K. H. Rao Consultant and Retired Scientist G and Group Director Ocean Sciences Group NRSC/ ISRO, Balanagar, Hyderabad

Remote Sensing Coastal and GIS K. H. Rao Consultant and Retired Scientist G and Group Director Ocean Sciences Group NRSC/ ISRO, Balanagar, Hyderabad

INTRODUCTION AVAILABILITY OF OPERATIONAL RESOURCES MONITORING SATELLITES LIKE LANDSAT, SPOT AND IRS SATELLITE SERIES, MONITORING OF COASTAL WATERS HAS BEEN UNDER TAKEN BY VARIOUS COUNTRIES ALL OVER THE WORLD. IN INDIA WITH THE AVAILABILITY OF LANDSAT DATA DURING EIGHTIES METHODOLOGIES HAS BEEN DEVELOPED FOR MONITORING OF : COASTAL WATERS WETLANDS MAPPING, SHORELINE CHANGES, MANGROVES MAPPING ETC.

CURRENTLY NUMBERS OF SENSORS OPERATING IN VARIOUS SPECTRAL BANDS WITHIN THE VISIBLE RANGE OF ELECTROMAGNETIC RADIATION ARE USED FOR COASTAL STUDIES. THESE SENSORS ARE HAVING DIFFERENT SPATIAL RESOLUTION WITH VARIABLE REPEATIVITY. A WIDE VARIETY OF REMOTELY SENSED IMAGERY ARE AVAILABLE FOR COASTAL STUDIES AND HABITAT MAPPING.

ONE OF THE MOST IMPORTANT QUESTIONS TO BE CONSIDER WHEN PLANNING FOR COASTAL STUDIES IS THE SENSOR AND DATA TO BE USED FOR MAPPING. REMOTE SENSING SENSORS DIVIDE THE EARTH S SURFACE INTO A GRID OF SAMPLING UNITS CALLED PIXELS, NAMED AS SPATIAL RESOLUTION OF A PARTICULAR SENSOR. THE SPATIAL RESOLUTION, TEMPORAL RESOLUTION AND SPECTRAL RESOLUTION ARE THE KEY SENSOR PARAMETERS REQUIRED FOR COASTAL STUDIES.

Spatial Resolution (m) Temporal Resolution (Days) Spatial and Temporal resolution requirements for Coastal studies.

SPATIAL AND TEMPORAL SAMPLING CHARACTERISTICS OF DIFFERENT SENSORS SPATIAL AND TEMPORAL SAMPLING CHARACTERISITICS OF DIFFERENT MEASUREMENT STRATEGIES IN CLOUD FREE CONDITIONS. LOWER BOUND DENOTES THE SAMPLING FREQUENCIES. THE UPPER SPATIAL BOUND DENOTES THE EXTENT OF SYNOPTIC VIEWING WHICH IS POSSIBLE... 4. 5. HIGH RESOLUTION SCANNING SENSOR IN POLAR ORBIT MEDIUM RESOLUTION SCANNING SENSOR IN POLAR ORBIT SCANNING RADIOMETER ON GEOSTATIONARY SATELLITE MEASUREMENTS FROM RESEARCH VESSEL (NO SYNOPTIC VIEW POSSIBLE, LINEAR TRANSECT ONLY) BUOYS

CURRENT SPACE ASSETS Communication Satellites 4 Operational INSAT-A, C, 4A, 4B, 4CR GSAT-6, 7, 8,,, 4, 5, 6 & 8 Earth Observation Satellites Four in Geostationary orbit INSAT-D, Kalpana, INSAT-A & INSAT-DR in Sun-synchronous orbit RESOURCESAT- /A; CARTOSAT-, CARTOSAT- series (4 Nos.) RISAT-, RISAT-, OCEANSAT-, MEGHA-TROPIQUES, SARAL SCATSAT- Navigation Satellites (NavIC) Full Constellation of 7 satellites realized Space Science MOM & ASTROSAT km < m

