# Algorithm for Automated Mapping of Land Surface Temperature Using LANDSAT 8 Satellite Data

Authors: Ugur Avdan; Gordana Jovanovska
Journal: Journal of Sensors
 (2016)

---

## Abstract

Land surface temperature is an important factor in many areas, such as global climate change, hydrological, geo-/biophysical, and urban land use/land cover. As the latest launched satellite from the LANDSAT family, LANDSAT 8 has opened new possibilities for understanding the events on the Earth with remote sensing. This study presents an algorithm for the automatic mapping of land surface temperature from LANDSAT 8 data. The tool was developed using the LANDSAT 8 thermal infrared sensor Band 10 data. Different methods and formulas were used in the algorithm that successfully retrieves the land surface temperature to help us study the thermal environment of the ground surface. To verify the algorithm, the land surface temperature and the near-air temperature were compared. The results showed that, for the first case, the standard deviation was 2.4°C, and for the second case, it was 2.7°C. For future studies, the tool should be refined within situ measurements of land surface temperature.


---

## Body

## 1. Introduction

Land surface temperature (LST) is defined as the temperature felt when the land surface is touched with the hands or the skin temperature of the ground [1]. As one of the most important aspects of the land surface, LST has been a main topic for developing methodologies to be measured from space. LST is an important factor in many areas of studies, such as global climate change, hydrological and agricultural processes, and urban land use/land cover. Calculating LST from remote sensed images is needed since it is an important factor controlling most physical, chemical, and biological processes of the Earth [2]. There is a growing awareness among environmental scientists that remote sensing can and must play a role in providing the data needed to assess ecosystems conditions and to monitor change at all special scales [3]. The tool developed in this paper is simple and does not require any background knowledge so scientists can use it very easy in their researches.The algorithm introduced in this paper has been developed using ERDAS IMAGINE 2014, with the Model Maker allowing us to create a model that will repeat the process automatically, and it is easy to develop a simple tool useful for doing pixel calculations. Without the tool, the process of retrieving LST is very long, and it is prone to many mistakes. The tool also can be developed in any software supporting pixel calculations from a given image, following step by step this paper. Although an LST retrieval method for LANDSAT 8 has been developed [1, 4], a tool is needed for the complicated process of obtaining the LST. A similar study for retrieving LST in ERDAS IMAGINE has been conducted for LANDSAT 7 data [5] but not for LANDSAT 8. The tool presented in this paper is used for calculating the LST of a given LANDSAT 8 image with the input of the fourth (red wavelength/micrometres, 0.64–0.67), fifth (near infrared (NIR) wavelength/micrometres, 0.85–0.88), and tenth (thermal infrared sensor (TIRS) wavelength/micrometres, 10.60–11.19) bands. Following January 6, 2014, recommendations of USGS of not using TIRS Band 11 due to its larger calibration uncertainty, only Band 10 was included in the algorithm.


## 2. Data and Methods

The algorithm was created in ERDAS IMAGINE 2014, and it can only be used to process LANDSAT 8 data because of the data complexity. The LST of any Landsat 8 satellite image can be retrieved following the steps of Figure1. The data of Landsat 8 is available at the Earth Explorer website free of charge. In this study, the TIR band 10 was used to estimate brightness temperature and bands 4 and 5 were used for calculating the NDVI. The metadata of the satellite images used in the algorithm is presented in Table 1.Table 1
Metadata of the satellite images.
Thermal constant, Band 10
K
1
1321.08
K
2
777.89
Rescaling factor, Band 10
M
L
0.000342
A
L
0.1
Correction, Band 10
O
i
0.29Figure 1
Flowchart for LST retrieval.


### 2.1. Top of Atmospheric Spectral Radiance

The first step of the algorithm is the input of Band 10. After inputting band 10, in the background, the tool uses formulas taken from the USGS web page for retrieving the top of atmospheric (TOA) spectral radiance (L
λ): (1)
L
λ
=
M
L
∗
Q
cal
+
A
L
-
O
i
,where M
L represents the band-specific multiplicative rescaling factor, Q
cal is the Band 10 image, A
L is the band-specific additive rescaling factor, and O
i is the correction for Band 10 [6].


