1. Yrd. Doç. Dr. Ali DENİZ
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

2. What is remote sensing?
Remote sensing is defined as the way to infer about the objects from distance i.e size, consentration, content etc.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

3. The interaction of electromagnatic waves with the objects
modifies the incident wave;
The resulting sinature depands on the composition and structure of the medium;
The principle of measurements of the Atmospheric parameters i.e. temperature and humidity is the interpretation of measured radiation in the specific spectral intervals which are sensitive to the constituent;
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

4. In the infrared and microwave regions of the spectrum
atmospheric constituents absorbs the radiation; then emit
According to Kirckhoff’s law;
Since the emitted radiance is a function of distribution of
objects, measurements of radiance gives information about
them.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

5. Absorption and Transmission of Monochromatic (spectral) Radiation:
The amount of energy, radiance, crossing a differencial area dA
in a time integral dt and wavenumber v is given as:
(...)
L= dE / Cos dA dt d d
its unit is W/m2 sr cm-1
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

6. is a solid angle and is defined as:
(...) d d
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

7. Absorption: L Incident beam Figure-.. Absorption through a Medium
Attenuated exit beam
Absorbing medium X L dx
Incident beam
Figure-.. Absorption through a Medium
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

8. When a monochromatic radition in Figure- whose radiance is L
peneterates into absorbing medium (non scatering) the fractional decrease is:
d L/ L = -k  dx
(...)
Where  is the density of medium, k is the spectral absoption
Coefficient.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

9. When integrating equation ... between 0 and x, becomes:
(...)
Where L(0) is the radiance entering the medium at x=0,
is called optical depth. And
is called transmittance.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

10. Blackbody radiation field is characterised as:
Isotropic and nonpolarized;
Independent of shape of cavity;
Depends on only temperature (T).
In a perfect blackbody emisivity is equal to unity due to
thermodynamic equilibirium.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

11. The ratio of emitted radiance by an object to the radiance
emitted by a blackbody at the same temperature is called
emisivity ().
Blackbody radiation E
 = 1 for blackbody.
 < 1 for greybody.
Greybody radiation 
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

12. To explain the spectral distribution of radiance emitted
Planck Law:
To explain the spectral distribution of radiance emitted
by solid bodies, Planck found that the radiance per unit frequency
emitted by a blackbody at temperature (T) is given as:
Planck function
Where h is Planck const,
k is Boltzmann const.
(...)
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

13. Figure-... Spectral Radiance of Blackbody
Kelvin
Figure-... Spectral Radiance of Blackbody
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

14. It gives the total radiation of a cavity (blackbody) not spectral
Stefan Boltzmann Law:
It gives the total radiation of a cavity (blackbody) not spectral
distribution of radiation. When Planck function (...) is
integrated 0(zero) to infinity (), S-B is given as:
E(Exitance)=E4
Where  is stefan Boltzmann constant.
(...)
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

15. When Planck equation is differentiated w.r.t wavenumber
Wien Law:
When Planck equation is differentiated w.r.t wavenumber
() or wavelength () and equated to 0(zero), one can find
max for a given temperature (T) called Wien Law.
What wavelengthg
gives maximum energy E
max =0.2897/T (cm) 
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

16. On the other hand eath’s atmospheric temperature is about 255
The radiative temperature of the sun surface is about 5780 K. After applying Wien law, maximum Planck radiance is obtained at the wavelength (max ) of m which is the center of the visible region of te spectrum.
On the other hand eath’s atmospheric temperature is about 255
K. Maximun emitted energy takes place around 11 m which is
infrared region (Figure...).
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

17. Brightness Temperature (or equivalent blackbody temperature) is the temperature estimated by inverting
Planck function.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

18. In the atmosphere, the absorption of radiation is mostly due to gases.
Gaseous Absorption:
In the atmosphere, the absorption of radiation is
mostly due to gases.
Major interest for the transfer of radiant energy is the value
of absorption coefficient (spectroscopy).
Total energy of a molecule consists of rotation, vibration,
electronic, and translation.
E=Erot+Evib+Eelc+Etrans
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