ISRO Current & Future Missions for Earth Observations YEAR... 4 5 6 7 8 9 4 5 6 7 8 9 4 5 6 7 8 9 8 9 KALPANA- (VHRR) G E O INSAT-A (VHRR, CCD) INSAT-D (IMAGER & SOUNDER) INSAT-DR (IMAGER & SOUNDER) INSAT-DS (IMAGER & SOUNDER) GISAT (MX-VNIR, HyS-VNIR, HyS-SWIR, MX-LWIR) Atmosphere & Ocean L E O Oceansat- (OCM, SCAT, ROSA) ISRO-CNES MT (MADRAS, SAPHIR, ScaRaB, ROSA) ISRO-CNES SARAL (ALTIKA, ARGOS) NEMO-AM (MADPI) SCATSAT- (Scatterometer) Oceansat- (OCM, LWIR, SCAT) ISRO-NASA NISAR Resourcesat-,A (LISS-/4, AWiFS) Land & Water RISAT- (C-SAR) Resourcesat-A (LISS-/4, AWiFS) Cartographic CARTOSAT- (Stereo PAN) CARTOSAT-S ( PAN, MSC) CARTOSAT- (PAN) CARTOSAT-E (PAN) CARTOSAT- (PAN) YEAR... 4 5 6 7 8 9 4 5 6 7 8 9 4 5 6 7

EO Missions - Near Future CARTOSAT- D & E VHR Panchromatic and Multispectral Imaging PAN (.6 m, km swath, bit) Mx (m, km swath, 4 Xs, bit) Orbit : 5 km Local time: 9 hrs CARTOSAT- VHR Panchromatic, Multispectral Imaging PAN (.5 m, 6 km swath, bit) Mx (m, 6 km swath, bit) Orbit : 45 km Local time: hrs RESOURCESAT- & A Continuity for Resourcesat-A ALISS-:m & m, 95 km, 5 Bands, ATCOR: 4m,.4- m,, bit) Orbit : 795 km Local time: hrs Oceansat- & A Continuity for OS- with Improvements band OCM, IR-SST Ku-band Scatterometer, Orbit : 7 km Local time: hrs RS SAMPLER- S & SA High Res. Stereo imaging GISAT - Geosynchronous Orbit HR Mx VNIR : 5m; SWIR:.5 Km HYSI VNIR: m; WIR : 9m Orbit : 6 km Every min RISAT-A Continuity for RISAT- C-Band SAR Orbit : 56 km Local time: 6 hrs NISAR Joint Mission with JPL/NASA PAN Fore & AFT APAN:.5m, 6Km Mx:.5m, 6Km, 4 Bands Orbit : 6 km Local time: hrs Payloads L & S Band SAR Orbit : 747 km Local time: 6 hrs

REMOTE SENSING DEFINITION: OBSERVING AN OBJECT FROM A DISTANCE WITHOUT HAVING DIRECT CONTACT WITH IT. REMOTE SENSING SYSTEMS ARE USED TO OBSERVE THE EARTH S SURFACE FROM DIFFERENT LEVELS OF PLATFORMS SUCH AS SATELLITES AND AIRCRAFT, AND MAKE IT POSSIBLE TO COLLECT AND ANALYZE INFORMATION ABOUT RESOURCES AND ENVIRONMENT OVER LARGE AREAS.

REMOTE SENSORS ARE GROUPED INTO TWO CATEGORIES: PASSIVE SENSOR SENSE NATURAL RADIATION EITHER EMITTED BY OR REFLECTED FROM THE EARTH S SURFACE. ACTIVE SENSOR SENSORS HAVE THEIR OWN SOURCE OF ELECTRO MAGNETIC RADIATION (EMR) FOR ILLUMINATING THE OBJECTS.

Spatial resolution A measure of the area or size of the smallest dimensions on the earth's surface over which an independent measurement can be made by the sensor. A small elemental area is observed at a time by a RS sensor by means of a suitable optical telescope or other electronic means and such a field of view of the sensor is called the Instantaneous Field of View (IFOV). Spectral resolution The spectral resolution of the remote sensor characterises the ability of the sensor to resolve the energy received in a given spectral bandwidth to characterise different constituents of earth surface. Thus the spectral resolution is defined by the spectral bandwidth of the filter and sensitiveness of detector.

