CN102253184A - Remote sensing inversion method for land surface evapotranspiration of arid and semi-arid regions - Google Patents
Remote sensing inversion method for land surface evapotranspiration of arid and semi-arid regions Download PDFInfo
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Abstract
The invention discloses a remote sensing inversion method for land surface evapotranspiration of arid and semi-arid regions. The method comprises the steps of: acquiring and processing EOS/MODISE (Earth Observing System/Moderate-resolution Imaging Spectroradiometer) remotely sensed data; performing the inversion of near-surface temperature and computing atmospheric transmittance; obtaining a land surface latent heat flux by solving a net radiation quantity, a soil heat flux and a sensible heat flux according to a land surface energy balance equation; and figuring out land surface evapotranspiration data according to the land surface latent heat flux. According to the invention, aiming at the characteristics of rare meteorological stations in the arid region of Northwest China, a near-surface temperature inversion model and an atmospheric transmittance model both based on remotely sensed data are established, and the temperature obtained by the remote sensing inversion is used for participating in the computation instead of the observed temperatures of the stations; therefore, requirements on meteorological and other observation data are reduced.
Description
Technical field
The present invention relates to a kind of face of land remote sensing inversion method that evapotranspires, relate in particular to a kind of characteristics and mainly use the technical method of satellite remote sensing data inverting face of land evapotranspiration, be used for the water resource monitoring and the management of arid and semiarid zone at arid and semi-arid area weather station rareness.
Background technology
Evapotranspiring in the face of land is key link in the Water Cycle process, also is the dominant term of energy equilibrium.Clearly be familiar with the spatial-temporal characteristics of evapotranspiring and have outstanding scientific value, help to further investigate land face process and correctly assess weather and mankind's activity Ecosystem System Influence for Water Cycle in understanding on a large scale and energy equilibrium process.Obtain accurately the face of land data of evapotranspiring, can provide important reference information for the regional water resources management, to the draining of instructing agricultural and irrigation, monitor drought using crop, etc. significance arranged.
Traditional face of land research method of evapotranspiring is often calculated according to meteorology or hydrology data, is confined to " point " yardstick, the point value of ad-hoc location can only be provided and can not calculate the face of land on regional scale and evapotranspire.And in fact, evapotranspire owing to the influence that is subjected to precipitation, soil hydrologic parameter and factors such as vegetation pattern and coverage has very strong special heterogeneity in the face of land.Evapotranspire and can only be extrapolated for the face yardstick by point scale by the method for space interpolation in the face of land that classic method calculates.The effect of space interpolation depends on website density and distribution situation to a great extent, because the complicacy of face of land underlying surface makes this method can cause bigger error when carrying out the space scale expansion, interpolation precision is undesirable under the situation of or website skewness less in website density.And arid and semi-arid area observation website is sparse and distribute serious unevenly, and spatial distribution state evapotranspires to be difficult to obtain accurately the face of land by space interpolation.
The calculating of evapotranspiring on the face of land that develops into of satellite remote sensing technology provides a kind of new means, satellite remote sensing have macroscopic view, dynamically, unique advantage such as convenient, obtain the face of land continuous on the space information of evapotranspiring in can be on a large scale.In the last few years, carried out the research of evapotranspiring both at home and abroad in succession based on the regional face of land of remote sensing data.But research is confined to humid region more, and is also fewer at the remote-sensing inversion research of evapotranspiring in the face of land, arid and semi-arid area.Existing research at the arid and semi-arid area mainly adopts existing SEBAL model directly to calculate, and the SEBAL Model parameter obtains based on the observational data of humid regions such as Holland, Brazil, has notable difference with the actual conditions in Chinese arid and semi-arid area.
Summary of the invention
Technical matters to be solved by this invention is the defective at the above-mentioned background technology, based on the EOS/MODIS satellite data, proposes a kind of face of land at arid and semi-arid area remote sensing inversion method that evapotranspires by face of land principle of energy balance.