### 2.2. Conversion of Radiance to At-Sensor Temperature

After the digital numbers (DNs) are converted to reflection, the TIRS band data should be converted from spectral radiance to brightness temperature (BT) using the thermal constants provided in the metadata file. The following equation is used in the tool’s algorithm to convert reflectance to BT [7]:(2)
BT
=
K
2
ln
⁡
K
1
/
L
λ
+
1
-
273.15
,where K
1 and K
2 stand for the band-specific thermal conversion constants from the metadata.For obtaining the results in Celsius, the radiant temperature is revised by adding the absolute zero (approx. −273.15°C) [8].


### 2.3. NDVI Method for Emissivity Correction

#### 2.3.1. Calculating NDVI

Landsat visible and near-infrared bands were used for calculating the Normal Difference Vegetation Index (NDVI). The importance of estimating the NDVI is essential since the amount of vegetation present is an important factor and NDVI can be used to infer general vegetation condition [9]. The calculation of the NDVI is important because, afterward, the proportion of the vegetation (P
v) should be calculated, and they are highly related with the NDVI, and emissivity (ε) should be calculated, which is related to the P
v: (3)
NDVI
=
NIR
band
5
-
R
band
4
NIR
band
5
+
R
band
4
,where NIR represents the near-infrared band (Band 5) and R represents the red band (Band 4).


#### 2.3.2. Calculating the Proportion of Vegetation

P
v is calculated according to (4). A method for calculating P
v [4] suggests using the NDVI values for vegetation and soil (N
D
V
I
v
=
0.5 and N
D
V
I
s
=
0.2) to apply in global conditions [10]: (4)
P
v
=
NDVI
-
NDVI
s
NDVI
v
-
NDVI
s
2
.However, since the NDVI values differ for every area, the value for vegetated surfaces, 0.5, may be too low. Global values from NDVI can be calculated from at-surface reflectivities, but it would not be possible to establish global values in the case of an NDVI computed from TOA reflectivities, since N
D
V
I
v and N
D
V
I
s will depend on the atmospheric conditions [11].


#### 2.3.3. Calculating Land Surface Emissivity

The land surface emissivity (LSE (ε)) must be known in order to estimate LST, since the LSE is a proportionality factor that scales blackbody radiance (Planck’s law) to predict emitted radiance, and it is the efficiency of transmitting thermal energy across the surface into the atmosphere [12]. The determination of the ground emissivity is calculated conditionally as suggested in [10]:(5)
ε
λ
=
ε
v
λ
P
v
+
ε
s
λ
1
-
P
v
+
C
λ
,where ε
vand ε
s are the vegetation and soil emissivities, respectively, and C represents the surface roughness (C = 0 for homogenous and flat surfaces) taken as a constant value of 0.005 [13]. The condition can be represented with the following formula and the emissivity constant values shown in Table 1 [4]:(6)
ε
λ
=
ε
s
λ
,
NDVI
<
NDVI
s
,
ε
v
λ
P
v
+
ε
s
λ
1
-
P
v
+
C
,
NDVI
s
≤
NDVI
≤
NDVI
v
,
ε
s
λ
+
C
,
NDVI
>
NDVI
v
.When the NDVI is less than 0, it is classified as water, and the emissivity value of 0.991 is assigned. For NDVI values between 0 and 0.2, it is considered that the land is covered with soil, and the emissivity value of 0.996 is assigned. Values between 0.2 and 0.5 are considered mixtures of soil and vegetation cover and (6) is applied to retrieve the emissivity. In the last case, when the NDVI value is greater than 0.5, it is considered to be covered with vegetation, and the value of 0.973 is assigned.The last step of retrieving the LST or the emissivity-corrected land surface temperatureT
s is computed as follows [14]: (7)
T
s
=
BT
1
+
λ
BT
/
ρ
ln
⁡
ε
λ
,where T
s is the LST in Celsius (°C, (2)), BT is at-sensor BT (°C), λ is the wavelength of emitted radiance (for which the peak response and the average of the limiting wavelength (λ
=
10.895) [15] will be used), ε
λ is the emissivity calculated in (6), and(8)
ρ
=
h
c
σ
=
1.438
×
10
-
2
m
K
,where σ is the Boltzmann constant (1.38 × 10−23 J/K),  h is Planck’s constant (6.626 × 10−34 J s), and c is the velocity of light (2.998 × 108 m/s) [9].


