CN107688006B - Quantification method for spectral distribution difference of different climate areas - Google Patents
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Abstract
The invention discloses a method for quantifying spectral distribution differences in different climatic regions, which comprises the steps of firstly carrying out one-dimensional linear interpolation processing on spectral distribution data of an upper boundary of an atmosphere layer of ASTM E-490AM0 to obtain spectral irradiance of any wavelength of the upper boundary of the atmosphere layer, then calculating direct spectral distribution data of a certain moment in a certain place by combining air temperature, ground relative humidity, ozone optical quality, nitrogen dioxide optical quality, aerosol solubility and air concentration parameter meteorological data, then measuring the ratio of a direct spectrum and a scattered spectrum at the moment by combining an irradiator, and analyzing and processing the spectral distribution differences by using cloud parameters of the place to obtain a direct spectrum correction coefficient of any wavelength by using cloud as an index, thereby reducing the prediction uncertainty of spectral distribution and achieving the purpose of quantifying the spectral distribution differences in different regions with higher precision.
Description
Technical Field
The invention relates to a quantification method of spectral distribution difference in different climate areas, and belongs to the technical field of photovoltaic system design.
Background
In recent years, with the enhancement of environmental protection consciousness, the utilization of renewable energy sources such as wind energy, tidal energy, solar energy and the like has increased year by year, and the installation amount of solar photovoltaic power stations has increased dramatically year by year. In the design of photovoltaic power plants, the total annual irradiation of the installation site, the power plant power, etc. are often considered, while local climate factors are less considered. The change of the climate factor affects the power output of the photovoltaic power station and the stability of the power station. In all climatic factors, the cloud layer is in the troposphere of the atmosphere, and all weather phenomena such as wind, rain, thunder and hail are generated by the cloud, and the change of the weather phenomena is random. In the research of the spectrum, only direct absorption influence and scattering absorption influence of stable components in the atmospheric layer in one day, such as ozone, nitrogen dioxide, aerosol, water vapor and the like, are researched, and the spectrum difference of sunlight passing through a cloud layer is not researched. The specific influence of the cloud layer on the design of the photovoltaic power station cannot be accurately considered.
Disclosure of Invention
The technical problem to be solved by the invention is to overcome the defects of the prior art and provide a method for quantifying the spectral distribution difference in different climatic regions, so as to quantify the spectral distribution difference caused by cloud cover.
In order to solve the technical problems, the technical scheme adopted by the invention is as follows: a quantification method for spectral distribution differences in different climatic regions comprises the following steps:
1) performing one-dimensional linear interpolation processing on the atmospheric upper-bound spectral distribution of ASTM E490AM0 to obtain irradiation E (lambda) corresponding to any wavelength, wherein lambda is the wavelength;
2) calculating the direct ground radiation spectral distribution;
3) measuring direct irradiation and scattering irradiation through an irradiation meter to obtain the proportion of the direct irradiation to the total irradiation;
4) calculating a spectral difference correction coefficient function with the cloud cover as an evaluation index;
5) and calculating the spectral distribution difference caused by different cloud cover in different areas based on the spectral difference correction coefficient function in the step 4).
The aforementioned direct ground spectral distribution eb(λ) is:
eb(λ)＝E(λ)AR(λ,mR)Ao(λ,mo)An(λ,mn)Ag(λ,mg)Aa(λ,ma)Aw(λ,mw) (1)
wherein A isR(λ,mR) Is the Rayleigh scattering absorption coefficient, Ao(λ,mo) Is the ozone absorption coefficient, An(λ,mn) Is the absorption coefficient of nitrogen dioxide, Ag(λ,mg) As the absorption coefficient of the mixed gas, Aa(λ,ma) Is the absorption coefficient of the aerosol, Aw(λ,mw) Is the water vapor absorption coefficient, mR,mo,mn,ma,mg,mwOptical qualities of Rayleigh scattering, ozone, nitrogen dioxide, aerosol, mixed gas and water vapor respectively;
the aforementioned ratio α of direct irradiation to total irradiation is:
α＝Ib/(Ib+Id) (2)
wherein, IbIs direct irradiation measured by an irradiator, IdIs the scattered radiation measured by an irradiator;
in the step 4), the cloud amount represents the degree of coverage of the cloud layer to the sky in a certain area, and the value range of the cloud amount is 0 to 10, which means the area of the sky occupied by the cloud block.
