CN114879280B - Atmospheric inverse temperature characteristic estimation method integrating radio occultation observation and ERA5 - Google Patents
Atmospheric inverse temperature characteristic estimation method integrating radio occultation observation and ERA5 Download PDFInfo
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Abstract
The invention discloses an atmospheric inverse temperature characteristic estimation method integrating radio occultation observation and ERA5, belonging to the field of atmospheric boundary layer characteristic estimation and research application. The method comprises the steps of extracting an atmospheric temperature profile from a first height of an area to be tested to the ground surface by using GPS radio occultation observation data of a multi-low orbit satellite platform and ERA5 atmospheric analysis data; after space-time matching is carried out by using a nearest neighbor method, selecting a lowest height threshold H, and compensating an atmospheric temperature profile of the ERA5 lower than the lowest height threshold H into the GPS radio occultation observation to obtain a complete atmospheric temperature profile; for estimating the height, thickness and strength characteristics of the atmospheric reverse temperature. The method can well estimate the reverse temperature structural characteristics of the near-surface, can detect the possibly-occurring reverse temperature layer in the upper layer in the troposphere, and has important significance for accurately predicting future polar regions and global change trends.
Description
Technical Field
The invention relates to the field of atmospheric boundary layer characteristic estimation and research application, in particular to an atmospheric inverse temperature characteristic estimation method integrating radio occultation observation and ERA 5.
Background
The inverse temperature structure and the distribution characteristics of the atmospheric boundary layer directly influence the material and energy exchange between the polar sea-ice-gas. On the one hand, the temperature inversion structure of the polar atmospheric boundary layer contributes to decoupling between the ground and the free atmosphere, exacerbating polar and global climate change by limiting turbulent mixing and inhibiting energy exchange. On the other hand, the inverse temperature structure of the polar region atmospheric boundary layer is closely related to the cloud distribution, and the surface energy balance can be influenced by increasing the downward long wave radiation. Therefore, the method for accurately estimating the inverse temperature structural characteristics of the regional atmospheric boundary layer has important significance for reasonably making a regional atmospheric boundary layer parameterization scheme in a propulsion climate mode and accurately predicting future regional and global change trends.
Many scholars currently conduct research work on the reverse temperature characteristics of the regional atmospheric boundary layer. Radiosonde observation is used as a traditional atmosphere detection means for estimating the inverse temperature characteristic of an atmospheric boundary layer of a polar region since 90 th century, but the radiosonde observation has low spatial resolution and has large difference in vertical resolution of observations of different instrument types, so that the related results are difficult to comprehensively reflect the distribution and change characteristics of the atmospheric boundary layer of the whole polar region. Numerical models can also be used for simulation of atmospheric boundary layer structures, but with lower accuracy, the estimated reverse temperature intensities are generally larger. Satellite remote sensing observation based on a medium resolution imaging spectrometer (MODIS) is often limited to winter only when used for inverse temperature characteristic estimation, and is only applicable to cloud-free conditions. Atmospheric infrared detectors (air) can be used to estimate the polar atmospheric boundary layer characteristics in cloudless and partially cloudy conditions, but the vertical resolution of air products is low and it is difficult to capture the fine inverse temperature structural features of the polar atmospheric boundary layer. The GPS radio occultation observation is used for extremely-large atmosphere boundary layer inverse temperature structure, and has the advantages of high vertical resolution (100 m), high precision, no instrument correction, long-term stability and the like, but the lowest height cannot reach the ground surface, and the observation at the near-surface is easily affected by multipath errors, so that certain systematic errors exist in the estimated atmosphere boundary layer structural characteristics. Therefore, there is an urgent need to develop a new method for precisely estimating the inverse temperature characteristics of a new polar atmospheric boundary layer.
Disclosure of Invention
According to the technical problems, the invention provides the atmospheric inverse temperature characteristic estimation method which fuses the radio occultation observation and the ERA5 by utilizing the mode layer data of the latest generation of atmospheric analysis data ERA5 provided by the GPS radio occultation observation and the European mesoscale weather forecast center.