Radiometric resolution In remote sensing the reflected radiation from different objects generate electrical signal (say voltage) as output from the detector which are converted into digital number. This is analogous to grey shades seen in a black and white photograph. The ability to distinguish the finer variations of the reflected or emitted. Temporal resolution This is another aspect which is specific to space-borne remote sensors. The polar orbiting satellites can be made to orbit in what is known as sun synchronous orbits. This means that the satellite crosses over the equator at the same local solar time in each orbit. Such an orbit offers similar sun illumination conditions for all observations taken over different geographical locations along a latitude (in the sun-lit area). By a suitable selection of the pacecraft altitude and the inclination angle of the orbit, the spacecraft can be made to cover the same area on the earth at regular intervals.

Remote sensing Sun, Earth, and Atmosphere The climate system on our planet is driven by the energy coming from the sun. The sunlight reaches the Earth through several atmospheric layers. The lowest one, from the Earth surface to about 7miles height, is called troposphere. Next layer, from 7 up to miles above the surface, is called stratosphere. Mesosphere and thermosphere follow above up to about 5 miles height. Thermosphere Mesosphere Stratosphere Troposphere

Earth Spectrum Solar spectrum Near IR short Visible Earth s spectrum In contrast, the Earth is colder celestial body with average surface temperature of 5oC. Far IR long Electromagnetic spectrum! X-rays in medicine Radio broadcasting So, remember: The Sun emits at short wavelengths (SW). The Earth emits at long wavelengths (LW). That is why Earth emits at longer wavelengths, called infrared (IR), visualized like this: 6 of 5

Solar energy at sea level Only a part of the SW solar radiation available at the top of the atmosphere reaches the Earth. Some of it is scattered, absorbed and reflected within the atmosphere by the gases, aerosols, and clouds. The absorbed radiation is re-emitted by the atmospheric constituents back as a LW radiation, i.e., it is converted in heat. 7 of 5

The attenuation of in coming Solar and out going earth radiation is depends upon atmospheric absorption and scattering. Scattering of EMR Within the atmosphere reduces the image contrast And changes are spectral signature of ground objects as seen by the sensor. Absorption spectrum of earth s atmosphere

% of Reflectance Wavelength (µm) A typical reflectance curve of green vegetation in the visible, near infrared and mid infrared region.

RELATIVE ABSORPTION / TRANSMITTANCE Spectral Absorption of common in water optical constituents, Mean Extraterrestrial Irradiance, and spectral transmittance of the atmospheric constituents, Oxygen and Water Vapour (IRS P4 OCM bands are highlighted) WAVELENGTH (NM). WATER VAPOUR MEAN EXTRATERRESTRIAL IRRADIANCE DIATOMS PHYCOERYTHRIN CHLOROPHYLL FLUORESCENCE OXYGEN CHLOROPHYTES GELBSTOFFS (YELLOW SUBSTANCE) WATER

Sun spectrum Recall: Each body with some temperature emits radiation. We feel the radiation emitted from our bodies as heat. This law applies to all objects in the Universe. Solar spectrum Near IR Far IR The sun is a celestial body with a temperature of 6 oc. Objects with such high temperature emit energy at the short wavelengths of the electromagnetic spectrum visualized as: Visible The Sun emission peaks in the visible range. 5 of 5

Under water light field Human eye sensitive: 4-7nm. EMR is in indivisible units: photons/quanta Speed of light x8 m/s( continuum of photons) In day light ( bright summer ) Sq meter of sea surface receives quanta/s of visible light Relation of = c/ c in meters, in meters, in cycles/s Energy : = hc / h = 6.6 x -4 Js

Photon of energy for a given wavelength = (988/ ) -9 J energy is in Watts or Js Radiation flux in ( ) in W conversion to quanta/s q/s= 5. x x x 5 For a given wavelength band conversion from quanta to W is difficult. for 4-7 nm (Q: W) or W to q/s is.77 x 8 q/s/w ( -5% accuracy ) (Morel & Smith 974 )

Refractive Index Light travels slowly in any media to vacuum Light velocity in media = light in vacuum/ Refractive index of medium RI of air =.8 ( assumed as ) RI of water =. ( natural water). Varies with T, S and C in water =. 5x 8 m/s. Frequency remains but diminishes in proportion to velocity