In the foregoing step 4), the spectral difference correction coefficient function includes the following steps:
5-1) carrying out one-dimensional linear interpolation processing on the spectral distribution data measured by the spectrometer to obtain the spectral distribution e of any measured wavelengthmea(λ)；
5-2) spectral difference e at arbitrary wavelength λ at cloud number H ═ QeQ(λ) is:
eeQ(λ)＝eb(λ)-αemea(λ) (3)
wherein α is the proportion of direct irradiation to total irradiation, Q is the specific value of cloud cover, and its value is 0-10;
5-3) assuming that the spectral difference caused by the cloud cover is a binary function with respect to the cloud cover H and the wavelength λ, defining a spectral difference correction coefficient function F (H, λ) as:
5-4) introducing boundary conditions, when H is 0, the spectral error caused by cloud amount is: e.g. of the typeeHWhen the discrete data are input into a surface fitting tool box of MATLAB, the analytical formula of the spectral difference correction coefficient function F (H, lambda) is obtained by multiple linear regression processing and fifth-order polynomial fitting, wherein the analytical formula is as follows:
wherein p is00，p10，p01，p20，p11，p02，p30，p21，p12，p03，p40，p31，p22，p13，p04，p50，p41，p32，p23，p14，p05As coefficients, the values of each coefficient are:
p00＝0.0866，p10＝-0.03091，p01＝0.07608，p20＝-0.002587，p11＝-0.02701，p02＝-0.08756，p30＝0.01446，p21＝-0.004073，p12＝-0.00367，p03＝-0.05656，p40＝-0.006386，p31＝0.01217，p22＝-0.001495，p13＝-0.000276，p04＝0.04503，p50＝-7.686e-15，p41＝-0.004913，p32＝0.0008028，p23＝8.292e-05，p14＝0.004897，p05＝0.02493。
in the step 5), the spectral distribution difference S (Δ H) caused by different cloud cover in different areas is:
S(ΔH)＝F(H1-H2,λ) (6)
where Δ H is the cloud cover difference for different regions, H1，H2Representing clouds in different regions.
The invention has the following beneficial effects:
according to the method, the spectral distribution difference is calculated according to different cloud cover quantities, so that the influence of the cloud cover on the photovoltaic power station is more accurately predicted.
Drawings
FIG. 1 is a flow chart of the method of the present invention;
FIG. 2 is a theoretical calculation distribution diagram and an actual measurement ground spectrum distribution diagram of an atmosphere upper boundary and a ground direct light spectrum of ASTM E490AM 0;
FIG. 3 is a graph showing the difference in spectral distribution among different clouds H;
FIG. 4 is a plot of the fitted spectral difference correction coefficient function.
Detailed Description
The invention is further described with reference to the following figures and detailed description. The following examples are only for illustrating the technical solutions of the present invention more clearly, and the protection scope of the present invention is not limited thereby.
The method for quantifying the spectral distribution difference of different climate areas comprises the following main processes: firstly, measuring the spectral distribution and irradiance at a certain moment in a certain place through a spectrometer and an irradiator to obtain the ratio of spectral data to direct irradiation, then carrying out one-dimensional linear interpolation processing on the spectral distribution data of the upper boundary of the atmosphere of ASTM E490AM0, calculating the theoretical spectral distribution of the local ground according to the air temperature, the ground relative humidity, the ozone optical quality, the nitrogen dioxide optical quality, the aerosol solubility, the water vapor optical quality and the air concentration parameter in the local meteorological data, finally extracting the direct irradiation spectral distribution, and processing by combining cloud data to obtain different wavelength spectral correction coefficients, wherein the calculation process is shown in figure 1 and comprises the following steps:
1. theoretical ground spectral distribution calculation
The ground spectral distribution is the superposition of the ground direct spectral distribution and the scattering spectral distribution, and the cloud layer is positioned in the troposphere of the atmosphere and is lower in height from the ground, so that the influence of the cloud layer on the direct spectrum and the influence of the scattering spectrum are the same.
