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GES DISC DAAC Data Guide: Total Ozone Mapping Spectrometer (TOMS) Level 2 Orbital Ozone and Reflectivity Data Set (Version 7)
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THIS DOCUMENT IS AVAILABLE ON THE GES DISC WEB SITE FOR HISTORICAL INFORMATION
PURPOSES ONLY.
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Summary:
The Nimbus-7 TOMS data represent the primary long-term, continuous record of
satellite-based observations available for use in monitoring global and
regional trends in total ozone over the past 15 years. The data record will be
continued by follow-on TOMS instrumentation flown aboard pre-EOS and
EOS-era platforms including Meteor-3, EP, and ADEOS. The data are produced by
the Laboratory for Atmospheres at the Goddard Space Flight Center and are
distributed by the Goddard Distributed Active Archive Center (DAAC). The
DAAC will continue to provide updates to this data set as it is reprocessed
by the data producer. As of May 1996, the Version 6 TOMS data has been
replaced in the DAAC archives by the latest Version 7 reprocessed data.
Table of Contents:
-
-
-
TOMS Level 2 Orbital Data
-
- This data set contains satellite-derived estimates of daily
averaged, global total column ozone and reflectivity measured along
the orbital track at each of 35 fields-of-view comprising a scan
line. The data were derived from backscattered ultraviolet
measurements taken aboard the Nimbus-7 spacecraft by the TOMS
instrument over a 14.5 year period extending from October 1978 - May
1993. The data were processed by the Ozone Processing Team at the
Goddard Space Flight Center using the latest Version 7 algorithm and
are available from the GSFC Distributed Active Archive Center. Each
file contains a day's worth of gridded data stored using the Hierarchical Data Format (HDF)
developed by the National Center for Supercomputing Applications (NCSA)
at the University of Illinois.
-
-
The purpose of this data set is to provide information pertaining to the
global and regional variability of ozone over both short- and long-term time scales. This includes understanding the factors influencing the month-to-month,
seasonal and interannual variability of ozone. In particular, this data set
has been extremely useful in monitoring long-term trends in ozone resulting
from the injection of chlorofluorocarbon (CFC) compounds into the
stratosphere over the past several decades.
-
-
The primary geophysical parameters contained in this data set are the following:
- Total Ozone
- Bulk UV Reflectivity
- Calibrated Backscattered UV Radiances (312 - 380 nm)
-
- Total ozone is the primary geophysical parameter of interest
derived from the TOMS radiance measurements. It represents the
cumulative amount of ozone contained in a column of air extending from
the surface of the earth to the top of the atmosphere. The
reflectivity parameter is derived from the TOMS wavelengths which are
not affected by ozone absorption. It is used to define an effective
lower boundary of the atmosphere for use in the computation of total
ozone, and is dependent upon the combined effects of the actual
surface albedo, the cloudiness and the amount or tropospheric aerosols
present within the instrument field-of-view. Both parameters are
reported on a daily basis for the entire globe. In addition, there are
several auxiliary parameters used in the derivation of the total ozone and
reflectivity including the calibrated, backscatterd UV radiances at
6 wavelengths. A quality flag for each retrieval is also included to assist users
in the selection and use of the primary retrieval quantites. Please refer to
in Variable Description/Definition for more details.
-
-
All of the above data sets are available from the GSFC DAAC.
-
- Richard McPeters
- Atmospheric Chemistry and Dynamics Branch
- NASA/Goddard Space Flight Center
- mcpeters@wrabbit.gsfc.nasa.gov
- Arlin Krueger
- Atmospheric Chemistry and Dynamics Branch
- NASA/Goddard Space Flight Center
- krueger@chapman.gsfc.nasa.gov
- P.K. Bhartia
- Atmospheric Chemistry and Dynamics Branch
- NASA/Goddard Space Flight Center
- bhartia@chapman.gsfc.nasa.gov
- Jay Herman
- Atmospheric Chemistry and Dynamics Branch
- NASA/Goddard Space Flight Center
- herman@jwocky.gsfc.nasa.gov
-
Incoming solar radiation undergoes absorption by gases such as ozone and
Rayleigh scattering by molecules in the stratosphere. Radiation that penetrates to the troposphere is scattered by clouds and aerosols, with the radiation that reaches the ground being scattered by surfaces of widely different reflectivity.