Properties of radiation field IAPSO defined the definitions Zenith angle( ): Angle between light beam to upward vertical Azimuth angle( ) = Angle between vertical plane incorporating the light beam to some other vertical plane ( to vertical plane of Sun ) Nadir angle: Angle between a given light beam to the downward vertical

Radiant flux : rate of flow of radiant energy in W ( J/s ) or in quanta/s Radiant Intensity: I flux per unit solid angle in specified direction. An infinitesimal cone in given direction / the element of a solid angle. I = d / d w in W or in (quanta/s) / steradian Radiance : L radiant flux per unit solid angle per unit Area of a plane Right angles to the direction of flow. Function of Direction ( zenith and Azimuth angles ) L (, ): = d / d A cos ( ) dw,

Irradiance : E = d / d A ( at point of source )W/m Downward irradiance &upwardirradiance( Ed&Eu)

Energy exchange processes in the natural environment (after Lillesand and Kiefer, 987)

Electromagnetic Spectrum (after curran, 988)

An Electromagnetic wave and its components (after Lillesand Kiefer, 987) Energy : = hc / h = 6.6 x -4 Js = c/ c in meters, in meters, in cycles/s

Stefan-Boltzmann Law All matters at temperatures above absolute zero (o K or - 7.6oC) continuously emit electromagnetic radiation. The total energy radiated by an object at particular temperature is given by Stefan- Boltzmann Law, which states that M T 4 where M is total radiant exitance from the surface of the material (Watts/m ); s is Stefan-Boltzmann constant, 5.6697x-8- W/m / ok4 ; T is absolute temperature in ok of the emitting material.

Wien's Displacement Law The dominant wavelength, or wavelength at which a blackbody radiation curve reaches a maximum, is related to its temperature by Wien's Displacement Law. m A T where m is wavelength ( m) corresponding to maximum spectral radiant exitance A is a constant with value of 898 m. ok; and T is temperature of the blackbody in ok.

Planck's Law The spectral radiant exitance M, i.e., the total energy radiated in all directions by unit area in unit time in a spectral band for a blackbody is given by Planck's law: M hc 5 e hc kt

Spectral distribution of energy radiated by black bodies of various temperatures (after Lillesand and Kiefer, 987)

INTERACTION OF EMR WITH EARTH SURFACE FEATURES THE REFLECTANCE FROM VEGETAION IS GOVERNED BY LAEF PIGMENT (Chlorophyll, Carotinoid etc.) LAEF CEL STRUCTURE LEAF MOISTURE CROWN ARCHITECTURE PLANT PHYSIOLOGY

Structure of plant leaf and (b) a typical reflectance curve of green vegetation in the visible, near infrared and mid infrared region (after Goetz et al, 98)

Spectral Response for (a) different canopies in visible and near IR (after Brooks, 97) (b) for corn leaves under various moisture content (after Hoffer and Johannsen, 969)

THE REFLECTANCE FROM SOIL IS GOVERNED BY SOIL IS FORMED BY DISINTEGRATION OF ROCKS THROUGH VARIOUS PROCESSES SAND, SILT & CLAY COMPOSITION SOIL MOISTURE SOIL TEXTURE, COLOUR, GRAIN SIZE MINARAL COMPOSITION SURFACE ROUGHNESS

Soil reflectance for (a) Clay soils for two moisture levels, (b) Sandy soils for three moisture levels (after Myers, 975), and (c) Soil with different composition

THE REFLECTANCE FROM ROCKS NATURE OF ROCK (IGNEOUS, SEDIMENTORY) TOP COVR (SOIL, VEGETATION, MIXED-RESPONSE) TOPOGRAPHY/ SHADOW SURFACE ROUGHNESS

Spectral reflectance characteristics of (a) fresh and weathered rocks (after Lyon, 97) and (b) Volconic and sedimentary rocks (after Goetz, 976)

THE REFLECTANCE FROM WATER DEPTH SUSPENDED PARTICLES IN WATER FLOATING VEGETATION, IF ANY SUN ANGLE

Effect of increasing phytoplankton concentrations (After Suits, 97 )

