Processing RADS Data - Google Sites

Processing RADS Data 

LAXMIKANT DHAGE

COAS OREGON STATE UNIVERSITY

 

 

 

1

Declaration I hereby declare that the work incorporated in this project is original and carried out at the College of Oceanic and Atmospheric Sciences, Oregon State University.

LAXMIKANT DHAGE B Tech 6th Semester Department of Mechanical Engineering Indian Institute of Technology, Guwahati.

 

2

Certificate

This is to certify that this project is an authentic record of the research carried out by Mr. Laxmikant Dhage under my supervision and guidance at COAS, OSU.

COAS, OSU. 22 July 2010

 

Dr. Ted Strub Professor 104 COAS Admin Bldg College of Oceanic & Atmos. Sciences Oregon State University

3

Table of Contents     

Declaration Certificate Acknowledgements Summary of work 1.

Introduction

2. Methods 3. Results and Figures 4. References

 

4

Acknowledgements

It is my pleasure and privilege to express my deep gratitude to Prof. P. Ted Strub for giving me the opportunity to carry out the project under his guidance. I owe much to Dr. Corinne James, Research Associate for helping me throughout the period of this project. Lastly, I thank my parents, and family members for their moral support and constant encouragement, without which the work carried, would not have been possible.

LAXMIKANT DHAGE B Tech 6th semester Department of Mechanical Engineering IIT Guwahati.

 

5

Summary of Work Our main emphasis was on creating a precise processing strategy on RADS database and obtain smooth Sea Level Anomaly field. Methodology involves editing of each and every corrective field with some specific sequential steps. We looked carefully into each and every data field involved in the construction of Sea Level Anomaly. These steps involve applying respective limits, removing outliers and smoothing with weighted moving average. Finally smooth SLA is interpolated into standard grid points. We removed the spatial and time series average from the gridded SLA data so that deviation from mean can be observed clearly. We started our work with pass 28 off Oregon coast and then implemented similar processing steps for other passes. Processed Sea Level Anomaly data is used to study seasonal oceanic variations. We plotted monthly mean of 7 years Jason 1 satellite data for all of those passes.

 

6

Introduction

Altimetry is a technique for measuring height. Satellite altimetry measures the time taken by a radar pulse to travel from the satellite antenna to the surface and back to the satellite receiver. Combined with precise satellite location data, altimetry measurements yield sea-surface heights. Altimetry satellites basically determine the distance or range from the satellite to a target surface by measuring the satellite-to-surface round-trip time of a radar pulse. The return yields information on the global distribution and variability of sea surface height, ocean swell amplitude and scalar wind speed. The shape of the return yields significant wave height and the magnitude yields the scalar wind speed. If the satellite orbit is precisely determined and the range is corrected for a variety of atmospheric, ocean surface and solid earth factors, then these measurements allow determination of changes in sea surface height (SSH) due to tides, geostrophic currents and other oceanographic phenomena to an accuracy of 2-3 cm. Several different frequencies are used for radar altimeters. Each frequency band has its advantages and disadvantages: sensitivity to atmospheric  

7

perturbations for Ku-band, better observation of ice, rain, coastal zones, land masses ... for Ka-band. The principal objective is to measure the range R from satellite to the sea surface. The pulse interacts with the rough sea surface and part of the incident radiation reflects back to the altimeter. The range R from satellite to mean sea level is estimated from round -trip travel time by

( Ŕ - ∑ ∆Rj ), where Ŕ= c×t/2, range computed neglecting refraction based upon the free

space speed of light c ∆Rj, j=1,.... are corrections for various components of atmospheric refraction and for biases. Now range is transformed to a fixed coordinate system by precision orbit determination of height H of the satellite relative to a specified reference ellipsoid approximation of the geoid. Then it is converted to the height h of the sea surface relative to the reference ellipsoid by h= H - R = H - ( Ŕ - ∑ ∆Rj )

Accurate estimation of R and H are not sufficient for oceanographic applications of altimeter range measurements. The above sea surface height h is the superposition of a number of geophysical effects. In addition to the dynamic effect of oceanographic currents, h is affected by undulation of geoid hg, tidal variations hT and the ocean surface response ha to atmospheric pressure loading. The dynamic sea surface height is thus estimated as hd = h - hg - hT - ha = H - ( Ŕ - ∑ ∆Rj ) - hg - hT - ha

 

8

Altimeter Noise: The presence of water vapor, dry gases and free electrons in the atmosphere reduces the propagation speed of radar pulse. Additional biases in the range estimates are introduced by non Gaussian distribution of the wave field. Failure to account for the effects of the atmospheric refraction and sea-state bias introduces errors in the range measurements that are more than an order of magnitude larger than 1 cm. Therefore these corrections must be applied to transform the round-trip travel time into a range estimate with the high degree of accuracy required for oceanographic applications of altimeter data.