1) The spectral distribution of the sun means that the irradiation size corresponding to any wavelength finally shows the spectral distribution under different wavelengths, so that the corresponding spectral distribution can be obtained by only obtaining the irradiation size of the corresponding wavelength, and the irradiation E (lambda) corresponding to any wavelength can be obtained by performing one-dimensional linear interpolation processing on the atmospheric upper-bound spectral distribution of ASTM E490AM 0;
2) according to the air temperature T, the relative humidity W, the atmospheric pressure P, the air concentration Cq, the nitrogen dioxide concentration Cn and the solar altitude angle gamma in the meteorological data, the corresponding Rayleigh scattering absorption coefficient A can be calculatedR(λ,mR) Ozone absorption coefficient Ao(λ,mo) Nitrogen dioxide absorption coefficient An(λ,mn) Mixed gas absorption coefficient Ag(λ,mg) Aerosol absorption coefficient Aa(λ,ma) Water vapor absorption coefficient Aw(λ,mw) Or transmittance of different atmospheric components, which is the ratio of radiant energy to total radiant energy after incident light reaches the surface of the medium and transmits through the medium; m isR,mo,mn,ma,mg,mwRespectively the optical qualities of rayleigh scattering, ozone, nitrogen dioxide, aerosol, mixed gas and water vapor. The absorption coefficients can be calculated through SMARTS2 model software, the calculation method comprises the steps of calculating all mass values according to local meteorological data, calculating the absorption coefficients of the whole selectable wavelength according to the data of different components in dat files built in the model software and different wavelengths, and finally reflecting that the spectral distribution calculated theoretically is different.
Because sunlight from the upper atmosphere to the earth's surface needs to pass through the atmosphere, the atmospheric components have two main effects on the irradiance of sunlight: direct incidence and scattering. The direct irradiation effect is the irradiance of sunlight which directly reaches the earth surface without scattering, and the attenuation effect of atmospheric components on the irradiance is mainly considered; the scattering effect is divided into rayleigh scattering and Mie scattering effects according to the size of particles in the air, small gas molecules produce rayleigh scattering, and larger aerosol particles produce Mie scattering.
3) Direct ground illumination spectrum eb(λ) distribution equal to:
eb(λ)＝E(λ)AR(λ,mR)Ao(λ,mo)An(λ,mn)Ag(λ,mg)Aa(λ,ma)Aw(λ,mw) (1)
4) the irradiance of the ground at the moment is actually measured by the irradiator, and the proportion α occupied by the direct irradiation is obtained as follows:
α＝Ib/(Ib+Id) (2)
Ibis direct irradiation measured by an irradiator, IdIs the scattered radiation measured by an irradiator;
2. calculation of spectral difference correction coefficient using cloud cover as evaluation index
The cloud amount is used for representing the degree of coverage of a cloud layer to the sky in a certain area, and the value range of the cloud amount is 0 to 10, which means the area of the sky occupied by a cloud block. Fine, less, cloudy and cloudy are divided according to the amount of clouds. The whole sky is generally divided into 10 equal parts, and when the sky is clear and has no cloud or is shielded by the cloud by less than 0.5 part, the cloud amount is '0'; when the cloud covers half of the sky, the cloud amount is '5'. When the cloud amount is large, the exposed youth should be estimated, and then the cloud amount is calculated. When the cloud amount is small, the number of parts of the sky shaded by the cloud is directly estimated, and if the cloud block occupies 1/10 of the whole sky, the cloud amount is '1'; when the cloud patch occupies the sky 2/10, the cloud amount is "3", and so on.