## 2.1. Top of Atmospheric Spectral Radiance

The first step of the algorithm is the input of Band 10. After inputting band 10, in the background, the tool uses formulas taken from the USGS web page for retrieving the top of atmospheric (TOA) spectral radiance (L
λ): (1)
L
λ
=
M
L
∗
Q
cal
+
A
L
-
O
i
,where M
L represents the band-specific multiplicative rescaling factor, Q
cal is the Band 10 image, A
L is the band-specific additive rescaling factor, and O
i is the correction for Band 10 [6].


## 2.2. Conversion of Radiance to At-Sensor Temperature

After the digital numbers (DNs) are converted to reflection, the TIRS band data should be converted from spectral radiance to brightness temperature (BT) using the thermal constants provided in the metadata file. The following equation is used in the tool’s algorithm to convert reflectance to BT [7]:(2)
BT
=
K
2
ln
⁡
K
1
/
L
λ
+
1
-
273.15
,where K
1 and K
2 stand for the band-specific thermal conversion constants from the metadata.For obtaining the results in Celsius, the radiant temperature is revised by adding the absolute zero (approx. −273.15°C) [8].


## 2.3. NDVI Method for Emissivity Correction

### 2.3.1. Calculating NDVI

Landsat visible and near-infrared bands were used for calculating the Normal Difference Vegetation Index (NDVI). The importance of estimating the NDVI is essential since the amount of vegetation present is an important factor and NDVI can be used to infer general vegetation condition [9]. The calculation of the NDVI is important because, afterward, the proportion of the vegetation (P
v) should be calculated, and they are highly related with the NDVI, and emissivity (ε) should be calculated, which is related to the P
v: (3)
NDVI
=
NIR
band
5
-
R
band
4
NIR
band
5
+
R
band
4
,where NIR represents the near-infrared band (Band 5) and R represents the red band (Band 4).


### 2.3.2. Calculating the Proportion of Vegetation

P
v is calculated according to (4). A method for calculating P
v [4] suggests using the NDVI values for vegetation and soil (N
D
V
I
v
=
0.5 and N
D
V
I
s
=
0.2) to apply in global conditions [10]: (4)
P
v
=
NDVI
-
NDVI
s
NDVI
v
-
NDVI
s
2
.However, since the NDVI values differ for every area, the value for vegetated surfaces, 0.5, may be too low. Global values from NDVI can be calculated from at-surface reflectivities, but it would not be possible to establish global values in the case of an NDVI computed from TOA reflectivities, since N
D
V
I
v and N
D
V
I
s will depend on the atmospheric conditions [11].


### 2.3.3. Calculating Land Surface Emissivity

The land surface emissivity (LSE (ε)) must be known in order to estimate LST, since the LSE is a proportionality factor that scales blackbody radiance (Planck’s law) to predict emitted radiance, and it is the efficiency of transmitting thermal energy across the surface into the atmosphere [12]. The determination of the ground emissivity is calculated conditionally as suggested in [10]:(5)
ε
λ
=
ε
v
λ
P
v
+
ε
s
λ
1
-
P
v
+
C
λ
,where ε
vand ε
s are the vegetation and soil emissivities, respectively, and C represents the surface roughness (C = 0 for homogenous and flat surfaces) taken as a constant value of 0.005 [13]. The condition can be represented with the following formula and the emissivity constant values shown in Table 1 [4]:(6)
ε
λ
=
ε
s
λ
,
NDVI
<
NDVI
s
,
ε
v
λ
P
v
+
ε
s
λ
1
-
P
v
+
C
,
NDVI
s
≤
NDVI
≤
NDVI
v
,
ε
s
λ
+
C
,
NDVI
>
NDVI
v
.When the NDVI is less than 0, it is classified as water, and the emissivity value of 0.991 is assigned. For NDVI values between 0 and 0.2, it is considered that the land is covered with soil, and the emissivity value of 0.996 is assigned. Values between 0.2 and 0.5 are considered mixtures of soil and vegetation cover and (6) is applied to retrieve the emissivity. In the last case, when the NDVI value is greater than 0.5, it is considered to be covered with vegetation, and the value of 0.973 is assigned.The last step of retrieving the LST or the emissivity-corrected land surface temperatureT
s is computed as follows [14]: (7)
T
s
=
BT
1
+
λ
BT
/
ρ
ln
⁡
ε
λ
,where T
s is the LST in Celsius (°C, (2)), BT is at-sensor BT (°C), λ is the wavelength of emitted radiance (for which the peak response and the average of the limiting wavelength (λ
=
10.895) [15] will be used), ε
λ is the emissivity calculated in (6), and(8)
ρ
=
h
c
σ
=
1.438
×
10
-
2
m
K
,where σ is the Boltzmann constant (1.38 × 10−23 J/K),  h is Planck’s constant (6.626 × 10−34 J s), and c is the velocity of light (2.998 × 108 m/s) [9].