The technical scheme adopted by the invention is as follows: an atmospheric inverse temperature characteristic estimation method integrating radio occultation observation and ERA5 is characterized by comprising the following steps:
Step one: extracting an atmospheric temperature profile from a first height of a region to be tested to the ground surface by using GPS radio occultation observation data of a multi-low orbit satellite platform;
Step two: processing mode layer data of ERA5 atmospheric analysis data, and extracting an atmospheric temperature profile from the first height to the surface of the region to be tested;
step three: performing space-time matching on the extracted GPS radio occultation observation and the atmospheric temperature profile of the ERA5 atmospheric analysis data by using a nearest neighbor method;
Step four: selecting a lowest detection height threshold H, and compensating an atmospheric temperature profile of the ERA5 lower than the lowest detection height threshold H to the GPS radio occultation observation to obtain a complete atmospheric temperature profile with high vertical resolution;
step five: and performing quality control on the obtained atmospheric temperature profile, and estimating the height, thickness and strength characteristics of the atmospheric reverse temperature.
Further, in the first step, the atmospheric temperature profile of the area to be tested is extracted, and whether the atmospheric temperature profile falls into the area to be tested is judged by selecting the tangential point position of the GPS radio occultation event as the position observed by the radio occultation.
Further, the first height is 500hPa.
Further, in the second step, ERA5 atmospheric analysis data is extracted for every 6 hours.
Further, in the second step, processing mode layer data of ERA5 atmospheric analysis data, including extracting the surface potential height and the surface pressure, and calculating the potential height corresponding to each mode layer;
(2.1) calculating the pressure p of each mode layer k
Where k=1, 2, …,137,P s is the surface pressure for the coefficients of each mixed layer;
the pressure p k of each mode layer can be calculated by:
(2.2) calculating the virtual temperature:
The virtual temperature T v can be expressed as:
Tv＝t(1+((Rvap/Rdry)-1)q)
wherein R vap,Rdry is the gas constants of water vapor and dry air, t is the temperature, and q is the humidity;
(2.3) calculating the potential height on each mode layer:
wherein phi s is the surface potential height; when k=1, α k =ln2, when k > 1,
Further, the nearest neighbor method in the third step is to complete the matching of the GPS radio occultation observation with the atmospheric temperature profile of the ERA5 atmospheric analysis data in time and space by using the nearest point.
Further, the estimated atmospheric reverse temperature height, thickness and strength characteristics in the fifth step need to satisfy:
(1) Removing any layer of atmospheric temperature profile with the temperature value lower than-40 ℃;
(2) Removing the temperature inversion layer with the temperature inversion thickness smaller than 100m from the temperature inversion layer with the temperature inversion thickness higher than the lowest height threshold;
(3) Removing the temperature inversion layer with the temperature inversion thickness smaller than 25m from the temperature inversion layer below the lowest height threshold;
(4) When the height interval between the two temperature inversion layers is smaller than 100m, combining the two temperature inversion layers;
(5) The reverse temperature layer having a reverse temperature strength lower than 0.3 ℃ is ignored.
The invention has the beneficial effects that:
(1) Carrying out regional atmosphere inverse temperature characteristic estimation by utilizing GPS radio occultation observation on a multi-low orbit satellite platform;
(2) The method for fusing the microwave remote sensing and atmospheric analysis data can cover the whole polar region, and has the advantages of all weather, no need of instrument correction, long-term stability, high vertical resolution and high precision;
(3) The method can well estimate the reverse temperature structural characteristics of the near surface and can also detect the possibly-occurring reverse temperature layer in the upper layer in the troposphere.
Drawings
FIG. 1 is a flow chart of a method for estimating the inverse temperature characteristic of the atmosphere by fusing radio occultation observation and ERA 5.
FIG. 2 is a plot of the arctic sounding station of the present invention for verification of results.
FIG. 3 is a plot of time-space matched COSIC, ERA5, RS and the resulting atmospheric temperature profile obtained by the proposed method.
FIG. 4 is a graph of the atmospheric temperature profile of a space-time matched GRACE, ERA5, RS and the proposed method of this patent.
FIG. 5 is a plot of the atmospheric temperature profile of a spatio-temporal match KOMPSAT-5, ERA5, RS and the method proposed in this patent.
FIG. 6 is a plot of the atmospheric temperature profile obtained by spatio-temporal matching METOP-A, ERA, RS and the proposed method.
FIG. 7 is a plot of space-time matching METOP-B, ERA, RS and the resulting atmospheric temperature profile from the proposed method.
FIG. 8 is a graph of space-time matched SAC-C, ERA, RS and the resulting atmospheric temperature profile of the proposed method.