The present invention is for solving the problems of the technologies described above by the following technical solutions:
A kind of face of land at arid and semi-arid area remote sensing inversion method that evapotranspires comprises the steps:
Steps A obtains and handles the EOS/MODIS remotely-sensed data:
A-1 obtains remotely-sensed data, and described remotely-sensed data comprises that the soil covers index, vegetation index, surface temperature and albedo data;
A-2 carries out the space projection conversion to all data, and is unified under identical georeferencing framework;
A-3, operate time sequence harmonic wave approximating method goes cloud to handle to vegetation index in the remotely-sensed data and surface temperature;
A-4, solar zenith angle data during from the imaging of vegetation index extracting data;
A-5 monthly synthesizes processing with surface temperature and albedo data, is complementary with normalized differential vegetation index NDVI data;
Step B, inverting of near surface temperature and atmospheric transmittance calculate:
B-1 is the data collection with the remotely-sensed data of meteorological site, sets up the empirical equation of near surface temperature by regretional analysis:
In the formula,
T a Be near surface temperature (unit: ℃),
T s Be surface temperature (unit: ℃),
hFor height above sea level (unit: m),
NDVIBe normalized differential vegetation index,
θBe solar zenith angle (unit: radian);
B-2 concerns with The altitude change by radiation transfer equation simulation atmospheric transmittance, sets up atmospheric transmittance τ
SwEmpirical equation:
(2)
Step C, face of land latent heat flux calculates:
C-1, set up face of land energy-balance equation:
In the formula,
R n Be net radiation flux,
GBe soil heat flux,
HBe sensible heat flux,
LEBe latent heat flux;
C-2 calculates surface net radiation flux
R n , computing formula is:
In the formula,
αBe surface albedo,
εBe face of land emissivity,
R s ↓ be sun shortwave radiation,
R L ↓ be the atmospheric long wave radiation that descending long-wave radiation promptly arrives the face of land,
R L ↑ be that up long-wave radiation is the ground long-wave radiation; Wherein:
R
s↓, R
L↓ and R
L↑ computing formula as follows:
In the formula,
G Sc Be solar constant,
θFor solar zenith angle (unit: radian),
E 0 Be the solar distance correction coefficient,
ε a Be the atmosphere emissivity,
δBe Si Tefen-Boltzmann constant,
T a For carry out the resulting near surface temperature of remote-sensing inversion according to formula (1);
C-3 calculates soil heat flux, is divided into the vegetation-covered area and non-vegetation coverage calculates respectively:
In the formula,
c g It is empirical constant at different surface;
C-4 calculates sensible heat flux, and computing formula is:
（7）
In the formula,
ρBe atmospheric density (units/m
3),
C p Be pressurization by compressed air specific heat (J/kgK of unit),
DTBe the ground vapour temperature difference (T
s-T
a),
r Ah Be aerodynamic resistance (s/m of unit);
C-4-1 obtains the friction speed under the indifferent equilibrium degree
μ *With aerodynamic resistance
r Ah :
In the formula,
kBe von Karman constant,
μ z Be the wind speed (m/s) at height z place,
zBe certain reference altitude (m),
z 0h Be face of land heat delivered roughness (m),
z 0h With face of land power roughness z
0mThe pass be:
z 0h =0.1*
z 0m
C-4-2, introduce Moin-obukov length by the recursive operation that repeatedly circulates to friction speed
μ * And aerodynamic resistance
R Ah Revise, up to obtaining stable sensible heat flux
HTill the value;
C-5 calculates net radiation flux respectively according to above-mentioned steps
R n , soil heat flux
GAnd sensible heat flux
H, according to formula (3), calculate face of land latent heat flux then
LE
Step D, the face of land calculating of evapotranspiring:
D-1, the latent heat flux that obtains according to step C-5
LE, calculate face of land evapotranspiration according to following formula
ET:
In the formula,
ETBe evapotranspiration (m of unit) that λ is the latent heat of vaporization (J/kg of unit), λ is calculated by following formula:
The present invention adopts above technical scheme compared with prior art, has following technique effect:
The characteristics that the present invention is directed to NORTHWEST CHINA arid and semi-arid area have been set up suitable temperature inverse model and atmospheric transmittance computation model, and have adopted the temperature of remote-sensing inversion rather than the observation temperature interpolation result of limited several websites in computation process.The present invention has better applicability and specific aim than other remote sensing inversion method that evapotranspires in the arid and semi-arid area.