The two shortest wavelengths chosen for use in the TOMS ozone measurements were selected because of their high ozone absorption. Absorption by other atmospheric components, at these wavelengths, is negligible compared to that of ozone.
The backscattered radiance at a given wavelength depends, in principle, upon the entire ozone profile from the top of the atmosphere to the surface. At wavelengths longer than 310 nanometers (nm), however, the backscattered radiance
consists primarily of solar radiation that penetrates the stratosphere and is reflected back by the dense tropospheric air, clouds, aerosols and the Earth's
surface. Because most of the ozone (about 90%) is in the stratosphere, the principal effect of total atmospheric ozone is to attenuate both the solar flux
reaching the troposphere and the component reflected back to the satellite. This nearly complete spatial separation of the absorber elements in the stratosphere (i.e. ozone) from the "reflector" elements in the troposphere (i.e.
aerosols, clouds, and Earth's surface) causes backscattered radiances longer
than 310 nm to depend only weakly on the vertical distribution of ozone in the atmosphere. In the simplest case, whereby tropospheric and surface characteristics remain unchanged from one measurement to the next, and with no aerosols
present in the stratosphere, a decrease (increase) in the backscattered radiance at the shortest TOMS wavelengths would signify an increase (decrease) in the total ozone amount below the satellite. Further discussion concerning the
theory behind backscattered ultraviolet radiation and its relationship to atmospheric ozone can be found in Liou (1980) and Klenk et al. (1982) .
Derivation of atmospheric ozone content from measurements of the backscattered radiances requires a treatment of reflection from the Earth's surface and of
scattering by clouds and other aerosols. In general, the scattered or
reflected light depends on both incidence angle of the sunlight and viewing angle of the satellite. Studies ( Dave (1978) ) show that,
in practice, the contribution of clouds and aerosols to the backscattered intensity can be treated by assuming the presence of an effective Lambertian
reflectivity characterizing the lower troposphere, which collectively accounts for the backscattering effects of clouds, aerosols and the surface of the earth. This process of deriving an effective "scene reflectivity" is performed
for every instantaneous field-of-view (IFOV) along the TOMS scanline, and is
described further in Derivation Techniques and Algorithms.
-
-
-
- Sun-synchronous polar orbiting satellite
-
- Nimbus-7 polar orbiting satellite
-
-
The Nimbus-7 satellite contains several
instruments used for earth/atmosphere research with respect to meteorology,
oceanography and atmospheric pollution. In particular, TOMS measures the
solar UV flux and backscattered earth radiance for the purposes of determining baseline variations of radiation outside the earth's atmosphere, and the
effect of these variations upon the earth's climate. This is most effectively
accomplished in conjunction with the measurements obtained from the other 6
instruments that comprise the Nimbus-7 observational package.
-
-
Nominal orbit parameters for the Nimbus-7 spacecraft were:
- Launch date : 10/24/78
- Orbit : Sun-synchronous, near polar
- Nominal Altitude (km) : 955
- Inclination (deg) : 99.3
- Nodal Period (min.) : 104
- Equator Crossing Time : 12:00 P.M. (ascending)
- Nodal Increment (deg) : 26.1
-
-
TOMS is a single stage fixed-grating Ebert-Fastie monochromater with a
rotating chopper wheel to resolve the incoming light into 6 wavelength bands using a
triangular slit function with a 1 nm bandpass. Backscattered radiances are
measured at the following wavelengths:
312.5 nm, 317.5 nm, 331.3 nm, 339.9 nm, 360.0 nm, and 380.0 nm
TOMS maps total ozone by scanning through the subsatellite point in a
direction perpendicular to the orbital plane. Scans are taken 8 seconds apart, providing a contiguous mapping of ozone.