FIG. 9 is a graph of space-time matched TanDEM-X, ERA, RS and the resulting atmospheric temperature profile from the proposed method.
FIG. 10 is a plot of the atmospheric temperature profile of a spatio-temporal match TerraSAR-X, ERA, RS and the method proposed by this patent.
Detailed Description
For a better explanation and understanding of the technical solutions and advantages of the present invention, the technical solutions of the embodiments of the present invention will be clearly and completely described below with reference to the accompanying drawings, but the contents of the present invention are not limited to the following embodiments.
As shown in fig. 1, a flowchart of a method for estimating the inverse temperature characteristic of the atmosphere by combining radio occultation observation and ERA5 is provided. The following description selects a partial GPS radio occultation observation after 2007 in arctic regions as an example, with a specific spatial range of-180 ° W to 180 ° E,60 ° N to 90 ° N.
S101, extracting an atmospheric temperature profile from a first height of a region to be tested to the ground surface by using GPS radio occultation observation data of a multi-low orbit satellite platform;
The GPS radio satellite-masking technology is that a GPS receiver is arranged on a space motion carrier (such as a low-orbit satellite), according to the relation between the refraction of electromagnetic waves in the atmosphere and parameters such as temperature, pressure, humidity and the like of the atmosphere, the Doppler frequency shift observed by the GPS receiver is used for adding the position and speed information of the GPS receiver and the GPS satellite, the atmospheric refraction index is inverted, and finally the parameters such as the temperature, the pressure, the humidity and the like are derived. GPS radio occultation data used in this patent are all from the American COSIC data analysis and storage center (CDAAC; https:// cdaac-www.cosmic.ucar.edu /), and the specific data type is the temperature and humidity profile data in the secondary product (wetPrf). The low-orbit satellite platform on which the used GPS radio occultation data is positioned mainly comprises COSMIC(Constellation Observing System for Meteorology Ionosphere&Climate)-1,GRACE(Gravity Recovery and Climate Experiment),KOMPSAT-5(Korea Multi-Purpose Satellite-5),Meteorological Operational satellite program(MetOp)-A/B,PAZ,SAC-C(Scientific Application Satellite-C),TanDEM-X, terraSAR-X and the like.
COSMIC is a multidisciplinary satellite task developed jointly by taiwan and the united states of China, and is mainly dedicated to researches related to the earth science such as neutral layer, ionosphere and earth gravitational field; the COSMIC constellation contains 6 low-orbit satellites such that its occultation observations are the most abundant occultation data for all data sources in the occultation plan. Grace is an internationally cooperative Medesin SST (satellite to satellite tracking) geodetic task involving the institutions of the space research Center (CSR) of the OGmbH university of Texas, the Jet Propulsion Laboratory (JPL) of the U.S. space agency, the German space agency (DLR) and the German national Global science center (GFZ). KOMPSAT-5 is the first occultation task of the korean space program, equipped with a dual-frequency GPS receiver to generate accurate orbit determination data and GPS occultation data. MetOpPAZ developed by spanish science and innovation, by receiving GPS signals of two polarized antennas, comparing measured phase differences between phase delays under different weather conditions to capture thermodynamic and hydraulic profiles in strong precipitation events, providing favorable conditions for extreme precipitation difficulty prediction; at present, the task development of the method in the aspect of atmosphere detection is very limited, and the method is to be gradually compensated and perfected. SAC-C satellites were launched on day 11 and 21 of 2000, which is an international earth observation satellite mission commonly developed by multiple countries such as Argentina, danish, italy, brazil, france and the United states, and is mainly responsible for satellite development by Argentina; its main scientific objective is to monitor the condition and dynamics of land and marine biospheres and environments, develop and utilize new global positioning system based technologies to measure the atmospheric phenomena globally to study weather, seasonal, annual and long term climate change. The TanDEM-X and TerraSAR-X binary stars are transmitted by DLR at 6, 15 and 21 months 2007, 2010, respectively, and in addition to the generation of a global elevation model (DEM), a GPS receiver is also mounted thereon for the observation of the atmospheric profile.
The position of a GPS occultation event (i.e., the occultation site) is represented by the latitude and longitude of the closest point from the earth's center on the line of the GPS satellite and the low-orbit satellite when tangent to the earth's surface. In the process of extracting wetPrf data of GPS radio occultation, we need to judge whether each occultation falls in the research area (i.e. arctic region) according to the tangent point position observed by the occultation. If the condition is met, the position of the occultation event, the potential high, the pressure, the atmospheric temperature and other profiles can be recorded for subsequent data processing.
