thermal infrared remote sensing - university of … infrared remote sensing lecture 7 october 16,...
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Thermal Infrared Remote Sensing
Lecture 7 October 16, 2007
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Thermal infrared of EM spectrum
All objects have a temperature above absolute zero (0 K) emit EM energy (in 3.0-100 µm).
Human being has normal 98.6 ºF (37 ºC)
Our eyes are only sensitive to visible energy (0.4-0.7 µm). Human sense thermal energy through touch. while detectors (sensors) are sensitive to all EM spectrum.All objects (vegetation, soil, rock, water, concrete, etc) selectively absorb solar short-wavelength energy and radiate thermal infrared energy.
100 µm
3.0 µm
0.7 µm
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Thermal infrared remote sensing measures:
Land and ocean surface temperature, Atmospheric
Temperature and humilityTrace gas concentrations
Radiation balanceEmissivity
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Kinetic heat, radiant flux and temperature,
The energy of particles of matter in random motion is called kinetic heat (also referred to as internal, real, or true heat). We can measure the true kinetic temperature (Tkin) or concentration of this heat using a thermometer. - We perform this in situ (in place) temperature measurement when we are ill. - We can also measure the true kinetic internal temperature of soil or water by physically touching them with a thermometer.When these particles (have kinetic heat) collide they change their energy state and emit electromagnetic radiation called radiant flux (watts). The concentration of the amount of radiant flux exiting (emitted from) an object is its radiant temperature(Trad). There is usually a high positive correlation between the true kinetic temperature of an object (Tkin) and the amount of radiant flux radiated from the object (Trad). Therefore, we can utilize radiometers placed some distance from the object to measure its radiant temperature which hopefully correlates well with the object’s true kinetic temperature. This is the basis of thermal infrared remote sensing. Unfortunately, the relationship is not perfect, with the remote measurement of theradiant temperature always being slightly less than the true kinetic temperature of the object. This is due to a thermal property called emissivity.
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Planck equationBlack body radiation (W m-2µm-1) using Planck equation:We call T the physical (kinetic) temperature
)1(2),( )/5
2
−= kThce
hcTB λλπλ
λ
K=(°F-32)/1.8+273.15http://tes.asu.edu/MARS_SURVEYOR/MGSTES/TES_emissivity.html
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Not a perfect emitter
http://tes.asu.edu/MARS_SURVEYOR/MGSTES/TES_emissivity.html
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Emmisivity
Emissivityspectrum is the ratio of radiance spectrum of a non-perfect emitter over that of a perfect emitter (blackbody) at the same temperature
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Emmisivityused to identify mineral composition
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Brightness temperature, and physical (surface) temperature
Through radiance recorded by a remote sensor, if we use the Planck equation, we can get a temperature, which we call brightness temperature Tb, which is less than the real physical (or surface) temperature T.
)1(2),(
)1(2),( )/5
2
)/5
2
−⋅=⋅=
−= kThckThcb e
hcTBe
hcTLb λλλλ λ
πελελ
πλ
)1ln( / bTkhcekhcT λ
λλ εελ +−⋅=
h, Planck’s constant =6.626 x 10-34 Ws2
T, Kelvin (K)c, 3 x 108 m/sk, Boltzmann’s constant=1.38 x 10-23 Ws/K
L or B, radiance (Wm-2µm-1)c1=2πhc2=3.74 x 10-16 Wm2
c2=ch/k=0.0144 mK
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Thermal Radiation Raw
Blackbody (perfect absorber and emitter)Stenfan-Boltzmann Law (MB = σT4 in Wm-2)Wien’s Displacement Law (λmax = 2898/T)Emissivity (ε = MR / MB) at the same temperature MB = σTkin
4
MR = σTrad4
ε = MR / MB= Trad4 / Tkin
4
The The dominant wavelength (dominant wavelength (λmax ) ) provides valuable information about which part of the provides valuable information about which part of the thermal spectrum we might want to sense in. For example, if we athermal spectrum we might want to sense in. For example, if we are looking for re looking for 800 800 ˚̊K K forest firesforest fires that have a dominant wavelength of approximatelythat have a dominant wavelength of approximately 3.62 3.62 µµmm then the most then the most appropriate remote sensing system might be a appropriate remote sensing system might be a 33--5 5 µµmm thermal infrared detector. thermal infrared detector.
-- MODIS band 20MODIS band 20--25 are in 25 are in 33--5 5 µµmm..
If we are interested inIf we are interested in soil, water, and rock with ambient temperatures on the earthsoil, water, and rock with ambient temperatures on the earth’’s s surface of 300 surface of 300 ˚̊KK and a dominant wavelength of and a dominant wavelength of 9.66 9.66 µµm,m, then a thermal infrared detector then a thermal infrared detector operating in the operating in the 8 8 -- 14 14 µµmm region might be most appropriate. region might be most appropriate.