To measure the solar irradiance, a ground aluminum diffuser plate is deployed to reflect sunlight into the instrument. It is normally deployed once a
week for TOMS and is required as part of the retrieval algorithm used to
derive total ozone from the backscattered radiance measurements.
However, no onboard measure of long-term changes in the reflective
characteristics of the diffuser is available; this must be derived from the
radiance measurements themselves prior to performing the total ozone
retrievals.
-
-
Facing the direction of spacecraft motion, TOMS scans from the extreme right,
passes through nadir to the extreme left, and returns to the extreme right to
begin scanning again. Each of the 35 steps is 3 x 3 degrees, which when
projected on the surface of the earth from the nominal orbit altitude of 955
km, varies from a diamond 125 x 280 km at the extremes to a square 50 km on
a side at nadir. On the ascending node, TOMS scans from east to west. The
total swath is 3000 km.
-
-
Beckman Instruments, Inc., Anaheim, California
-
-
Portions of the following sections on TOMS calibration were quoted from:
The Nimbus-7 Total Ozone Mapping Spectrometer (TOMS) Data Products User's
Guide, NASA Reference Publication 1384, April, 1996, which can be downloaded
from here as a PDF document.
-
- The TOMS prelaunch wavelength calibration was determined
using a photographic technique wherein the positions of the images of
the back-illuminated TOMS exit slit were compared to the positions of
the spectral-line images of a low-pressure mercury-argon lamp that was
placed at the exit slit. The wavelengths, determined from prelaunch
calibration results, have an estimated accuracy of +/- 0.05 nm. TOMS
wavelength calibration monitoring uses observations of four wavelength
bands, near the center and in the wings of the 296.7 nm Hg line. More
detailed descriptions of the instrument calibration can be found in Heath et. al. (1975) and the Nimbus-7 User's Guide (1978) .
-
- Uncertainties in the determination of the wavelength calibration yield an upper limit of 0.005 nm to any possible change in the wavelength scale.
-
- Scans of the mercury-argon lamp for in-flight monitoring of the wavelength calibration were normally made twice per week.
-
- Prelaunch radiometric calibration coefficients were
obtained for both the incident solar irradiance, F, and the
backscattered radiance measurements, I, at all six TOMS
wavelengths. However, since the total ozone algorithm utilizes the
ratios I/F, the detection of trends in total ozone is critically
dependent upon the optical properties of the diffuser plate with time,
involving changes in both the magnitude and angular distribution of
the reflected radiation. Proper characterization of both the TOMS
diffuser plate and spectrometer degradation must be performed through
careful analysis and is described in greater detail in Herman et al. (1991) . See also
Special Corrections/Adjustments and Processing
Changes for further information.
-
-
Not available at this time.
-
-
- Not Applicable.
-
- Not Applicable.
-
-
-
- Global
-
-
Typical daily coverage, June
Typical daily coverage, March or September
Typical daily coverage, December
-
- 50 km at nadir, 150 km at scan extremes
-
- Swath coordinates
-
- Not Applicable.
-
-
- October 31, 1978 - May 6, 1993
-
- Not available at this time.
-
- Daily
-
-
- See Variable Description/Definition below.