S102, processing mode layer data of ERA5 atmospheric analysis data, extracting an atmospheric temperature profile from the first height to the surface of the region to be tested, and calculating potential heights corresponding to the mode layers, wherein the surface potential heights and the surface pressure;
ERA5 is the fifth generation of analysis data product (https:// cds. Close. Co-nick. Eu/cdsapp # |/searchtype = dataset) of the mid-term numerical prediction center in europe, which reprocesses satellite climate datasets and uses RTTOV11 radiation transmission mode, resulting in higher time resolution of the data. In addition, ERA5 assimilates more observation data and satellite data, enabling more accurate estimation of atmospheric conditions. ERA5 mode layer data is 137 layers, and in the height from 500hPa to the surface, the ERA5 mode layer data has about 42 layers of data. In the near-surface 100hPa, there are about 18 layers of ERA5 mode layer data. Thus, ERA5 mode layer data can be used well to remedy the defect of GPS radio occultation observation at the near-surface. However, since ERA5 mode layer data does not provide a potential height and pressure corresponding to each mode layer directly, in order to obtain the potential height and pressure on each mode layer, it is also necessary to obtain the surface potential height and surface pressure and then perform the following calculation.
In formula (1), k=1, 2, …,137,For each mixed layer coefficient (as shown in table 1), p s is the surface pressure. The pressure p k of each mode layer can be calculated by:
The virtual temperature T v can be expressed as:
Tv＝t(1+((Rvap/Rdry)-1)q) (4)
In the formula (4), R vap,Rdry is the gas constants of water vapor and dry air, t is the temperature, and q is the humidity.
The potential height at each mode layer can be expressed as
In the formula (6), phi s is the surface potential; when k=1, αk=ln2, when k > 1,
Table 1 mixed layer coefficients of ERA5 mode layer data
S103, performing space-time matching on the extracted GPS radio occultation observation and the atmospheric temperature profile of the ERA5 atmospheric analysis data by using a nearest neighbor method;
After acquiring the atmospheric temperature profile of the arctic region GPS radio occultation observation from 500hPa to the lowest altitude and ERA5 mode layer data from 500hPa to the earth's surface on a 6-hour basis, a space-time match between the two is initiated. Since the time resolution of ERA5 data is 6 hours, the maximum time interval between GPS radio occultation observation and ERA5 data is 3 hours, which allows matching over the time domain to be accomplished based on nearest neighbor method. When using ERA5 data with a spatial resolution of 0.5 ° x 0.5 °, matching over the spatial domain can also be done using nearest neighbor method, provided there is no significant difference in temperature between two points over a spatial distance of 0.5 ° in arctic regions.
S104, selecting a lowest height threshold H, and compensating an atmospheric temperature profile of the ERA5 lower than the lowest height threshold H to the GPS radio occultation observation to obtain a complete atmospheric temperature profile with high vertical resolution;
After the matching of the GPS radio occultation observation and the atmospheric temperature profile of ERA5 in the time domain and the space domain is completed, setting a minimum height threshold H (h=500 m is selected in this embodiment) of the GPS radio occultation observation, and performing data fusion on the GPS radio occultation observation and the atmospheric temperature profile of ERA 5. It should be noted that if the GPS radio occultation observation is not effectively observed within the height range from the earth surface H, the atmospheric temperature profile will not participate in the estimation of the atmospheric inverse temperature characteristic, and need to be removed. And further intercepting the atmospheric temperature profile in the lowest observed height range from the earth surface to the GPS radio occultation aiming at the atmospheric temperature profile extracted by ERA5, and then fusing the atmospheric temperature profile of the part with the atmospheric temperature profile observed by the original GPS radio occultation according to the height sequence, namely obtaining the complete atmospheric temperature profile with high vertical resolution from 500hPa to the earth surface.
S105, step five: and performing quality control on the obtained atmospheric temperature profile, and estimating the height, thickness and strength characteristics of the atmospheric reverse temperature.