19. Absorption or emmision occurs when molecule changes
from energy level E1 to E2 with a frequency f = (E1- E2 ) / h.
Where h is a planck constant.
Significance in the spectrum:
rotational energy in the microwave and far IR regions;
vibrational energy in the near IR region;
electronic as well as vibrational and rotational energy
in the visible and UV regions.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

20. In order to posses rotational energy (interact with
the elecrtromagnatic field), molecules shall have dipole
moment.
Atmospheric such gases important for satellite
meteorology as CO, N2O, H2O and O3 have dipole moments
while N2, O2 , CO2 and CH4 do not.
However, as CO2, and CH4 vibrate electrical dipole moment
is produced and so rotational interaction take place. Therefore,
vibration-rotation interaction takes place with the incident wave.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

21. O-C-O O-C-O O-C O =7.46 m =14.98 m =4.26 m
No static and dynamic electric dipole
So no interection with the incident radiation
So no absoption (Figure-...).
(Wavelength
of vibration)
Symetric Stretching
Dipole occurs due to bending
Vibration (vibration-rotation) so
Absoption takes place (Figure-...).
O-C-O
=14.98 m
Bending
O-C O
=4.26 m
Asymetric Stretching
Figure-... Vibration modes of CO2
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

22. Temperature Sounding and measurements of some trace gases
in the atmosphere are based on vibrational transition. For example;
The 15 m and 4.3m of CO2 bands are used for temperature
soundings.
The 6.3 m H2O band is used for water vopour.
The 9.6 m O3 band is used for the total ozone measurements.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

23. Figure-... IR transmittance of several gases in the atmosphere (after Kidder,S.Q)
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

24. Radiation scattered from a particle depends on: Size; Shape;
Scattering:
Radiation scattered from a particle depends on:
Size;
Shape;
Index of refraction;
Wavelength of radiation;
View geometry.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

25. Fundemental two types of scattering are Mie and Rayleight.
For Rayleight scattering,  >> 
For Mie scattering,  ≈ 
Where  is particle size.
Scattering properties of such aerosols as smoke, dust, haze
in the visible part of the spectrum and of cloud droplets
in the IR region can be explanined by Mie scattering, while
of air molecules in the visible part can be explained by Rayleight
Scattering (Figure-...).
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

26. Figure-... Scattering Properites of atmospferic Contitiuens (after Kidder, S.Q).
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

27. Scattering phase function determines the direction in which
the radiation is scattered. As the size parameter (x=2πr/) inreases,
more scattering takes place in the forward direction (Figure-...).
Figure-...Scattering phase function of water droplets (after Kidder, S.Q).
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

28. Radiative Transfer Equation (RTE):
Consider a volume of gas (Figure-...) where absorption
and emission takes place but no scattering, energy transfer
equation can be written as:
(...)
Where first therm on the right hand side is abrorption within dx
and second term is emission within dx.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

29. Applying Kirchhof law and some manpulation and integration
finally we get:
(...)
The first term on the right hand side is the radiance at the
Boundary multiplied by the transmitance from the boundary to a.
Second term is the contribution due to emission from the medium
in the direction of incident wave.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

30. Similar equation can be computed for the emitted radiance
in the atmospfere with  zenith angle as:
(...)
where
and
is called weighting function.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

31. Figure-... NOAA HIRS weighting functions.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

32. So equation (...) can be written in a more compact form as:
Radiance
at the TOA
Surface contribution
Atm layer cont. z
TOA
, B(T) dz τ
L(0)=εs,ν B(T)
surface
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

33. Previous RTE (Figure-...) is driven in cartesian coordinate system
Brain Storming!
Previous RTE (Figure-...) is driven in cartesian coordinate system
drive it in presure coordinate system in p by using hydrostatic
Equation.
Where q is mixing ratio and g is gravity.
Good luck...
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