RELATIVE ABSORPTION / TRANSMITTANCE SPECTRAL SIGNATURES WAVELENGTH (NM). WATER VAPOUR MEAN EXTRATERRESTRIAL IRRADIANCE DIATOMS PHYCOERYTHRIN CHLOROPHYLL FLUORESCENCE OXYGEN CHLOROPHYTES GELBSTOFFS (YELLOW SUBSTANCE) WATER

Characteristics of present Ocean colour sensors Sensor OCM MODIS SeaWiFs MERIS Orbital Inclination 98. 98. 98. 98.5 Equatorial Crossing Time(h) : : : : Altitude(Km) 7 75 75 8 Resolution at Nadir(Km).6.../. Swath(Km) 4 8 5 Tilt(degree) No No Direct Link X-band X-band L-band X-band Recorded Yes X-band S-band X-band Solar Calibration Yes Yes Yes Yes Lunar Calibration No Yes Yes No Lamp Calibration No Yes No No

Differences between OCM and MODIS MODIS OCM Center ( nm) 4 FWHM (Band pass,nm) NE L Wm-sr-um-) Center ( nm) FWHM (Band pass,nm) NE L Wm-sr-um-) 4 5.48 44. 488.5 5.8 55.9.6 44. 49.7 5.7 555.5 667.8 67. 68.7 765 4.5 748.9 865 4.8 87 5.6 469*.45 555*.7 645** 5.7 858** 5. * Spatial resolution.5 Km ** Spatial resolution.5 Km

RETRIEVAL OF SEA SURFACE TEMPERATURE AND POTENTIAL FISHING ZONE MAP PREPARATION The idea of remote measurement of the surface temperatures of an object stems from Planck s law. The spectral radiance of a perfect emitter (Black body) at an absolute temperature T in the spectral band with wave number (cm-) is given by Planck s function, (,T), mw/m Sr cm-. (,T) = C /[exp(c /T) - ] Where C and C are known as Planck s radiation constants. C =.966 X -5 mw/(m Sr cm-) C =.488 Cm K. For a real object having emittance, the spectral radiance is given by (,T) *. Application of Planck s radiation for remote measurement of the Sea Surface Temperature(SST) using Air/Satellite borne Infra-Red (IR) detectors is well known today. SST, NRSA, HYDERABAD

The radiance received at the satellite sensor I( ) may be written as: I( ) = Ie( ) + Isc( ) + Ir( ) + Iem( ) Where Ie( )= Isc( )= Ir( )= Iem( )= Contribution due to emission from the surface the earth/oceans. Contribution due to Scattering process by the atmospheric constituents. Contribution due to reflection at the sea surface. Contribution due to emission from the atmospheric gases. In the thermal Infra-Red region, which is of interest to us, the Scattering effects can be ignored for clear atmospheric conditions because the wave length of the radiation (say - m) is much larger than the sizes of the molecules (. m) or the aerosol particles (.- m). Hence Isc( ) =. The contribution from the solar radiation reflected at the sea surface is about ten times smaller than the digitization error in the.5-.5 m window region. Therefore, for all practical purposes, the solar radiation reflected at the surface in the thermal channels can safely ignored (Ir( ) = ). Then the Equation cab written as: I( ) = Ie( ) + Iem( ) SST, NRSA, HYDERABAD

The NOAA-AVHRR data are being processed regularly at NRSA for the retrieval of Sea Surface Temperatures (SSTs). The processing steps are as follows:. Radiometric Calibration. SST computation for cloud free areas. Geometric corrections 4. Generation of Potential Fishing Zone (PFZ) maps 5. Computation of grid averages SST Computation: SSTs are computed for cloud free pixels using the following equation: SST(C) = a*tb4 + b*(tb4 - Tb5) + c*(tb4 - Tb5)*Sec( ) + d Where Tb4 and Tb5 are the brightness temperatures of AVHRR channels 4 and 5 respectively and is satellite zenith angle and is given below: I = Sin-[{(R + h)/r}*sin I ] R = Radius of the Earth (678.88 Km) h = Height of the satellite (8 Km) I = Look angle at ith pixel I = -55.4 + (55.4/4)*I SSTs are computed when satellite zenith angle is less than 5 degrees SST, NRSA, HYDERABAD