And estimating the characteristics of the atmospheric inverse temperature height, thickness, strength and the like of the occultation point position by utilizing a complete atmospheric temperature profile obtained by fusing GPS radio occultation observation and ERA5 mode layer data. The reverse temperature height refers to the lowest height of an atmospheric reverse temperature layer which increases with the rise of the height, the reverse temperature height refers to the difference between the top and the bottom of the reverse temperature layer, and the reverse temperature strength refers to the difference between the top and the bottom of the reverse temperature layer. In order to ensure the effectiveness and quality of the estimated atmospheric temperature profile, the following points are required to be paid attention to when the atmospheric temperature profile obtained by the patent is used for estimating the temperature profile:
(1) The temperature value of any height of the atmospheric temperature profile is not lower than-40 ℃, otherwise, the inverse temperature characteristic estimation is not participated;
(2) Neglecting a temperature reversal layer with the temperature reversal thickness smaller than 100m in the temperature reversal layer above the lowest observed height of the GPS radio occultation;
(3) Neglecting an inverse temperature layer with the inverse temperature thickness smaller than 25m in an inverse temperature layer below the lowest observed height of the GPS radio occultation;
(4) When the multi-layer reverse temperature occurs, if the height interval between different reverse temperature layers is less than 100m, the reverse temperature layers with the height interval less than 100m need to be combined;
(5) The reverse temperature layer having a reverse temperature strength lower than 0.3 ℃ is ignored.
In order to objectively evaluate the effectiveness of the method proposed by the patent, the patent further introduces a sounding (RS) observation station in the international meteorological organization framework of the arctic region to estimate the atmospheric inverse temperature characteristic. The sounding station data selected by the patent is derived from a second-generation high-quality global radiosonde dataset (IGRA 2; https:// www.ncei.noaa.gov/products/weather-balloon/integrated-global-radiosonde-array) of the national climate data center, and comprises datasets of atmospheric parameters such as dew point temperature, pressure, water vapor pressure and the like of a plurality of distributed sites (radiosondes and sounding balloons) worldwide 2700. Sounding devices typically observe at times 0 and 12 of universal coordinated time (UTC) daily, as well as at UTC 6 and 18h for some sites in addition to UTC 0 and 12 h. The pressure, temperature and potential height in each site data of IGRA2 are subject to strict quality control. Considering that the sounding stations are sparsely distributed, when the atmospheric inverse temperature characteristics estimated by the method are evaluated, only GPS radio occultation observation with the sounding stations with the space distance smaller than 50km and the observation time interval within 3 hours is selected for comparison. Further, when the atmospheric reverse temperature characteristics are estimated using IGRA2 data, the reverse temperature layer having a reverse temperature thickness of less than 10m is ignored.
Fig. 2 shows the distribution of sounding stations in the arctic region introduced for objective evaluation and verification of the accuracy of the atmospheric temperature profile estimation extracted by the method of use of the present patent. Fig. 3 is an atmospheric temperature profile observed by COSMIC radio occultation in the vicinity of nomann wils sounding station (WMO number: 71043) in canada, and the atmospheric temperature profile obtained by the time-space matching ERA5, RS and the method of the present patent. The COSMIC radio occultation observation time was 49 minutes (UTC time, the same applies hereinafter) of 2007, 2 months, 6 days, 10 hours, and the spatial distance from the 71043 sounding station was about 18km, with the observation time difference of 1.17 hours. The atmospheric temperature profiles estimated by COSMIC and ERA5, although offset from RS, have better consistency. Compared to COSMIC observations, the atmospheric temperature profile of ERA5 has difficulty capturing the reverse temperature structure at locations other than the low troposphere. The absence of the atmospheric temperature profile observed by COSMIC was more severe at the low troposphere than in ERA5 results. Thus, the COSIC observations and ERA5 have good complementarity. According to the convention of the inversion temperature characteristic, the RS detects 3 inversion temperature layers, the corresponding inversion temperature heights are 95 m, 1572 m and 2304m, the inversion temperature thicknesses are 677 m, 89 m and 424m, and the inversion temperature intensities are 7 ℃, 1.8 ℃ and 5.4 ℃ respectively. ERA5 captures only one reverse temperature layer located near the surface, and the reverse temperature height, thickness and strength are respectively: 8.6m, 1072m and 9.4 ℃. After the COSIC and ERA5 are fused by the method, 3 temperature reversal layers are detected, the temperature reversal heights of the temperature reversal layers are respectively 8.6, 1400 and 2000m, the temperature reversal thicknesses of the temperature reversal layers are respectively 891, 300 and 400m, the temperature reversal intensities of the temperature reversal layers are respectively 9.2, 2.5 and 4.1 ℃, and the temperature reversal characteristics of the temperature reversal layers are more consistent with those of RS observation and estimation.