34. Processes of Atmospheric Radiation:
transmitted
absorbed,
emitted and
scattered by
aerosols and
molecules
reflected
absorbed
&scattered
emitted
transmitted
transmitted
reflected
emitted
reflected
emitted
Land
transmitted
absorbed
absorbed
Ocean
Figure-... Process of Atmospheric Radiation
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

35. Sensors are the devices for detecting the photons. The critical
part of the sensors is the detectors which works based
on photoelectric effect. That is, There will be an emmision of
negative particles (electrons) when negatively charged plate is
subject to a beam of photons.
The electrons then can be made to follow,collected and counted
as signals.
The magnitude of electric current (number of photoelectrons
per unit volume is directly proportional to light intensity.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

36. Thus, the change of electric current can be used to measure
the change in the photons (number, intensity) which strikes the
plate during the given time interval.
Photon beam C
Negatively
Charged
Plate R C
Figure-... Shemetic view of a detector.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

37. Remote Sensor Types: passive Sensor types aktive non-imaging imaging
Microwave radiometer
Magnatic ensor
Gravimeter
Fourier spectrum
non-imaging
non-scaning
passive
Monochrom IR
imaging
Camera
TV camera
imaging
image plane scanning
Solid scanner
Sensor
types
scanning
Optical mechanical scan.
object plane scanning
Microwave radiometer
non-scaning
non-imaging
Microwave radiometer
Microwave altimeter
aktive
image plane scanning
Passive phased array radar
scanning
imaging
Real aperture radar
object plane scanning
Synthetic aperture radar
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

38. Passive sensors: Radiation comes from the external sources.
Active sensors: Radiation is generated within the sensor.
Non-imaging: Measured radiation received from all points in the sensed
target and integrated.
Imaging: Radiaiton is received from a specific points (pixels) in the target
end result is an image(picture).
Sensors which instantaneously measure radiation coming from entire scene
called framing systems e.g eye, camera; if the scene is sensed point by point
along successive lines over finite time called scanning systems.
The size of scene which is determined by the aperture and optics called field
of view (FOV).
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

39. Radiometer is the general term for any instrument which
quantitatively measures the EM radiation in some interval of
EM spectrum.
When the radiation is light from the narrow visible band,
the term photometer is used.
If the sensor includes such components as prism or difraction
grating which can break incoming radiation into discrete
wavelengths and despers them to detectors called spectrometer.
Spectroradiometer implies that dispersed radiation is in bands
(Δλ) rather than discrete wavelenght (); most space sensors are
of this type.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

40. Retrieval methods can be classified in three general categories:
Physical;
Statistical and;
Hybrid.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

41. To predict the obserable parameters from arbitrary model
parameters called forward problem; on the other hand,
invers problem is to infer the model from observed parameters,
Invers problems are “ill posed”; that is, the solution is not unique.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

42. Estimation of L(z) from known temperature profıle, T,
Example:
Estimation of L(z) from known temperature profıle, T,
is a forward problem, while estimation of T profile from
satellite measurement of L(z) is an invers problem.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

43. Temperature Sounding Retrieval:
Physical Retrieval:
It is based on itiration of RTE by using first guess NWP
profile until the desired solution is optained.
Statistical Retrievals:
The siplest is to make regression between radiosonde
sounding called training data and measured radiance.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

44. RTE can be written in the dicrete formas:
Hybrid Retrieval:
RTE can be written in the dicrete formas:
After putting surface contribution into
Summation and replacing Li by Ri.
in maxrix notation
Where W is a matrix containing discrete weighting function.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

45. Assuming linearity and introducing basis function
by matrix inversion;
b=A-1R
(...)
Which is an exact solution of RTE. However not a
satisfactory solution because it is ill conditioned;
smaller error in R results in larger errors in B.
Trying least square fit of
Σ(R-Σab)2
gives the solution as:
b=(AT.A)-1.AT.R
(...)
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

46. Which is better solution than equation (...), yet it can be
improved by applying other methods (e.g. minimum variance)
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