-
PARAMETER DESCRIPTION UNITS
--------- ----------- -----
LSEQNO Sequential number of scan unitless
YEAR Four digit year GMT
DAY Day of year at start of scan GMT
GMT Seconds of day GMT sec
ALTITUDE Spacecraft altitude km
NADIR Nadir scan angle degrees * 100
SYNC Chopper non-synch occurrence flag unitless
0 ---> doesn't occur in current or next scan
1 ---> occurs in current scan, not in next
2 ---> occurs in next scan, not current
3 ---> occurs in both current and next scan
LATITUDE Geodetic latitude degrees * 100
LONGITUDE Geodetic longitude degrees * 100
SOLAR_ZENITH_ANGLE Solar zenith angle at IFOV degrees * 100
PHI Sun-satellite azimuth angle degrees * 100
TOTAL_OZONE Total column ozone amount matm-cm * 10
REFLECTIVITY Lambertian surface reflectivity % * 100
ERROR_FLAG Error flag unitless
0 ---> good data
1 ---> good data, 84 < SOLAR_ZENITH_ANGLE < 88
2 ---> 331 nm residue too large
3 ---> triplet residue too large
4 ---> SOI > 24 (SO2 contamination)
5 ---> | residue | > 12.5 for at least 1 channel
10-15 ---> same as above but for descending path
OZONE_BELOW_CLOUD Ozone below cloudy portion of scene matm-cm
TERRAIN_PRESSURE Ground pressure from NMC atm * 100
CLOUD_PRESSURE ISCCP climatological cloudtop height atm * 100
SOI Sulfur-dioxide index unitless + 50
ALGORITHM_FLAG Retrieval scheme indicator unitless
1 ---> A triplet alone used
2 ---> B triplet alone used
3 ---> B triplet with A triplet to select profile
4 ---> C triplet with B triplet to select profile
CLOUD_FRACTION Fractional cloud cover percent
MIXING_FRACTION Profile mixing fraction unitless * 10
SURFACE_CATEGORY Surface category code unitless
0 ---> ocean
1 ---> land
2 ---> low inland (below sea level)
3 ---> mixed land and ocean
4 ---> mixed land and low inland
5 ---> mixed ocean, land , and low inland
THIR_CLOUD_PRESSURE Co-located THIR cloud top pressure atm * 100
NVALUE Radiance N-Values at 6 wavelengths unitless * 50
dN/dR Reflectivity sensitivity (dN/dR) -50 / %
SENSITIVITY Ozone sensitivity (dN/dO3) 10^4 / matm-cm
RESIDUE Nmeas - Ncalc *10 + 127
Please refer to Data Manipulations or the Nimbus-7 Total Ozone
Mapping Spectrometer (TOMS) Data Products User's Guide (1996) for
more details on these parameters.
-
- See Variable Description/Definition above.
-
-
The source of information for the two most important parameters derived from
the TOMS instrument (total ozone and reflectivity) are the backscattered UV
radiances measured by the satellite. Information on the total ozone content
originates from the modulation of the shortest wavelength radiances by
atmospheric ozone absorption, while information on reflectivity originates from
the modulation of the longer wavelengths due to scattering by molecules, clouds,
aerosols, and the surface of the earth.
PARAMETER DATA SOURCE
--------- -----------
Total Ozone Backscattered radiances measured by the TOMS
instrument in four discrete spectral channels
between 312.5 and 339.9 nm.
Reflectivity Backscattered radiances measured by the TOMS
instrument in the additional two discrete
spectral channels 360 nm and 380 nm.
-
- Not available at this time.
-
- Since the TOMS data are stored as scientific data objects in
the HDF format, it is not possible to provide a simple representation
of a "data record" in the conventional sense for this section. Please
refer to the section Data Format for details on
the structure of the TOMS HDF file and the fields contained therein.
-
-
- A general description of data granularity as it applies to the IMS appears in the EOSDIS Glossary.
- A Level 2 TOMS granule consists of a single orbit of data at the
original resolution of the instrument. There are multiple geophysical parameter arrays
within each orbital file. The approximate compressed and uncompressed file sizes for a TOMS level 2 file are 600 kB and 830 kB, respectively.
-
- The TOMS level 2 orbital parameters are stored as Scientific Data Sets (SDS) in the
Hierarchical Data Format (HDF) . There are 27 HDF SDSs for the data fields, which are either 1 dimensional (scan), 2 dimensional (scan x scene), or 3 dimensional
(scan x scene x wavelength). The table below lists the data type and dimension of each SDS in the orbital file.
