Construct O2(a 1 Δ g ) band target layer altitude ozone concentration set C a 30-90 .

7. The method for inverting ozone concentration profiles from airglow radiation in oxygen atmosphere zone and near-infrared atmosphere zone according to claim 6, characterized in that: The step 500 includes: Step 510: O2(b 1 ∑ + g ) band self-absorption effect correction of single-layer airglow radiation spectrum intensity value According to the observation wavelength λ b Perform integral operation to obtain O2(b 1 ∑ + g ) band target layer airglow concentration at altitude h2 Among them, E b O2(b 1 ∑ + g ) band Einstein transition probability constant; Step 520: Construct O2(a) based on the kinetic photochemical model 1 Δ g ) band and O2(b 1 ∑ + g ) bands to jointly calculate the ozone concentration relationship equation, adding O2(b 1 ∑ + g ) band target layer airglow concentration at altitude h2 Item, calculate the ozone concentration at the target layer altitude h2 in the range of 70km-90km Among them, k Σ O2(b 1 Σ g + ) eventually releases energy in the form of photons and transfers back to the ground state rate constant, is responsible for the electronic excited state O2(b 1 Σ g + ) is the collision quenching molecular concentration constant coefficient, O2(a 1 Δ g ) The airglow concentration in the target layer of the band h1 within the range of 70km-90km, Responsible for the photoexcitation to produce O2(a 1 Δ g ) oxygen molecule concentration constant coefficient within the height range of h2; Step 530: Construct O2(b 1 ∑ + g ) band to calculate the ozone concentration relationship equation, and calculate the ozone concentration in the target layer altitude h2 within the range of 90km-130km Among them, A2 is O2 (a 1 Δ g ) band eventually releases energy in the form of photons and transfers back to the ground electron state, the inverse constant of the photochemical lifetime, g A is the resonance absorption coefficient of ground state molecular oxygen at 762nm in the A band, g B is the resonance absorption coefficient of ground state molecular oxygen at 688nm in the B band; Step 540: Based on O2(a 1 Δ g ) band airglow concentration and O2(b 1 ∑ + g ) band airglow concentration Traverse all altitude values ​​in the target layer altitude H2 and calculate the ozone concentration at all altitudes in the target layer altitude set H2 Then, construct O2(a 1 Δ g ) band target layer altitude ozone concentration set

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