FIG. 4 is an atmospheric temperature profile fused with the GRACE radio occultation observation, ERA5, RS and the method of the present patent for space-time matching near the Alaska Fisher sounding station (WMO number: 70261) in the United states. The GRACE radio occultation observation time is 46 minutes of 9 hours of 4 months of 2008, the space distance between the GRACE radio occultation observation time and 70261 sounding stations is about 40.3km, and the observation time difference between the GRACE radio occultation observation time and the GRACE radio occultation observation time is 2.23 hours. The RS detects 2 temperature reversal layers, the corresponding temperature reversal heights are 135 m and 1827m, the temperature reversal thicknesses are 140 m and 69m, and the temperature reversal intensities are 1.6 ℃ and 1.5 ℃. ERA5 captures only one reverse temperature layer located near the surface, and the reverse temperature height, thickness and strength are respectively: 9.1m, 116.5m and 3.7 ℃. After GRACE and ERA5 are fused by the method, 2 temperature reversal layers are detected, the temperature reversal heights of the two layers are respectively 9.1 and 1700m, the temperature reversal thicknesses of the two layers are respectively 116.6 and 300m, and the temperature reversal intensities of the two layers are respectively 3.7 and 1.2 ℃, so that the temperature reversal characteristics of the two layers are more consistent with those of RS observation and estimation.
FIG. 5 is a KOMPSAT-5 radio occultation observation, ERA5, RS of space-time matching near the Cambridge bay ballasted survey station (WMO number: 71925) of southeast of Victoria island, canada and the atmospheric temperature profile fused by the method of this patent. KOMPSAT-5 radio occultation observation time is 28 minutes of 14 days of 20161 month and 2 days, the space distance between the satellite and a 71925 sounding station is about 21.2km, and the observation time difference between the satellite and the satellite is 2.48 hours. The RS detects 2 temperature reversal layers, the corresponding temperature reversal heights are 26 and 2172m, the temperature reversal thicknesses are 1019 and 119m, and the temperature reversal intensities are 13 and 2.8 ℃ respectively. ERA5 captures only one reverse temperature layer located near the surface, and the reverse temperature height, thickness and strength are respectively: 8.5m, 1070.2m and 14.1 ℃. After KOMPSAT-5 and ERA5 are fused by the method, 2 temperature reversal layers are detected, the temperature reversal heights of the two layers are 8.5 and 2200m respectively, the temperature reversal thicknesses of the two layers are 1291.5 and 400m respectively, and the temperature reversal intensities of the two layers are 15.1 and 2.5 ℃ respectively.
FIG. 6 is an atmospheric temperature profile of a space-time matched METOP-A radio occultation observation, ERA5, RS, and the fusion of the methods of the present patent in the vicinity of an Inuvy sonde sounding station (WMO number: 71957) in Canada. The time for carrying out radio occultation observation of METOP-A is 18 minutes at 1 day of 2008, the space distance between the radio occultation observation and a 71957 sounding station is about 12.6km, and the time difference between the radio occultation observation and the sounding observation is 0.32 hour. The RS detects 3 temperature reversal layers, the corresponding temperature reversal heights are 218 m, 1492 m and 3200m, the temperature reversal thicknesses are 96 m, 365 m and 227m, and the temperature reversal intensities are 0.6 ℃, 1.6 ℃ and 2.0 ℃ respectively. ERA5 did not catch the reverse temperature layer. After METOP-A and ERA5 are fused by the method, other 2 temperature reversal layers are detected except that the temperature reversal layer with weak near-surface strength is not captured, the temperature reversal heights of the temperature reversal layers are 1400 m and 3200m respectively, the temperature reversal thicknesses of the temperature reversal layers are 700 m and 300m respectively, and the temperature reversal intensities of the temperature reversal layers are 3.3 ℃ and 2.3 ℃.