PARAMETER DATA TYPE DIMENSIONS
--------- --------- ----------
LSEQNO int16 394
YEAR int16 394
DAY int16 394
GMT int32 394
ALTITUDE int16 394
NADIR int16 394
SYNC int16 394
LATITUDE int16 394 x 35
LONGITUDE int16 394 x 35
SOLAR_ZENITH_ANGLE int16 394 x 35
PHI int16 394 x 35
TOTAL_OZONE int16 394 x 35
REFLECTIVITY int16 394 x 35
ERROR_FLAG int16 394 x 35
OZONE_BELOW_CLOUD uint8 394 x 35
TERRAIN_PRESSURE uint8 394 x 35
CLOUD_PRESSURE uint8 394 x 35
SOI uint8 394 x 35
ALGORITHM_FLAG uint8 394 x 35
CLOUD_FRACTION uint8 394 x 35
MIXING_FRACTION uint8 394 x 35
SURFACE_CATEGORY uint8 394 x 35
THIR_CLOUD_PRESSURE uint8 394 x 35
NVALUE int16 394 x 35 x 6
dN/dR uint8 394 x 35 x 6
SENSITIVITY int16 394 x 35 x 5
RESIDUE uint8 394 x 35 x 5
where:
uint8 = 8-bit unsigned integer
int16 = 16-bit integer
int32 = 32-bit integer
Fill values for missing data for each of these parameters depends upon the data type used. These fill values are shown below:
DATA TYPE FILL VALUE
--------- ----------
uint 255
int16 32767
int32 2147483647
In addition to the actual data, each TOMS orbital file contains self-documenting text and metadata information. These include:
- A File Label
- A Detailed File Description or Annotation
- A list of Metadata Attributes (stored as a 2nd File Description)
- A list of Global File Attributes
More detailed descriptions
of the metadata information can be obtained from The Nimbus-7 Total Ozone Mapping Spectrometer (TOMS) Data Products
User's Guide (1996).
-
-
-
The intensity of solar radiation backscattered by the earth-atmosphere system and received by a sensor aboard an earth-orbiting satellite can be expressed as:
I(i) = Ia(i) + Ig(i)
where
- I(i) is the backscattered radiance at wavelength i
- Ia(i) is the atmospheric contribution to the radiance at wavelength i
- Ig(i) is the contribution due to multiple reflections from the surface
The ground contribution is given by:
Ig(i) = [ R/(1-R*S(i)) ] * T(i) = R*T(i) / (1-R*S(i))
where - R is the Lambertian reflectivity of the lower
boundary
- T(i) is the amount of direct plus diffuse radiation
reaching the surface, then diffusely transmitted upward to the
satellite
- S(i) is the fraction of radiation reflected by the
surface that is scattered back to the surface by the atmosphere. The
term 1/( 1- R*S) effectively accounts for multiple reflections between
the ground and the atmosphere.
In the above, I(i) and Ig(i)
depend upon total ozone amount, the effective scene pressure level and
reflectivity, the solar zenith angle and the satellite viewing
angle. The purely atmospheric contribution Ia(i) as well as T(i)
depend upon all of the above except the reflectivity R. The values of
I(i), Ia(i) and to a lesser extent Ig(i) are also somewhat dependent
upon the shape (i.e., vertical distribution) of the ozone profile.