## 2.3.1. Calculating NDVI

Landsat visible and near-infrared bands were used for calculating the Normal Difference Vegetation Index (NDVI). The importance of estimating the NDVI is essential since the amount of vegetation present is an important factor and NDVI can be used to infer general vegetation condition [9]. The calculation of the NDVI is important because, afterward, the proportion of the vegetation (P
v) should be calculated, and they are highly related with the NDVI, and emissivity (ε) should be calculated, which is related to the P
v: (3)
NDVI
=
NIR
band
5
-
R
band
4
NIR
band
5
+
R
band
4
,where NIR represents the near-infrared band (Band 5) and R represents the red band (Band 4).


## 2.3.2. Calculating the Proportion of Vegetation

P
v is calculated according to (4). A method for calculating P
v [4] suggests using the NDVI values for vegetation and soil (N
D
V
I
v
=
0.5 and N
D
V
I
s
=
0.2) to apply in global conditions [10]: (4)
P
v
=
NDVI
-
NDVI
s
NDVI
v
-
NDVI
s
2
.However, since the NDVI values differ for every area, the value for vegetated surfaces, 0.5, may be too low. Global values from NDVI can be calculated from at-surface reflectivities, but it would not be possible to establish global values in the case of an NDVI computed from TOA reflectivities, since N
D
V
I
v and N
D
V
I
s will depend on the atmospheric conditions [11].


## 2.3.3. Calculating Land Surface Emissivity

The land surface emissivity (LSE (ε)) must be known in order to estimate LST, since the LSE is a proportionality factor that scales blackbody radiance (Planck’s law) to predict emitted radiance, and it is the efficiency of transmitting thermal energy across the surface into the atmosphere [12]. The determination of the ground emissivity is calculated conditionally as suggested in [10]:(5)
ε
λ
=
ε
v
λ
P
v
+
ε
s
λ
1
-
P
v
+
C
λ
,where ε
vand ε
s are the vegetation and soil emissivities, respectively, and C represents the surface roughness (C = 0 for homogenous and flat surfaces) taken as a constant value of 0.005 [13]. The condition can be represented with the following formula and the emissivity constant values shown in Table 1 [4]:(6)
ε
λ
=
ε
s
λ
,
NDVI
<
NDVI
s
,
ε
v
λ
P
v
+
ε
s
λ
1
-
P
v
+
C
,
NDVI
s
≤
NDVI
≤
NDVI
v
,
ε
s
λ
+
C
,
NDVI
>
NDVI
v
.When the NDVI is less than 0, it is classified as water, and the emissivity value of 0.991 is assigned. For NDVI values between 0 and 0.2, it is considered that the land is covered with soil, and the emissivity value of 0.996 is assigned. Values between 0.2 and 0.5 are considered mixtures of soil and vegetation cover and (6) is applied to retrieve the emissivity. In the last case, when the NDVI value is greater than 0.5, it is considered to be covered with vegetation, and the value of 0.973 is assigned.The last step of retrieving the LST or the emissivity-corrected land surface temperatureT
s is computed as follows [14]: (7)
T
s
=
BT
1
+
λ
BT
/
ρ
ln
⁡
ε
λ
,where T
s is the LST in Celsius (°C, (2)), BT is at-sensor BT (°C), λ is the wavelength of emitted radiance (for which the peak response and the average of the limiting wavelength (λ
=
10.895) [15] will be used), ε
λ is the emissivity calculated in (6), and(8)
ρ
=
h
c
σ
=
1.438
×
10
-
2
m
K
,where σ is the Boltzmann constant (1.38 × 10−23 J/K),  h is Planck’s constant (6.626 × 10−34 J s), and c is the velocity of light (2.998 × 108 m/s) [9].