The regression coefficients a, b, c and d for different satellites are used as follows: Satellite a b c d NOAA-.9794.674.84-67.9 NOAA- (-4-9) NOAA-.455.45.64.9656.579.4598-6.6 NOAA-4.74.9588.77976-78.4-8.67 SST, NRSA, HYDERABAD

Ocean phenomena detectable readily from IR SST images Magnitude (OC) Length scale (km) Time scale SST distribution in ocean basins 5 - - Seasonal variation of the SST distribution with ocean basins - month- year Monthly SST map sequence Intra and inter annual variation of SST distribution (e.g.el Nino).5-5 5-5 Months-years Monthly sequence of SST anomalies Tropical monsoon events.5-5 - weeks-year Weekly sequence of SST maps Oceanic planetary (e.g.rossby) waves.- - Months-years Hovmuller plots of SST anomalies Tropical instability waves.5-5 - week-4months Hovmuller plots of SST anomalies Major ocean fronts.5-5 - month-years SST maps Western boundary currents -8 5- - SST maps Meanders and eddies on boundary and ocean currents -8 5- weeks- 6 months.5-5 -5 weeks SST map as series Major ocean upwelling regions -5 - weeks SST map series Deep convection cooling events.- - Days SST anomalies Major river plumes in the ocean.- 5- - Coral bleaching events.- - Days SST anomalies Diurnal warming events.5-5 5- -hr SST anomalies Local wind Mixing phenomena.- 5-5 hours SST map series Shelf edge mixing phenomena.- - Days SST map series Shelf sea tidal mixing fronts.5-5 - Days SST ma series Shelf sea circulation and mixing.-5-5 Days SST map series Regions of freshwater influence.- -5 Days SST map series Coastal wind induced phenomena.- - Hours SST ma series Phenomenon Oceanic mesoscale eddies Process required SST map weekly sequence of SST maps SST maps

CURRENT SPACEBORNE SENSORS FOR SST Satellite Sensor Resolution Accuracy NOAA METOP ENVISAT TRMM AVHRR AVHRR AATSR TMI VIRS MODIS km km km 5 kms kms km.5 K. K <.5 K.6 K.4 K <.5 K 58 & 6 km 4 km 8 km 5 km km 4 km <.6 K.7 K TERRA AQUA AQUA AMSR-E GOES INSAT-A/KALPANA METEOSAT MSG AVHRR INSAT-D Imager <.5 K <.5 K

Solar Radiation Spectrum & Absorption by Atmosphere

EM SPECTRUM & ABSORPTION LINES Solar and Terrestrial Radiances Absorption Lines

Contributions to the IR radiation received at the sensor c a b Isat = Ia + Ib + Ic a- Signal emitted by the sea surface b- Downward atmospheric emission, reflected at sea surface c Direct upward atmospheric emission

RADIATIVE TRANSFER RADIANCE RECEIVED BY AN EARTH-VIEWING RADIOMETER a c b I (, ) Isea(, ) Iatm(, ) Iatmr (, ) Isea (, ) ( ) (,, Z, ) B (, SST ) Iatm (, ) I (, z ) (, z,, ) dz = frequency = incidence angle = atm. absorption = surface emissivity = atm transmittance z= altitude Iatmr (, ) ( ( )) (,,, ) I (, z ) (,, z, ) dz z (, z, z, ) exp[ sec (, u ) du ] z

RADIATIVE TRANSFER (continued) RADIANCE EMITTED BY A THIN ATMOSPHERIC LAYER I (, z ) h B{, T ( z )} a (, z ) h B= Planck s Function t=atm layer temperature h= Planck s constant k= Boltzman s constant = channel response function, = channel freq limits B(,T)=h /[c(eh /kt-] Iatm (, ) B{, T ( z )} a (, z ) (, z,, ) dz INTEGRATED RADIANCE OVER CHANNEL BANDWIDTH Ii [ i i I (, ) ( )d ] /[ ( )d ] i i i i