-- LandsatLandsat image thermal band (6) is in image thermal band (6) is in 10.410.4--12.512.5 µµmm-- ASTER band 12 and 13 are inASTER band 12 and 13 are in 8 8 -- 14 14 µµmm-- MODIS band 29MODIS band 29--30 and 3130 and 31--32 are in32 are in 8 8 -- 14 14 µµmm
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Diurnal Temperature Cycle of Typical MaterialsDiurnal Temperature Cycle of Typical MaterialsDiurnal Temperature Cycle of Typical Materials
• The diurnal cycle encompasses 24 hours. Beginning at sunrise, the earth begins intercepting mainly short wavelength energy (0.4 - 0.7 µm) from the Sun. From about 6:00 am to 8:00 pm, the terrain intercepts the incoming short wavelength energy and reflects much of it back into the atmosphere where we can use optical remote sensors to measure the reflected energy. • However, some of the incident short wavelength energy is absorbed by the terrain and then re-radiated back into the atmosphere as thermal infrared long wavelength radiation (3 - 100 µm). The outgoing longwave radiation reaches its highest value during the day when the surface temperature is highest. This peak usually lags two to four hours after the midday peak of incoming shortwave radiation, owing to the time taken to heat the soil. • The contribution of reflected short wavelength energy and emitted long wavelength energy causes an energy surplus to take place during the day. Both incoming and outgoing shortwave radiation become zero after sunset (except for light from the moon and stars), but outgoing longwave radiation continues all night.
•• The The diurnal cyclediurnal cycle encompasses 24 hours. Beginning at sunrise, the earth begins encompasses 24 hours. Beginning at sunrise, the earth begins intercepting mainly short wavelength energy (0.4 intercepting mainly short wavelength energy (0.4 -- 0.7 0.7 µµm) from the Sun. From about m) from the Sun. From about 6:00 am to 8:00 pm, the terrain intercepts the 6:00 am to 8:00 pm, the terrain intercepts the incoming short wavelength energyincoming short wavelength energy and and reflects much of it back into the atmosphere where we can use opreflects much of it back into the atmosphere where we can use optical remote sensors tical remote sensors to measure the reflected energy. to measure the reflected energy. •• However, some of the incident short wavelength energy is absorbHowever, some of the incident short wavelength energy is absorbed by the terrain ed by the terrain and then reand then re--radiated back into the atmosphere as thermal infrared long wavelradiated back into the atmosphere as thermal infrared long wavelength ength radiation (3 radiation (3 -- 100 100 µµm). The m). The outgoing outgoing longwavelongwave radiationradiation reaches its highest value reaches its highest value during the day when the surface temperature is highest. This peaduring the day when the surface temperature is highest. This peak usually lags two to k usually lags two to four hours after the midday peak of incoming shortwave radiationfour hours after the midday peak of incoming shortwave radiation, owing to the time , owing to the time taken to heat the soil. taken to heat the soil. •• The contribution of reflected short wavelength energy and emittThe contribution of reflected short wavelength energy and emitted long wavelength ed long wavelength energy causes an energy surplus to take place during the day. Boenergy causes an energy surplus to take place during the day. Both incoming and th incoming and outgoing shortwave radiation become zero after sunset (except fooutgoing shortwave radiation become zero after sunset (except for light from the r light from the moon and stars), but outgoing moon and stars), but outgoing longwavelongwave radiation continues all night. radiation continues all night.
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Peak Period of Daily Outgoing Longwave
Radiation and the Diurnal Radiant Temperature of
Soils and Rocks, Vegetation, Water, Moist Soil and Metal Objects
Peak Period of Daily Peak Period of Daily Outgoing Outgoing LongwaveLongwave
Radiation and the Diurnal Radiation and the Diurnal Radiant Temperature of Radiant Temperature of
Soils and Rocks, Soils and Rocks, Vegetation, Water, Moist Vegetation, Water, Moist Soil and Metal ObjectsSoil and Metal Objects
Temperature
At the thermal crossover times, most of the materials have the almost same radiant temperature, it is not wise todo thermal remote sensing.
Water and vegetation have higher thermalcapacity. In different time of thermal images, there are different performances even the materials.