## 3. LST Validation

The two major LST validation models are through ground measurements or near-surface air temperature [16, 17]. The LST results comparing with the ground measurements results may have an error up to 5°C; in the case of Srivastava et al., the accuracy of the results in some area showed difference of ±2°C with actual ground temperature measurements. According to Liu and Zhang, another method using the mean near-surface air temperature to verify the retrieved LST results showed that the LST retrieving error is about 0.7°C. For the validation, six representative points have been used.For the validation of the final retrieved LST results in the presented tool, the mean near-surface air temperature was used [18] but with bigger amount of data and taking not only the mean temperature but also the actual temperature in the given pixel at the moment of the satellite passing over the area for 27 representative points.The comparison was made with air temperature, which is different and can sometimes result in big differences since the resolution of LANDSAT 8 for the used bands is 100 m for the thermal band and 30 m for the red and NIR bands. The LST was calculated and taken for the pixel in which the meteorological station fell. Sometimes, the differences can be very big depending on the weather condition and other factors [19]. It should also be taken into consideration that there is 1.1 to 2 meters’ difference between the LST and the air temperature, which means that differences in the temperatures are normal and expected.


### 3.1. Application of the Algorithm to Ontario and Quebec, Canada

Hourly data were collected from the Canadian Weather and Meteorology website (http://climate.weather.gc.ca/) and used for comparison with the retrieved LST for which, according to the available data, satellite images were downloaded for 02/05/2015 (Toronto area) and 04/06/2015 (Moncton area) for the areas shown in Figure 2.Figure 2
Application of algorithm in Ontario and Quebec, Canada. (a) Geographic location of Ontario in Canada; (b) frames of satellite images of study areas; (c) first case located between Toronto and Huntsville; (d) second case located in surrounding area of the city of Moncton.The study area was the Canadian provinces of Ontario and Quebec (Figure2). One satellite image was downloaded from each of the two provinces. These areas were chosen because of their specifications. That is, both study areas included water, urban areas, and green areas.


### 3.2. Comparison of LST Validation Results

To compare the results, two different satellite images from two different dates in two different areas were chosen according to the available data. After downloading the satellite images fromhttp://earthexplorer.usgs.gov/, LSTs were retrieved in ERDAS using the algorithm presented in this paper. In the first case, the satellite image was located between Toronto and the city of Huntsville near Lake Simcoe in Ontario, Canada. For this area, 20 meteorological stations were found, but only 16 of them were used for the accuracy assessment because of the presence of clouds or other unwanted events. The differences between the retrieved LSTs and the air temperatures and details on the stations are presented in Table 2 and Figure 3.Table 2
Emissivity of representative terrestrial materials for LANDSAT 8 TIRS Band 10.
Terrestrial material
Water
Building
Soil
Vegetation
Emissivity
0.991
0.962
0.966
0.973Figure 3
Retrieved LST image and meteorological stations from first study area used in accuracy assessment.In the second case, the study area was located in the area surrounding the city of Moncton and included part of New Brunswick, Prince Edward Island, and Nova Scotia in Canada. For this area, we found 11 meteorological stations, and all of them were used for the accuracy assessment. The details are presented in Table3 and Figure 4.Table 3
Details and differences of station from first study case.
ST name
Data 12pm
LST
Difference
Latitude
Longitude
H
Barrie-Oro
19.9
20.9
−1.0
44°29′00.000′′
79°33′00.000′′
289.00 m
Pa Hardwood Mountain Bike Park
19.2
24.9
−5.7
44°31′08.900′′
79°35′24.200′′
334.50 m
Borden Awos
20.0
20.7
−0.7
44°16′20.000′′
79°54′42.000′′
222.50 m
Pa Udora Strong
19.8
22.3
−2.5
44°15′03.600′′
79°12′18.300′′
266.50 m
Lagoon City
10.7
9.2
1.5
44°32′50.000′′
79°13′00.000′′
220.70 m
Collingwood
13.8
18.7
−4.9
44°30′00.000′′
80°13′00.000′′
179.80 m
Mono Centre
19.1
18.4
0.7
44°01′56.100′′
80°01′28.010′′
436.00 m
Uxbridge West
19.4
22.3
−2.9
44°05′54.000′′
79°09′49.020′′
325.00 m
Pa Uxbridge Taris
19.7
23.2
−3.5
44°03′16.000′′
79°06′55.000′′
359.50 m
Pa Atmos Vaughan
20.9
17.9
3.1
43°51′47.700′′
79°32′28.900′′
254.00 m
Pa Angus Glen Golf Club
20.4
23.3
−2.9
43°54′29.800′′
79°19′23.400′′
230.50 m
Toronto Buttonville A
21.2
23.3
−2.1
43°51′44.000′′
79°22′12.000′′
198.10 m
Pa Claremont Silo Farm
19.8
21.8
−2.0
43°59′37.900′′
79°05′43.900′′
263.50 m
Pa Markham North Toyota
21.6
27.4
−5.8
43°49′01.000′′
79°20′33.810′′
187.50 m
Pa Atmos Claremont
21.5
23.5
−2.0
43°56′09.800′′
79°05′05.400′′
167.00 m
Pa Atmos Erin
19.8
21.6
−1.8
43°49′33.620′′
80°07′12.840′′
470.00 mFigure 4
Retrieved LST image and meteorological stations from second study area used in accuracy assessment.