FIG. 7 is a map of the atmospheric temperature profile fused with the method of the present patent, ERA5, RS, and the satellite-occultation observation of the METOP-B radio for space-time matching near the Russian GMO IM.E.K.FEDOROVA sounding station (WMO number: 20292). The time for METOP-B radio occultation observation is 32 minutes at 2013, 12, 9 and 23 days, the space distance between the radio occultation observation and a 20292 sounding station is about 19.0km, and the time difference between the radio occultation observation and the satellite observation is 0.45 hours. The RS detects 4 temperature reversal layers, the corresponding temperature reversal heights are respectively 99, 514, 2193 and 3390m, the temperature reversal thicknesses are respectively 126, 288, 87 and 224m, and the temperature reversal intensities are respectively 4.2, 3.8, 2.6 and 0.6 ℃. ERA5 captures only one reverse temperature layer located near the surface, and the reverse temperature height, thickness and strength are respectively: 8.7m, 791.3m and 8.1 ℃. After METOP-B and ERA5 are fused by the method, 2 low-layer temperature inversion layers detected by RS are combined by the fused atmospheric temperature profile due to resolution, 3 temperature inversion layers are detected, the temperature inversion heights of the two layers are 8.7, 2100 and 3200m respectively, the temperature inversion thicknesses of the two layers are 991, 300 and 300m respectively, and the temperature inversion intensities of the two layers are 9.3, 1.3 and 1.1 ℃.
FIG. 8 is an atmospheric temperature profile fused with the method of this patent, ERA5, RS, and SAC-C radio occultation observations of space-time matching near the Canadian North island Alert probe station (WMO number: 71082). The SAC-C radio occultation observation time is 10 minutes at 10 months of 2010 and 10 days of 2 days, the space distance between the SAC-C radio occultation observation time and a 71082 sounding station is about 49.1km, and the observation time difference between the SAC-C radio occultation observation time and the air sounding station is 1.95 hours. The RS detects 2 temperature reversal layers, the corresponding temperature reversal heights are 258 and 2440m respectively, the temperature reversal thicknesses are 800 and 228m respectively, and the temperature reversal intensities are 1.6 and 4.6 ℃ respectively. ERA5 captures only one reverse temperature layer located near the surface, and the reverse temperature height, thickness and strength are respectively: 8.9m, 795.6m and 5.3 ℃. After SAC-C and ERA5 are fused by the method, 2 temperature reversal layers are detected, the temperature reversal heights of the layers are 400 and 2100m respectively, the temperature reversal thicknesses of the layers are 500 and 500m respectively, and the temperature reversal intensities of the layers are 2.6 and 6.4 ℃ respectively.
FIG. 9 is an atmospheric temperature profile fused with the ERA5, RS and the method of the present patent for space-time matched tanDEM-X (TDX) radio occultation observation, ERA5, RS near the Russian day Gan Sike sonde station (WMO: 24343). The time for TDX radio occultation observation was 23 minutes from 2016, 4, 9, and 23 days, the spatial distance from 24343 sounding stations was about 49.7km, and the difference in observation time was 0.6 hours. The RS detects 2 temperature reversal layers, the corresponding temperature reversal heights are 80 and 1204m respectively, the temperature reversal thicknesses are 400 and 260m respectively, and the temperature reversal intensities are 7.4 and 1.6 ℃ respectively. ERA5 captures only one reverse temperature layer, and the reverse temperature height, thickness and strength are respectively: 71.5m, 190m and 1.8 ℃. After the TDX and ERA5 are fused by the method, 2 temperature reversal layers are detected, the temperature reversal heights of the temperature reversal layers are 71.5 and 1300m respectively, the temperature reversal thicknesses of the temperature reversal layers are 528.5 and 400m respectively, and the temperature reversal intensities of the temperature reversal layers are 6.5 and 1.5 ℃ respectively.
FIG. 10 is a TerraSAR-X (TSX) radio occultation observation, ERA5, RS, and atmospheric temperature profile fused by the method of this patent for space-time matching near the Alert sounding station (WMO number: 71082) of North Polaroid Canada. The time for TSX radio occultation observation is 2011, 4, 11, 0 and 50 minutes, the space distance between the TSX radio occultation observation and 71082 sounding stations is about 34.9km, and the observation time difference between the TSX radio occultation observation and the satellite sounding stations is 0.83 hours. The RS detects 2 temperature reversal layers, the corresponding temperature reversal heights are 65 and 3018m respectively, the temperature reversal thicknesses are 225 and 477m respectively, and the temperature reversal intensities are 5.6 and 4.4 ℃ respectively. ERA5 captures only 1 reverse temperature layer in the middle troposphere, and the reverse temperature height, thickness and strength are respectively: 2284m, 1768.5m and 2.0 ℃. After the TSX and ERA5 are fused by the method, 2 temperature reversal layers are detected, the temperature reversal heights of the two layers are respectively 100 and 3000m, the temperature reversal thicknesses of the two layers are respectively 400 and 700m, and the temperature reversal intensities of the two layers are respectively 1.5 and 3.0 ℃.