The present invention has made full use of the multiple remote sensing product of EOS/MODIS data, has reduced the requirement to observational datas such as meteorologies.
Description of drawings
Fig. 1 is the comparison diagram of Bosten basin remote sensing appraising temperature value and actual observed value;
Fig. 2 is the process flow diagram of setting up of surface layer temperature remote-sensing inversion model;
Fig. 3 is the comparison diagram of Bosten basin remote sensing appraising evapotranspiration and actual observed value.
Embodiment
Below in conjunction with accompanying drawing technical scheme of the present invention is described in further detail:
(1) EOS/MODIS Remote Sensing Data Processing
The EOS/MODIS remotely-sensed data that the present invention uses comprises that the soil covers product, month synthetic vegetation index product, 8 days synthetic surface temperature products and 16 days synthetic albedo products.At first all data are carried out the space projection conversion, unified under identical georeferencing framework; Operate time sequence harmonic wave approximating method goes cloud to handle to vegetation index and surface temperature afterwards, eliminates cloud and covers the data disappearance problem that causes.Solar zenith angle data when from the vegetation index product, being extracted into picture; Then surface temperature and albedo data are monthly synthesized processing, be complementary with the NDVI data.
(2) inverting of near surface temperature and atmospheric transmittance calculate
Difference between near surface temperature and the surface temperature is the material impact factor of face of land energy equilibrium process, has vital role in refutation process is evapotranspired on the face of land.Because arid and semi-arid area meteorological site rareness and height above sea level are widely different, can not get temperature space distribution information accurately with meteorological site observation temperature interpolation.The present invention proposes a kind of near surface temperature inversion method based on remotely-sensed data.
With month synthetic daily temperature data of meteorological site and the remotely-sensed datas such as surface temperature, height above sea level, NDVI and solar zenith angle of correspondence position is the data collection, sets up the empirical equation of near surface temperature by regretional analysis.Because the face of land covers for ice and snow easily under the low temperature condition in the winter time, and be natural terrains such as bare area, vegetation under the general case, the different covering situations power transfer process between the face of land-atmosphere that makes exists than big-difference, therefore whether has set up equation respectively greater than 0 ℃ according to surface temperature:
In the formula, T
aBe near surface temperature (unit: ℃), T
sBe surface temperature (unit: ℃) that H is that (unit: m), NDVI is a normalized differential vegetation index to height above sea level, and θ is a solar zenith angle (unit: radian).
As shown in Figure 1, be the test block with Bosten basin, Xinjiang, temperature and the meteorological site observation temperature that utilizes formula 1 inverting to obtain is compared, inversion error is 2.56 ℃, coefficient of determination R
2Be 0.9298, show that this method can well estimate near surface temperature.
Atmospheric transmittance is for calculating the important parameter of solar radiation, the experimental formulas that adopt the SEBAL model in the existing remote sensing technique that evapotranspires more, this formula obtains according to the observational data match at humid regions such as Holland, Brazil, has than mistake in Chinese arid and semi-arid area.The present invention concerns with The altitude change by radiation transfer equation simulation atmospheric transmittance according to northwest China's aerosol optical characteristics, sets up empirical equation (the coefficient of determination R of atmospheric transmittance
2=0.9985):
In the formula, H is face of land height above sea level (m of unit).
(3) face of land latent heat flux calculates
Face of land energy equilibrium is the theoretical foundation that remote sensing appraising evapotranspires, and under the situation of not considering photosynthesis power consumption and horizontal direction energy transport, face of land energy-balance equation can be expressed as:
In the formula, R
nBe net radiation, G is a soil heat flux, and H is a sensible heat flux, and LE is a latent heat flux.Calculate latent heat flux by calculating net radiation flux, soil heat flux and sensible heat flux, further calculating can obtain face of land evapotranspiration.