## 3.1. Application of the Algorithm to Ontario and Quebec, Canada

Hourly data were collected from the Canadian Weather and Meteorology website (http://climate.weather.gc.ca/) and used for comparison with the retrieved LST for which, according to the available data, satellite images were downloaded for 02/05/2015 (Toronto area) and 04/06/2015 (Moncton area) for the areas shown in Figure 2.Figure 2
Application of algorithm in Ontario and Quebec, Canada. (a) Geographic location of Ontario in Canada; (b) frames of satellite images of study areas; (c) first case located between Toronto and Huntsville; (d) second case located in surrounding area of the city of Moncton.The study area was the Canadian provinces of Ontario and Quebec (Figure2). One satellite image was downloaded from each of the two provinces. These areas were chosen because of their specifications. That is, both study areas included water, urban areas, and green areas.


## 3.2. Comparison of LST Validation Results

To compare the results, two different satellite images from two different dates in two different areas were chosen according to the available data. After downloading the satellite images fromhttp://earthexplorer.usgs.gov/, LSTs were retrieved in ERDAS using the algorithm presented in this paper. In the first case, the satellite image was located between Toronto and the city of Huntsville near Lake Simcoe in Ontario, Canada. For this area, 20 meteorological stations were found, but only 16 of them were used for the accuracy assessment because of the presence of clouds or other unwanted events. The differences between the retrieved LSTs and the air temperatures and details on the stations are presented in Table 2 and Figure 3.Table 2
Emissivity of representative terrestrial materials for LANDSAT 8 TIRS Band 10.
Terrestrial material
Water
Building
Soil
Vegetation
Emissivity
0.991
0.962
0.966
0.973Figure 3
Retrieved LST image and meteorological stations from first study area used in accuracy assessment.In the second case, the study area was located in the area surrounding the city of Moncton and included part of New Brunswick, Prince Edward Island, and Nova Scotia in Canada. For this area, we found 11 meteorological stations, and all of them were used for the accuracy assessment. The details are presented in Table3 and Figure 4.Table 3
Details and differences of station from first study case.
ST name
Data 12pm
LST
Difference
Latitude
Longitude
H
Barrie-Oro
19.9
20.9
−1.0
44°29′00.000′′
79°33′00.000′′
289.00 m
Pa Hardwood Mountain Bike Park
19.2
24.9
−5.7
44°31′08.900′′
79°35′24.200′′
334.50 m
Borden Awos
20.0
20.7
−0.7
44°16′20.000′′
79°54′42.000′′
222.50 m
Pa Udora Strong
19.8
22.3
−2.5
44°15′03.600′′
79°12′18.300′′
266.50 m
Lagoon City
10.7
9.2
1.5
44°32′50.000′′
79°13′00.000′′
220.70 m
Collingwood
13.8
18.7
−4.9
44°30′00.000′′
80°13′00.000′′
179.80 m
Mono Centre
19.1
18.4
0.7
44°01′56.100′′
80°01′28.010′′
436.00 m
Uxbridge West
19.4
22.3
−2.9
44°05′54.000′′
79°09′49.020′′
325.00 m
Pa Uxbridge Taris
19.7
23.2
−3.5
44°03′16.000′′
79°06′55.000′′
359.50 m
Pa Atmos Vaughan
20.9
17.9
3.1
43°51′47.700′′
79°32′28.900′′
254.00 m
Pa Angus Glen Golf Club
20.4
23.3
−2.9
43°54′29.800′′
79°19′23.400′′
230.50 m
Toronto Buttonville A
21.2
23.3
−2.1
43°51′44.000′′
79°22′12.000′′
198.10 m
Pa Claremont Silo Farm
19.8
21.8
−2.0
43°59′37.900′′
79°05′43.900′′
263.50 m
Pa Markham North Toyota
21.6
27.4
−5.8
43°49′01.000′′
79°20′33.810′′
187.50 m
Pa Atmos Claremont
21.5
23.5
−2.0
43°56′09.800′′
79°05′05.400′′
167.00 m
Pa Atmos Erin
19.8
21.6
−1.8
43°49′33.620′′
80°07′12.840′′
470.00 mFigure 4
Retrieved LST image and meteorological stations from second study area used in accuracy assessment.