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Kirchoff’s radiation law
Φiλ = Φrλ + Φτλ + Φαλ
1 = rλ + τλ + αλ
Kirchoff found in the infrared portion of the spectrum αλ = ελ: “good absorbers are good emitters”Most materials does not lose any incident energy to transmittance, i.e. τλ = 0, so we can get 1 = rλ + αλ= rλ + ελ (or A + ε)
This means reflectivity and emissivity has a inverse relationship: “good reflectors are poor emitters”
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NASA’s Earth Observing System missions with Thermal IR capability
Landsat systems (MSS, TM, ETM+)ETM+ has a 60 m band at 10.5-12.5 µm)
TRMMCERES
EOS Terra (Dec. 1999)CERES, MODIS, ASTER, MOPITT
EOS Aqua (May 2002)AIRS, CERES, MODIS
EOS Aura (July 2004)HIRDLS, TES
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Source: Jeff Dozier
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Source: Jeff Dozier
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Source: Jeff Dozier
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Source: Jeff Dozier
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Source: Jeff Dozier
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Source: Jeff Dozier
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Source: Jeff Dozier
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MODIS land surface temperature and emissivity product led by Dr. Wan
http://www.icess.ucsb.edu/modis/modis-lst.html
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Calibration and validation of
MODIS T and E in Sevilleta, NM
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Urban Heat Island of San Antonio downtown area detected by MODIS temperature product2:30 pm (CDT), July 14, 2004
306308310312314316318320322324
0 20 40 60 80 100 120 140
Distance (pixel)
T (K
)
X profile Y Profile NW-SE Profile NE-SW Profile
Xie and Ytuarte, 2005
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Urban Heat Island of San Antonio downtown area detected by MODIS temperature product2:00 am (CDT), July 15, 2004
288289290291292293294295296297
0 20 40 60 80 100 120 140
Distance (pixel)
T (K
)
X Profile Y Profile NW-SE NE-SW
Xie and Ytuarte, 2005
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Source: Jeff Dozier
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Active fire detection:MODIS fire and thermal anomalies products
http://modis-fire.gsfc.nasa.gov/index.asp
Image caption: Fires in the Bahamas, Florida and Cuba (03 April 2004, 18:30 UTC) identified using MODIS Aqua and outlined in red on the MODIS 1km corrected reflectance product
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Source: Jeff Dozier
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NASA Mars missions with Thermal IR capability
Mars global surveyor Launched 11/1996. landed 12/1997, 3/1999 began have maps TES (6-50 µm)
Mars Odyssey Launched 4/7/2001, landed 10/24/2001THEMIS (5 visible at 18m, 10 thermal (6.78-10.88 µm) at 100m)
Mars Spirit RoverLaunched 6/10/2003, landed 1/3/2004 Mini-TES
Mars opportunity RoverLaunched 7/7/2003, landed 1/24/2004Mini-TES
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What is TES? Thermal Emission Spectroscopy
Michelson Interferometer, is the thermal IR portion of TES, covers the 6-50 µm (1655-200 cm-1) wavelength range, with spectral sampling 5 and10 cm-1 (spectral resolution ~10 - 20 cm-1), 286 or 142 bands
Bolometric thermal radiance channel (5.5 to ~100 µm)
Solar reflectance channel (0.3 to 2.7 µm ), to measure the brightness of reflected solar energy
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MGS - TES
Entered Mars orbit on board the MGS on Sep.11,1997
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How does TES determine surface composition?
Mixed Spectra
Rocks are a mixture of minerals
Emissivity spectrum from individual components of a mixture add together in a simple linear fashion.
The linearity of the mixed spectrum allows it to be deconvolved.
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Two distinct surface types found on Mars
Type 1 - Similar to Basalt Type 2 – Andesite?( < 52 wt% SiO2) ( 52-63 wt% SiO2)Mostly in southern highlands Mostly in northern lowlands
(note the larger percentage of high silica glass is the main diff.)
Bandfield et al. (2000), Hamilton et al. (2001)
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MGS TES Basalt Map
Basalt (Type 1 spectra) concentrated in Southern HighlandsBandfield et al. (2000), Hamilton et al. (2001)
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MGS TES Andesite Map
Andesite (type 2 spectra) appears concentrated in Northern Lowlands, but also intermixed with basalt in Southern Highlands.Bandfield et al. (2000), Hamilton et al. (2001)
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Mars Hematite detected by TES
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Rocks at the Mars Opportunity Rover landing site (on 1/24/2004, launched 7/7/2003)
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NOAA and other missions with Thermal IR capability
GOES (NOAA)3.78-4.03 (4 km), 6.47-7.02 (8 km), 10.2-11.2 (4 km), and 11.5-12.5 (4 km)
AVHRR (NOAA)3.55-3.93, 10.30-11.30, 11.5-12.5. all in 1.1 km
NPOESS (joint NOAA/NASA/DoD)Middle-wave thermal 8 bands, long-wave thermal 4 bandshttp://www.ipo.noaa.gov/Technology/viirs_summary.html400-800 m
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One application: detection of loss of heat from buildings due
to faulty insulation
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Typical IR imagery of Heat Loss in Residential Structures
24.0°F
43.0°F
25
30
35
40
Furnace Vent
Vent Duct
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Energy Gain (Floor Leak)
Missing Insulation in Vaulted Ceiling Area
Moisture
Heat Loss Heat Loss
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Typical Institutional Building Heat Loss
Typical Air Leak Patterns
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Apartment balcony door during the summer the A/C system reads a slight positive pressure but this building is under a negative
pressure, bringing in warm, moist air into the building throughwalls, doors, ceilings and under the floor system.
Typical air in-leakage at doors
Typical pattern of air in-leakage
Typical pattern of air in-leakage
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Air Leakagefrom non-
insulated areas and window
frames.