47. Atmospheric wind retrieval from the images is based on
cross correlation method of successive three images.
cc pick
center of search area
Wind wector VH+1/2
VH-1/2
cc pick
32x32 pixel H
96x96
96x96
Image 2
(target image)
Image 1 (H-1/2)
Image 3 (H+1/2)
First, cross-correlation matrix produced between target image and
Last image (H+1/2) to find the correlation peak .
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

48. The distance between the center of search and the cc peak
is the cloud tracking wind vector.
In order to eleminate the spurious (false) peak cc is estimated
between the target image and first image (H-1/2). If cc peaks are
not symetric, it is rejected. If not, wind speed is claculated as:
V=1/2 (VH-1/2 + VH+1/2 )
Wind direction is the vectorial sum of two winds:
VH-1/2 V
VH+1/2
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

49. Height assignment: After finding the most contributing cloud
cluster to cc peak, its top temperature is used to assign height to
V by means of NWP forecast temperature profile. CO2 slicing
method can also be used for height assignment gives better
solution.
Sea surface wind speed and direction are estimated by means
of scatterometer which works like a radar.
Tracking winds can also be retrieved from atmospheric
soundings data.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

50. Radiance measurements around 15m CO2 band ( e.g HIRS
CO2 Slicing:
Radiance measurements around 15m CO2 band ( e.g HIRS
sounder) allows to detect clouds at various level. In the center
of band, upper level clouds and at the wings lower level clouds
are detected (Figure …).
Cloud amont and level (top pressure) can be estimated by means
of RTE.
Effectively detects thin cirrus clouds which are missed by IR
window and VIS channels.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

51. Radiance from the partly cloudy regions are given by
L=Lcd+(1-)Lcl where  is a fractional cloud cover,
Lcd is radiance from clouds and Lcl is radiance from clear air.
The cloud radiance is given by Lcd=Lbcd+(1-)Lcl
where Lbcd is radiance from completely opaque cloud.
After expresing Lcl and Lbcd in the form of RTE and some algebric manipulation, it becomes:
(…)
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

52. Where  is called effective cloud amount. Lcl estimated from
known temp and moisture profiles and L is a satellite measurement
(e.g HIRS). Right hand side is calculated from known temp profile
and atmospheric transmitance profile.
Representing left hand side with, L, and right hand side, B,
and taking the ratio of two spectral channels which see the same
FOV (e.g 14.2m/14.0m or 14.2m/13.3m), it becomes:
(…)
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

53. The optimum cloud pressure is obtained when the absolute
differences of right hand side and left hand side is minimum.
Once the cloud height is determined, an effective cloud amount
can be estimated by using IR window channel.
Sat measurement.
(…)
Calculated from temp profile
Opaque cloud radiance.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

54. Objective cloud retrieval is carried out by using imaging
Clouds:
Objective cloud retrieval is carried out by using imaging
radiometers rather than sounders due to their high resolution.
Widely used cloud analysis techniques are:
Threshold:
Temperature thresh is set for the spectral channels such that
if pixel temp is colder, it is assigned as a cloudy pixel.
Level of the cloud is determined by comparing brightness
temp of pixel with a known temp sounding.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

55. It is based on the histogram analysis of pixels which
represent cloud types and surface. Various dimentional
histograms may be constructed.
Figure-… shows two Dimentional ( IR vs VIS) historam
analysis.High clouds are located on the cold region while middle
clouds are clustered at the center and sea pixels are clustered
warm (dark) region.
Histogram
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

56. Kernels of the classes are:
230
Cloud id VIS count IR Count
220
High clouds
Cirrus thin
Medium clouds
Low clouds
Warm land
Sea
200 IR
180
150
130
VIS
Figure_... Bi-dimentional histogram of IR vs VIS
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

57. For an area of pixels, standard deviations (SD) and mean
Pattern recognition:
For an area of pixels, standard deviations (SD) and mean
values are Calculated. Uniform scenes (cloudy or clear) tend
to have low standard deviation while partly cloudy scene tends
to have high standard deviation.
Estimated statistical values (SD and mean etc) compared with
the background information (e.g. Climatological) to classify
the scene (cloudy, land, sea).
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