Through the comparison, the method used by the method can effectively estimate the inverse temperature characteristic of the atmosphere, can well estimate the inverse temperature structural characteristic of the near surface, and can also detect an inverse temperature layer possibly appearing in the upper layer in the troposphere. Meanwhile, the method for fusing the microwave remote sensing and atmospheric analysis data can cover the whole polar region, and has the advantages of all weather, no need of instrument correction, long-term stability, high vertical resolution and high precision; has important significance for accurately predicting future polar regions and global change trend.
Claims (6)
1. An atmospheric inverse temperature characteristic estimation method integrating radio occultation observation and ERA5 is characterized by comprising the following steps:
Step one: extracting an atmospheric temperature profile from a first height of a region to be tested to the ground surface by using GPS radio occultation observation data of a multi-low orbit satellite platform;
Step two: processing mode layer data of ERA5 atmospheric analysis data, and extracting an atmospheric temperature profile from the first height to the surface of the region to be tested;
Extracting the surface potential height and the surface pressure, and calculating the potential height corresponding to each mode layer;
(2.1) calculating the pressure p of each mode layer k
Wherein: k=1, 2, …,137,P s is the surface pressure for the coefficients of each mixed layer;
the pressure p k of each mode layer can be calculated by:
(2.2) calculating the virtual temperature:
The virtual temperature T v can be expressed as:
Tv＝t(1+((Rvap/Rdry)-1)q)
wherein: r vap,Rdry is the gas constants of water vapor and dry air, t is the temperature, and q is the humidity;
(2.3) calculating the potential height on each mode layer:
Wherein: phi s is the surface potential height; when k=1, α k =ln2, when k > 1,
Step three: performing space-time matching on the extracted GPS radio occultation observation and the atmospheric temperature profile of the ERA5 atmospheric analysis data by using a nearest neighbor method;
Step four: selecting a lowest detection height threshold H, and compensating an atmospheric temperature profile of the ERA5 lower than the lowest detection height threshold H to the GPS radio occultation observation to obtain a complete atmospheric temperature profile with high vertical resolution;
step five: and performing quality control on the obtained atmospheric temperature profile, and estimating the height, thickness and strength characteristics of the atmospheric reverse temperature.
2. The method for estimating the inverse atmospheric temperature characteristic by combining the radio occultation observation and the ERA5 according to claim 1, wherein the first step is to extract the atmospheric temperature profile of the area to be tested, and to determine whether the area to be tested falls into the area to be tested by selecting the tangential point position of the GPS radio occultation event as the position of the radio occultation observation, and if the area to be tested falls into the area to be tested, to extract the position of the occultation event, and the high potential, pressure and atmospheric temperature profile.
3. The method for estimating the inverse atmospheric temperature characteristic by combining radio occultation observation and ERA5 according to claim 1, wherein: the first height is 500hPa.
4. The method for estimating the atmospheric inverse temperature characteristic of the ERA5 by combining the radio occultation observation and the ERA 1 according to claim 1, wherein the ERA5 atmospheric re-analysis data is extracted in the second step for every 6 hours.
5. The method according to claim 1, wherein the nearest neighbor method in the third step is to complete the matching of the GPS radio occultation observation with the atmospheric temperature profile of the ERA5 atmospheric analysis data in time and space by using the nearest point.
6. The method for estimating the inverse atmospheric temperature characteristic by combining radio occultation observation and ERA5 according to claim 1, wherein the estimated inverse atmospheric temperature height, thickness and intensity characteristics in the fifth step are as follows:
(1) Removing any layer of atmospheric temperature profile with the temperature value lower than-40 ℃;
(2) Removing the temperature inversion layer with the temperature inversion thickness smaller than 100m from the temperature inversion layer with the temperature inversion thickness higher than the lowest height threshold;
(3) Removing the temperature inversion layer with the temperature inversion thickness smaller than 25m from the temperature inversion layer below the lowest height threshold;
(4) When the height interval between the two temperature inversion layers is smaller than 100m, combining the two temperature inversion layers;
(5) The reverse temperature layer having a reverse temperature strength lower than 0.3 ℃ is ignored.
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