Surface net radiation R
nComputing formula be:
In the formula, α is a surface albedo, and ε is a face of land emissivity, R
s↓ be sun shortwave radiation, R
L↓ be the atmospheric long wave radiation that descending long-wave radiation promptly arrives the face of land, R
L↑ be that up long-wave radiation is the ground long-wave radiation.
R
s↓, R
L↓ and R
L↑ computing formula as follows:
（5）
In the formula, G
ScBe solar constant, θ is a solar zenith angle, τ
SwBe atmospheric transmittance, E
0Be solar distance correction coefficient, ε
aBe the atmosphere emissivity, δ is Si Tefen-Boltzmann constant, T
aFor carry out the resulting near surface temperature of remote-sensing inversion according to formula 1.
Consider that arid and semi-arid area vegetation coverage is lower, many areas are the Gobi desert bare area, therefore are divided into the vegetation-covered area when calculating soil heat flux and non-vegetation coverage calculates respectively.
In the formula, c
gBe the empirical constant at different surface, comprehensive forefathers are at the observed result of various faces of land type, c
gValue sees Table 1.
The c of table 1 different surface type
gValue
The computing formula of sensible heat flux is:
In the formula, ρ is atmospheric density (units/m
3), C
pBe pressurization by compressed air specific heat (J/kgK of unit) that dT is the ground vapour temperature difference (T
s-T
a), r
AhBe aerodynamic resistance (s/m of unit).
Relatively stable at the blending height layer wind speed that distance face of land 200m highly locates, can suppose that this wind speed highly is not subjected to the influence of surface roughness, obtains friction speed μ * and aerodynamic resistance r under the indifferent equilibrium degree thus
Ah
In the formula, μ
*Be friction speed, μ
zBe the wind speed (m/s) at height z place, z is certain reference altitude (m), z
0hBe face of land heat delivered roughness (m), with face of land power roughness z
0mThe pass be: z
0h=0.1*z
0m, k is a von Karman constant.
The present invention has directly quoted the LDAS of the NASA soil Data Assimilation system face of land power roughness Z in the vegetation parameter database month by month
0m, this database provides 12 kinds of UMD soil cover types (except water body) at annual 12 months Z
0mIn addition, the Z of water body
0mBe made as 0.0003 with reference to former study.
Atmosphere has three kinds of states: unstable, stable and neutral, atmospheric condition can influence the aerodynamic resistance of heat delivered, therefore need to introduce Moin-obukov length by the recursive operation that repeatedly circulates to friction speed μ
*With aerodynamic resistance R
AhRevise, till obtaining stable sensible heat flux H value.
Calculate after net radiation, face of land thermoflux and the sensible heat flux, can calculate face of land latent heat flux according to face of land principle of energy balance (formula 3).
(4) face of land calculating of evapotranspiring
Calculate after the sensible heat flux, can calculate face of land evapotranspiration according to following formula:
In the formula, ET is evapotranspiration (m of unit), and λ is the latent heat of vaporization (J/kg of unit), can be calculated by following formula:
The remote-sensing inversion model flow process of evapotranspiring in the face of land, arid and semi-arid area is seen Fig. 2.
(5) case verification
For the result of being evapotranspired in the face of land of the inventive method verifies, with Bosten basin, Xinjiang is study area, by EOS/MODIS surface temperature, vegetation index, albedo and soil cover data based on this method inverting face of land evapotranspiration, and Bohu weather station observational data in result and the basin contrasted, as shown in Figure 3.Both coefficient R are 0.97(sample number 59), mean absolute error MAE is 12.12mm, and relative error MRE is 13.84%, illustrates that the remote-sensing inversion value of evapotranspiring precision is higher, and the result is rationally credible.
In sum, the invention has the advantages that the following aspects:
1. at the sparse situation that is unfavorable for the temperature space interpolation of arid and semi-arid area meteorological site, set up temperature inverse model based on remotely-sensed data.
2. set up atmospheric transmittance computation model at northwest China.