58. For the scene classified as sea, after applying atmospheric
SST:
For the scene classified as sea, after applying atmospheric
correction, the radiance is converted to brightness temperature
by means of Planck function.
For NOAA, SST estimation is based on the reression
Between Brightness temperatures of the channels (11 m,
12 m and 3.7 m) ans SST.
For sea scene, in the daytime SST is:
(…)
SST=1.9346T (T11-T12)
Where T in K and SST in Celsius.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

59. At nightime SST is given by:
SST1 =1.0088T (T3.7-T11)
SST2 =1.0350T (T11-T12)
SST3 =1.0170T (T3.7-T12)
(…)
All three SST result must agree within 1K to be accepted.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

60. Split Window Technique:
Making of two measurements rather then one in the atm
window region (near 11 m ) called split window. The two
channel see the same absorbers but in different amount.
The aim of the split window is to correct atm attenuation (mostly
due to water vapour) to estimate better surface temperature.
The siplit window equation driven as follows: in the windows
region transmitance can be expressed as  = exp(-ku), using
talor expention, = 1-ku and d=-kdu then RTE becomes
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

61. Where B is mean atm radiance and u total atm absorbtion
(…)
Where B is mean atm radiance and u total atm absorbtion
path length due to water vapour.
After linearizing the RTE and using for two channels (e.g.
11 and 12 m ), we get
(…)
Where Ts is a surface skin temp corrected for water vapour,
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

62. k is absorption coefficient and T 1 and T 2 are brightness
temp for the windows channels.
In a similar manner atm precipitable water can be retrieved.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

63. Calibration is the process to obtain physical parameters
(e.g. Tempareture) from the radiometric measurements
(count)
On board Calibartion:
Hot and cold targets located in the spectrometer are sensed
to get relative radiomatric responses to estimate calibration slope.
Vicarious calibration:
The method of vicarious calibration by means of calculated
radiance allow absolute calibartion of radiometers.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

64. It works by comparing radiometric count to be calibrated
with corresponding alsolute radiance which is calculated from
actual atmospheric parameters (e.g. Temperature and humidity
profile).
Radiometric respons to the radiance can be linear or nonlinear.
In the case of linear response (e.g. METEOSAT) calibration
coefficient is calculated as:
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

65. The motion of the satellites around the earth is governed
Orbits:
The motion of the satellites around the earth is governed
by the Newton’s law of motion.
The attractive force is: r
satellite
earth
Satellite orbit
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

66. Where M is earth mass, m is satellite mass, and g is garvitational
Constant.The centrifugal force of the spacecraft’s motion in orbit
must balance the attraction force such that:
introducing period T=2r/v and substituting in the equation we get:
Ex: NOAA satellites are app 850 km above
the earth surface, inserting into equation
T=102 min.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

67. However, real satellite orbit is nerly elliptical due to
the external foreces(e.g. gravitational potential of earth, solar
pressure). Eliptical orbit is to be explained by Kepler’s law.
Six orbital elements are used to express the spacecraft position
given by:
Semimajor axis,a (km);
Eccentricity,e;
Inclination,i (degree);
Right ascensing of ascending node,  (degree);
Argument of perigee,  (degree);
And true anomaly, , degree.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

68. For the meteorological satellites, mainly two orbits are used: Z
spacecraft
Orbit plane 
apogee
earth
perigee Y a  i
Equator plane  X
Ascending node
Ascending node
For the meteorological satellites, mainly two orbits are used:
and sunsynchronous and geostationary.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003

69. Sunsynchronous orbit have high inclination angle (e.g
98.7 for NOAA sat), pass the equator at the same local time,
and located in the lower orbit (e.g km).
Geostationary orbit consides with the earth’s equatorial plane,
located nearly 36 km above the equator. Geostationary satellites
drift from the desired orbit so that periodic orbit manoeuvres are
needed in the east-west and north-south directions and vise versa.
WMO-RMTC-EUMETSAT Satellite Meteorology Course, Alanya, Turkey September 2003