1) One-dimensional linear interpolation processing is carried out on the spectral distribution data measured by the spectrometer to obtain the spectral distribution e of any measured wavelengthmea(λ)；
2) When the cloud H is Q, Q is a specific value of the cloud, and its value is 0 to 10. The spectral ranges measured by the spectrometers do not correspond one-to-one to the spectral distribution of the upper bound of the atmosphere, so that only spectral differences of arbitrary wavelengths λ within the wavelength measurement ranges of the spectrometers can be determined, but the system design of photovoltaic plantsFrom the point of view, this is also satisfactory, since components of different materials have corresponding spectral responses, none of which are all wavelength-intensive. Because the cloud amount is lower from the ground, the influence of the cloud amount on the direct irradiation is assumed to be similar to the influence of the scattering irradiation, so that only the influence of the cloud amount on the direct irradiation is analyzed, and the corresponding spectral distribution difference e is obtainedeQ(λ) is:
eeQ(λ)＝eb(λ)-αemea(λ) (3)
fig. 2 is a theoretical calculation distribution diagram and an actual measurement ground spectrum distribution diagram of the upper atmospheric boundary and the ground direct spectrum of ASTM E-490AM0, in which the wavelengths of the ground direct spectrum and the actual measurement ground spectrum distribution are not full wavelengths, but based on the measuring range of the spectrometer, it can be seen from the diagram that the influence of the cloud cover on each wavelength is different, and under the influence of different cloud covers, the influence on each wavelength should be different, so it can be assumed that the spectral difference caused by the cloud cover is a binary function of the cloud cover H and the wavelength λ, so the spectral difference correction coefficient function is defined as F (H, λ):
the specific spectral distribution difference curve under different clouds H is shown in fig. 3, and there are boundary conditions, when H is 0, the spectral error caused by the clouds is: e.g. of the typeeHWhen the discrete data are input into the surface fitting tool box of MATLAB, the multivariate linear regression processing and the quintic polynomial fitting are performed to obtain the function curve of the spectral difference correction coefficient as shown in fig. 4, it can be seen that the influence of different clouds on the spectral distribution difference is different, and the analytic formula of the function F (H, λ) after the surface fitting is as follows:
p00，p10，p01，p20，p11，p02，p30，p21，p12，p03，p40，p31，p22，p13，p04，p50，p41，p32，p23，p14，p05as coefficients, the values of each coefficient are shown in table 1;
TABLE 1 fitting coefficient values of spectral difference correction coefficient functions
| p00 | p10 | p01 | p20 | p11 | p02 | p30 |
| 0.0866 | -0.03091 | 0.07608 | -0.002587 | -0.02701 | -0.08756 | 0.01446 |
| p21 | p12 | p03 | p40 | p31 | p22 | p13 |
| -0.004073 | -0.00367 | -0.05656 | -0.006386 | 0.01217 | -0.001495 | -0.000276 |
| p04 | p50 | p41 | p32 | p23 | p14 | p05 |
| 0.04503 | -7.686e-15 | -0.004913 | 0.0008028 | 8.292e-05 | 0.004897 | 0.02493 |
The specific difference of spectral distribution caused by different clouds in different areas can be calculated by the analytical formula of the fitted spectral difference correction coefficient function F (H, lambda). Expressed as S (Δ H):
S(ΔH)＝F(H1-H2,λ) (6)
Δ H is the cloud cover difference in different regions, H1，H2Representing specific clouds in different regions.
The above description is only a preferred embodiment of the present invention, and it should be noted that, for those skilled in the art, several modifications and variations can be made without departing from the technical principle of the present invention, and these modifications and variations should also be regarded as the protection scope of the present invention.