PAN 8 LISS-IV LISS-III Spatial Resolution (m) 6 LISS-II 4 WIFS LISS-I 8 6 4 986 988 99 99 994 996 998 Year EVALUATION OF INDIAN REMOTE SENSING SATELLITE FOR COASTAL STUDIES

RADIATIVE TRANSFER (continued) RADIANCE EMITTED BY A THIN ATMOSPHERIC LAYER I (, z ) h B{, T ( z )} a (, z ) h B= Planck s Function t=atm layer temperature h= Planck s constant k= Boltzman s constant = channel response function, = channel freq limits B(,T)=h /[c(eh /kt-] Iatm (, ) B{, T ( z )} a (, z ) (, z,, ) dz INTEGRATED RADIANCE OVER CHANNEL BANDWIDTH Ii [ i i I (, ) ( )d ] /[ ( )d ] i i i i

REMOTE SENSING SATELLITES AND SENSORS

SATELLITE SENSORS NO. OF BANDS LANDSAT,, MSS 4.5.6.7.8 - LANDSAT 4, 5 TM 7.45.5.6.76.55.8.4.5.6.79.5 SPOT,, HRV PAN IRS - A LISS-I LISS-II 4 4 IRS - B IRS-C SPATIAL RESOLUTION SWATH LAUNCH DATE.6.7.8. 8 M 85 KM July 97 () Jan 975 () Mar 978 () -.5.59.69.9.75.5.5 M 85 KM July 98 (4) Marc 984 (5) -.59.68.89.7 M 7 KM Feb 986 () Jan 99 () M 7 KM Sept 99 () 7.5 M 6.5 M 48 KM X 74 KM Mar 988 B.45 -.5 B.5 -.59 M B.6 -.68 B4.77 -.86 LISS-III 4 IRS-D IRS-P WAVELENGTH (MM) PAN WiFS LISS-II 4 B.5 -.59 B.6 -.68 B4.77 -.86 B5.55 -.7.5 -.75 B.6 -.68 B4.77 -.86 B B B B4.45.5.6.77 -.5.59.68.86 Aug 99.5 M 4 KM Dec 995 Sept 997 5.8 M 88 M 7.5 KM 8 KM Steerable + 6.74 M (Across Track) 7.9 M (Along Track) KM Oct 994

SATELLITE SENSORS NO. OF BANDS IRS-P MOS-A MOS-B MOS-C WiFS IRS-P4 OCM 8 MSMR 4 ERS-, SAR IMAGE MODE JERS WAVELENGTH (MM) SPATIAL RESOLUTION 57 M 5 M 5 M 88 M SWATH 95 9 774 Km Km Km Km LAUNCH DATE Mar 996 4 KM 6th May 999 M KM July 99 () April 995 () L Band.75 GHz 8 M 75 KM Feb 99 C Band 5. GHz 5m x 8m 48 - m x 8 m - 5 m x 8 m - 9 m x 9 m KM 65 KM 5 KM 45 KM Sept 995 MSS 4 4. m KM Sept 999 PAN.45-.5.5-.6.6-.69.76-.9.45-.9.4-.4.4-.45.48-.5.5-.5.545-.565.66-.68.745-.785.845-.885 6.6,.65, 8,GHz 46x6m C Band 5. GHz SAR RADARSAT- SAR IKONOS,8,4, 4m. m

STATUS ON UTILIZATION OF REMOTE SENSING DATA FOR COASTAL STUDIES

STATUS ON UTILIZATION OF REMOTE SENSING DATA FOR COASTAL STUDIES. Resources/ Parameters /Processes Mangroves, Coral reefs, Salt pans, Aquaculture, Wetlands, Other Coastal Inland Resources Remote sensing compliances Mapping and Monitoring in different scales Fisheries Forecasting and Monitoring Minerals & Energy Exploring and Monitoring Coastal Geomorphology Mapping and and Shoreline changes Monitoring in different scales SST, Winds, Waves, Fishery forecasting, Water vapour content, Monsoons, Ocean Cloud liquid water etc. and Atmospheric studies Status Operational using High Resolution Multispectral sensors Data from IRS series Semi operational with NOAA and IRS--P4 IRS R & D stage with existing RS Data Operational High Resolution Data from IRS Series Operational with IRS--P4 and other IRS foreign satellites