Atmospheric sources of error Dry troposphere: The dry tropospheric range delay varies with the amount of atmospheric mass between sensor and the surface or equivalently with sea level pressure. Correction for this delay uses the surface pressure fields produced by ECMWF. For JASON1 based on the ECMWF rms pressure accuracy of 3 mbar, the associated range error is 7 mm. Wet troposphere: The wet tropospheric range correction is designed to correct the observed altimetric sea-surface elevations for the propagation delay caused by atmospheric water vapor and cloud liquid water. Although it is smaller than the corresponding `dry tropospheric range correction,' the wet correction is more complex, with possibly rapid variations in both time and space. The correction can vary from just a few millimeters in dry, cold air to more than 40 cm in hot, wet air. Ionospheric Free Electrons: Ionospheric refraction of altimetric radar signals is determined by the dielectric properties of the upper atmosphere associated with presence of free electrons. The ionospheric range derived from dual-frequency altimeters has an error about 5 mm.

Sea-state bias: It is generated by ocean swell and mainly consists of electromagnetic (EM) bias and tracker or skewness bias. The sum of these two is called as sea-state bias. Skewness bias can be reduced by post processing, however EM bias cannot be further reduced.

 

9

Electromagnetic bias: It refers to the apparent depression of the mean sea level generated by interaction of the radar pulses with the physical wave properties. In an ocean swell field, EM bias occurs because the troughs of even pure sinusoidal waves are better reflectors than the crests, so that the mean reflecting surface is depressed below mean sea level. Tracker or skewness bias: In the calculation the algorithm assumes that the wave amplitude has a Gaussian distribution. Because the actual waveform is non-Gaussian or skewed, the tracker generates an additional negative offset. This is an instrument error and can be reduced by post processing.

Error in orbit determination: At short time scales, uncertainties in the satellite orbital position are the largest source of range error. Orbit errors divide into single pass errors, which are associated with a single range estimate, and the error associated with monthly or greater time scale averages over spatial scales of few hundred kilometers.

Environmental Sources of uncertainty In addition to the height changes generated by geostrophic flows, sea surface height is also physically altered by ocean tides and the inverse barometer effect. Tides are generated by the relative motion of Earth, moon and sun; the inverse barometer effect is the surface response to spatially variable changes in sea level pressure. Tides: Ocean tides occur at specific discrete frequencies. Tides produce elevation changes of 1-3m, and except for very large ocean waves are the largest contributor to ocean surface variability. Given tidal models, most of the tidal signals can be removed from the altimeter range retrieval, which greatly improves the accuracy of geostrophic height retrieval. Inverse barometer: Atmospheric pressure exerts a downward force on the sea surface. Spatial and temporal variations of this force are compensated at least partially by variations of the sea surface elevation. These variations of the sea surface elevation are unrelated to sea surface topographic features associated with geostrophic currents and therefore must be removed to obtain accurate estimates of the dynamic sea surface height hd. The in 

10

verse barometer correction works well over the open ocean, but breaks down in small marginal seas and in the western boundary currents. Although the inverse barometer and dry troposphere corrections are both functions of sea level pressure, they differ fundamentally. The dry troposphere correction yields an electromagnetic range delay independent of surface displacement; inverse barometer effect is a physical surface displacement. Similar to the dry troposphere correction, the inverse barometer effect is removed using ECMWF surface pressure fields. The error in this correction is about 3 cm.

RADS DATA: The RADS data base consists of one metafile and one or more data files per satellite pass. Ascending passes have odd numbers; descending passes have even numbers. The data files contain the binary data. The meta files describe the contents, for example, data type, units, creation history etc. of the data in one data file. There is only one metafile for each pass. The data files are grouped in one directory for each cycle. These cycle directories are then grouped into one directory for each mission phase, which are finally part of one directory per satellite. To read and manipulate the data, the standard netCDF tools, like ncdump (that comes with netCDF package), GMT(Generic Mapping Tools),nco(NetCDF Operators) can be used.

 

11

Methods

We started processing by selection of valid ocean data. STEPS 1] Initially we sort out the appropriate data by applying maximum and minimum limits on specific data fields. For the construction of sea level anomaly all fields with a positive option number described in RADS manual are checked against respective limits. A data field with a factor of 0 means that correction is neither added nor subtracted from sea surface height, but may be considered as an edit criterion in the construction of sea level anomaly. However a negative option means that the data field is not used for creation of the sea level anomaly, nor for its editing. Following are the limits of all the data fields having positive option number mentioned in RADS manual. (all values are in m) Altitude: >=1300000 & =1300000 & =•.6 & =•.40 & =•5 & =•2.4 & =•1.0 & =•1.0 & =•5 & =•5 & =•0.1 & =•1.0 & =•200 & =•1.0 & =0 & =6 & =0 & =0 & =0 & =15.5 &