Claims (4)
1. A quantification method for spectral distribution difference of different climate areas is characterized by comprising the following steps:
1) performing one-dimensional linear interpolation processing on the atmospheric upper-bound spectral distribution of ASTM E490AM0 to obtain irradiation E (lambda) corresponding to any wavelength, wherein lambda is the wavelength;
2) calculating the direct ground radiation spectral distribution;
3) measuring direct irradiation and scattering irradiation through an irradiation meter to obtain the proportion of the direct irradiation to the total irradiation;
4) calculating a spectral difference correction coefficient function with the cloud cover as an evaluation index; the method comprises the following steps:
4-1) carrying out one-dimensional linear interpolation processing on the spectral distribution data measured by the spectrometer to obtain the spectral distribution e of any measured wavelengthmea(λ)；
4-2) spectral difference e at arbitrary wavelength λ when the cloud number H ═ QeQ(λ) is:
eeQ(λ)＝eb(λ)-αemea(λ) (3)
wherein e isb(lambda) is the direct ground spectral distribution, α is the proportion of direct irradiation to total irradiation, Q is the specific value of cloud cover, which is 0-10;
4-3) assuming that the spectral difference caused by the cloud cover is a binary function with respect to the cloud cover H and the wavelength λ, defining a spectral difference correction coefficient function F (H, λ) as:
4-4) introductionBoundary conditions, when H is 0, the spectral error caused by the cloud cover is: e.g. of the typeeHWhen the discrete data are input into a surface fitting tool box of MATLAB, the analytical formula of the spectral difference correction coefficient function F (H, lambda) is obtained by multiple linear regression processing and fifth-order polynomial fitting, wherein the analytical formula is as follows:
wherein p is00，p10，p01，p20，p11，p02，p30，p21，p12，p03，p40，p31，p22，p13，p04，p50，p41，p32，p23，p14，p05As coefficients, the values of each coefficient are:
p00＝0.0866，p10＝-0.03091，p01＝0.07608，p20＝-0.002587，p11＝-0.02701，p02＝-0.08756，p30＝0.01446，
p21＝-0.004073，p12＝-0.00367，p03＝-0.05656，p40＝-0.006386，p31＝0.01217，p22＝-0.001495，p13＝-0.000276，
p04＝0.04503，p50＝-7.686e-15，p41＝-0.004913，p32＝0.0008028，p23＝8.292e-05，p14＝0.004897，p05＝0.02493；
5) calculating the spectral distribution difference caused by different cloud cover in different areas based on the spectral difference correction coefficient function in the step 4), wherein the spectral distribution difference S (delta H) is calculated as follows:
S(ΔH)＝F(H1-H2,λ) (6)
where Δ H is the cloud cover difference for different regions, H1，H2Representing clouds in different regions.
2. The method as claimed in claim 1, wherein the direct ground spectral distribution e is a direct ground spectral distributionb(λ) is:
eb(λ)＝E(λ)AR(λ,mR)Ao(λ,mo)An(λ,mn)Ag(λ,mg)Aa(λ,ma)Aw(λ,mw) (1)
wherein A isR(λ,mR) Is the Rayleigh scattering absorption coefficient, Ao(λ,mo) Is the ozone absorption coefficient, An(λ,mn) Is the absorption coefficient of nitrogen dioxide, Ag(λ,mg) As the absorption coefficient of the mixed gas, Aa(λ,ma) Is the absorption coefficient of the aerosol, Aw(λ,mw) Is the water vapor absorption coefficient, mR,mo,mn,ma,mg,mwRespectively the optical qualities of rayleigh scattering, ozone, nitrogen dioxide, aerosol, mixed gas and water vapor.
3. The method as claimed in claim 1, wherein the ratio α of direct irradiation to total irradiation is:
α＝Ib/(Ib+Id) (2)
wherein, IbIs direct irradiation measured by an irradiator, IdIs the scattered radiation measured by the radiometer.
4. The method of claim 1, wherein in the step 4), the cloud amount represents a degree of coverage of the cloud layer of a certain region to the sky, and the value ranges from 0 to 10, which means an area of the cloud layer occupying the sky.
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