3. in calculating face of land latent heat flux process, utilize remote-sensing inversion temperature to calculate, rather than the observation temperature interpolation result of limited several websites.
Claims (1)
1. the face of land at arid and semi-arid area remote sensing inversion method that evapotranspires is characterized in that comprising the steps:
Steps A obtains and handles the EOS/MODIS remotely-sensed data:
A-1 obtains remotely-sensed data, and described remotely-sensed data comprises that the soil covers index, vegetation index, surface temperature and albedo data;
A-2 carries out the space projection conversion to all data, and is unified under identical georeferencing framework;
A-3, operate time sequence harmonic wave approximating method goes cloud to handle to vegetation index in the remotely-sensed data and surface temperature;
A-4, solar zenith angle data during from the imaging of vegetation index extracting data;
A-5 monthly synthesizes processing with surface temperature and albedo data, is complementary with normalized differential vegetation index NDVI data;
Step B, inverting of near surface temperature and atmospheric transmittance calculate:
B-1 is the data collection with the remotely-sensed data of meteorological site, sets up the empirical equation of near surface temperature by regretional analysis:
In the formula,
T a Be near surface temperature (unit: ℃),
T s Be surface temperature (unit: ℃),
hFor height above sea level (unit: m),
NDVIBe normalized differential vegetation index,
θBe solar zenith angle (unit: radian);
B-2 concerns with The altitude change by radiation transfer equation simulation atmospheric transmittance, sets up atmospheric transmittance τ
SwEmpirical equation:
(2)
Step C, face of land latent heat flux calculates:
C-1, set up face of land energy-balance equation:
In the formula,
R n Be net radiation flux,
GBe soil heat flux,
HBe sensible heat flux,
LEBe latent heat flux;
C-2 calculates surface net radiation flux
R n , computing formula is:
In the formula,
αBe surface albedo,
εBe face of land emissivity,
R s ↓ be sun shortwave radiation,
R L ↓ be the atmospheric long wave radiation that descending long-wave radiation promptly arrives the face of land,
R L ↑ be that up long-wave radiation is the ground long-wave radiation; Wherein:
R
s↓, R
L↓ and R
L↑ computing formula as follows:
In the formula,
G Sc Be solar constant,
θFor solar zenith angle (unit: radian),
E 0 Be the solar distance correction coefficient,
ε a Be the atmosphere emissivity,
δBe Si Tefen-Boltzmann constant,
T a For carry out the resulting near surface temperature of remote-sensing inversion according to formula (1);
C-3 calculates soil heat flux, is divided into the vegetation-covered area and non-vegetation coverage calculates respectively:
（6）
In the formula,
c g It is empirical constant at different surface;
C-4 calculates sensible heat flux, and computing formula is:
In the formula,
ρBe atmospheric density (units/m
3),
C p Be pressurization by compressed air specific heat (J/kgK of unit),
DTBe the ground vapour temperature difference (T
s-T
a),
r Ah Be aerodynamic resistance (s/m of unit);
C-4-1 obtains the friction speed under the indifferent equilibrium degree
μ *With aerodynamic resistance
r Ah :
In the formula,
kBe von Karman constant,
μ z Be the wind speed (m/s) at height z place,
zBe certain reference altitude (m),
z 0h Be face of land heat delivered roughness (m),
z 0h With face of land power roughness z
0mThe pass be:
z 0h =0.1*
z 0m
C-4-2, introduce Moin-obukov length by the recursive operation that repeatedly circulates to friction speed
μ * And aerodynamic resistance
R Ah Revise, up to obtaining stable sensible heat flux
HTill the value;
C-5 calculates net radiation flux respectively according to above-mentioned steps
R n , soil heat flux
GAnd sensible heat flux
H, according to formula (3), calculate face of land latent heat flux then
LE
Step D, the face of land calculating of evapotranspiring:
D-1, the latent heat flux that obtains according to step C-5
LE, calculate face of land evapotranspiration according to following formula
ET:
In the formula,
ETBe evapotranspiration (m of unit) that λ is the latent heat of vaporization (J/kg of unit), λ is calculated by following formula:
。
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