STATUS ON UTILIZATION OF REMOTE SENSING DATA FOR COASTAL STUDIES. Resources/ Remote sensing Parameters /Processes compliances Upwelling, Eddies, Fishery and Gyres etc. Ocean Dynamics studies Coastal Regulation Mapping and Zone Monitoring in : 5, and : 5, scale Suspended Sediments Mapping and concentration Monitoring Oil Slicks Mapping and Monitoring Chlorophyll Concentration Currents and Surface Circulation Patterns Mapping and Monitoring Mapping and Monitoring Status Operational with IRSIRSP4 and other foreign satellites Operational using IRS IC & ID data Semi operation with IRS--P4 IRS Semi operational with IRS--series and other IRS foreign satellites Semi operation with IRS--P4 IRS Semi operational with IRS--series and other IRS foreign satellites

PERFORMANCE OF AIRCRAFT AND SATELLITE REMOTE SENSORS FOR COASTAL ZONE STUDIES Platform: AC = Aircraft (Medium & Low Altitude) SC = Spacecraft (Satellite) RATING: = = = = RELIABLE (OPERATIONAL) NEEDS ADDITIONAL FIELD TESTING LIMITED VALUE (FUTURE POTENTIAL) NOT APPLICABLE

PERFORMANCE OF AIRCRAFT AND SATELLITE REMOTE SENSORS FOR COASTAL ZONE STUDIES SENSORS Platforms Vegetation and Landuse Biomass & Veg. Stress Coastline Erosion FILM CAMERA AC SC MULTI SPECTRAL SCANNER AC SC THERMAL IR SCANNER AC SC LASER PROFILER AC SC LASER FLUOROSENSORS AC SC MICROWAVE RADIOMETERS AC SC IMAGING RADAR (SAR OR SLAR) AC SC RADAR ALTIMETER AC SC AC SC RADAR SCATTEROMETER

PERFORMANCE OF AIRCRAFT AND SATELLITE REMOTE SENSORS FOR COASTAL ZONE STUDIES SENSORS Platforms Coastal Geomorphology Depth Profiles Suspend Sediment Profiles Suspend Sediment Concentration FILM CAMERA AC SC MULTI SPECTRAL SCANNER AC SC THERMAL IR SCANNER AC SC LASER PROFILER AC SC LASER FLUOROSENSORS AC SC MICROWAVE RADIOMETERS AC SC + + + + IMAGING RADAR (SAR OR SLAR) AC SC RADAR ALTIMETER AC SC + + + + AC SC RADAR SCATTEROMETER

PERFORMANCE OF AIRCRAFT AND SATELLITE REMOTE SENSORS FOR COASTAL ZONE STUDIES SENSORS Platforms Chlorophyll Concentration Oil Slicks SST Water Salinity Current Circulation Pattern FILM CAMERA AC SC MULTI SPECTRAL SCANNER AC + SC + THERMAL IR SCANNER AC SC LASER PROFILER AC SC LASER FLUOROSENSORS AC - SC MICROWAVE RADIOMETERS AC SC IMAGING RADAR (SAR OR SLAR) AC SC RADAR ALTIMETER AC SC AC SC RADAR SCATTEROMETER

PERFORMANCE OF AIRCRAFT AND SATELLITE REMOTE SENSORS FOR COASTAL ZONE STUDIES SENSORS Platforms Wave Spectra Sea State Surface Winds FILM CAMERA AC SC MULTI SPECTRAL SCANNER AC SC THERMAL IR SCANNER AC SC LASER PROFILER AC SC LASER FLUOROSENSORS AC SC MICROWAVE RADIOMETERS AC SC IMAGING RADAR (SAR OR SLAR) AC SC RADAR ALTIMETER AC SC AC SC RADAR SCATTEROMETER

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PHYTOPLANKTON FLUORESCENCE

Fluorescence spectral signature.6.4 Chlorophyll absorption. Lu/Es..8 Increase in fluorescence.6.4. 4 45 5 55 Wavelength, nm 6 65 7