## 4. Conclusion

This paper presented a new LST software tool and its algorithm created in ERDAS for calculating the LST from LANDSAT 8 TIRS. The algorithm was derived using the observed thermal radiance of the TIRS Band 10 of LANDSAT 8 TIRS. To verify the final retrieved LST results, the near-surface air temperature method was used. From the analysis of the two areas in Canada from two different dates, the standard deviation calculated for the first case based on 16 meteorological stations was 2.4°C, and that for the second case based on 11 stations was 2.7°C. It should be mentioned that sometimes, the difference between the near-surface temperature and the LST can be drastic since we are comparing two different temperatures in different places (ground temperature and 1.1 to 2.0 m off the ground). It should also be taken into consideration that the resolution of the LANDSAT 8 TIRS data is 100 m for the thermal band and 30 m for the red and NIR bands. Values smaller than −5°C in the two cases were considered to be clouds or other unwanted events on the satellite images since the data were from springtime; it was not expected. From Tables3 and 4 and Figures 3 and 4, it can be concluded that, for the first case, the smallest difference between the LST retrieved from the presented tool and the near-air temperature was 0.7°C and the biggest was 5.8°C. In the second study case, the smallest difference was 0.2°C and the biggest was 7.8°C.Table 4
Details and differences of station from second study case.
ST name
Data 11pm
LST
Difference
Latitude
Longitude
H
Mechanic Settlement
8.4
8.6
−0.2
45°41′37.040′′
65°09′54.040′′
403.00 m
Moncton Intl A
15.3
14.3
1.0
46°06′44.000′′
64°40′43.000′′
70.70 m
Fundy Park (Alma) Cs
12.4
10.2
2.2
45°36′00.000′′
64°57′00.000′′
42.70 m
Buctouche Cda Cs
15.1
14.9
0.2
46°25′49.006′′
64°46′05.009′′
35.90 m
Nappan Auto
15.4
13.3
2.1
45°45′34.400′′
64°14′29.200′′
19.80 m
Doaktown Auto Rcs
15.9
11.5
4.4
46°35′06.090′′
66°00′35.071′′
43.00 m
Saint John A
15.1
12.5
2.6
45°18′58.000′′
65°53′24.000′′
108.80 m
Parrsboro
15.9
8.1
7.8
45°24′48.000′′
64°20′49.000′′
30.90 m
Gagetown A
15.0
10.2
4.8
45°50′00.000′′
66°26′00.000′′
50.60 m
Gagetown Awos A
16.3
18.6
−2.3
45°50′20.000′′
66°26′59.000′′
/
Summerside
13.9
11.7
2.2
46°26′28.000′′
63°50′17.000′′
12.20 mThe tool can be significant since it is opening an opportunity to many researchers to get to the LST values easy and they can apply them in a number of researchs. The tool presented in this paper produced quite good results considering that the accuracy assessment was made with near-air temperatures and it can be used for different types of research. For future studies, the tool should be refined within situ measurements of LST.



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*Source: 1480307-2016-02-29.xml*