Once the measured backscattered radiances have been corrected for
the effects of wavelength drift and changes in the instrument optics
and sensitivity (see McPeters et al. (1996)
), a quantity called the "N-value", or N(i), is formed in order to
decrease the dynamic range of the total ozone dependence:
N(i) = -100 log[ I(i) / F(i) ] where the ratio I/F denotes the
backscattered radiance I(i) normalized by the direct solar radiation,
F(i), incident at the level of the sensor. Given the optical
properties of the atmosphere at each TOMS wavelength, a set of tables
is created relating total ozone to I/F (and thus N) for several
independent variables. These include - Climatological ozone
profiles (26 profiles, 6 low latitude, 10 mid latitude, 10 high
latitude, each group in increments of 50 Dobson units)
- Pressure at
the reflecting surface.(2 pressures, 400 mb and 1000 mb)
- Solar
zenith angle (10 angles from 0 to 88 degrees)
- Satellite zenith
angle at the IFOV (6 angles from 0 to 70 degrees)
The scene
reflectivity R is not included as a table variable since the tabulated
quantities of interest, S(i), T(i) and Ia(i), do not depend upon
it. The theoretical values of I/F at each of the 6 TOMS wavelengths
are calculated using the radiative transfer methodology of Dave (1964) . The computation of total column
ozone is accomplished by computing radiance ratios called pair values,
which are ratios of I/F at a longer wavelength, which is relatively
insensitive to ozone, to that of a shorter, ozone-sensitive
wavelength: - A-pair = N(313 nm) - N(331 nm)
- B-pair =
N(318 nm) - N(331 nm)
- C-pair = N(331 nm) - N(340 nm)
Pairs are chosen about 20 nm apart or less, so that scattering effects
are about the same, and the relative attenuation of the pair is
sensitive mostly to ozone absorption. In addition, the ratios of the
radiances help to minimize calibration errors and wavelength
independent effects. Different pairs of wavelengths are used for
different conditions, i.e., for large ozone amounts at low sun angles
the A-pair becomes less sensitive to changes in total ozone since 313
nm senses higher in the atmosphere ( Klenk at
al. (1982) ). It also becomes more sensitive to ozone profile
shape; thus more weight will be placed upon the derived B-pair and
C-pair ozone values in this case. A modification of the N-pair
technique using wavelength triplets was implemented in the Version 7
methodology, and is described below. The basic procedure for
deriving total ozone from TOMS measurements consists of the following
steps: - Determination of the reflectivity of the lower
boundary of the atmosphere, R
This is obtained using
the TOMS measurement (Im) at 380 nm, which is insensitive to ozone
absorption. Two radiance values are extracted from the tables for the
particular location and observing geometry, a ground radiance (Ig)
derived using the ground pressure and a corresponding surface
reflectivity (Rg) of 8%, and a cloud radiance (Ic) derived using the
climatological ISCCP cloud top pressure and corresponding cloud
reflectivity (Rc) of 80%. If the measured 380 nm radiance Im lies
between Ic and Ig, then an effective cloud fraction is determined by
f = (Im - Ig) / (Ic - Ig) with an associated effective
reflectivity for the IFOV given by R = Rg*(1-f) + f*Rc If Im
is outside this range, the effective reflectivity at 380 nm is
computed from the following expression: R = (I - Ia)/(T - S*(I -
Ia) ) where Ia, T, and S are obtained from the tables for the
given sun and satellite angles. In both cases above, a special
adjustment is made to the derived value of R in the presence of ice
and/or snow. Please refer to McPeters et
al. (1996) for more details. - Derivation of a first
guess total ozone value
An initial guess is obtained for the
total ozone using the B-pair wavelengths and the information on
effective cloud fraction and reflectivity found in step 1. For the
particular latitude and geometry, radiances are calculated from the
quantities in the tables for the range of ozone values appropriate to
that band. This is done to obtain both ground radiances Ig as well as
cloud radiances Ic by interpolating between the 1000 mb and 400 mb
entries for the given terrain and cloud heights. The cloud fraction is
then used to combine the ground and cloud radiances into a single
value representative of that TOMS IFOV for each tabulated ozone
amount. The measured B-pair N-value is compared with the set of B-pair
N-values calculated at each tabulated ozone value, and linear
interpolation in N-value is performed to obtained the first guess
total ozone amount. - Derivation of a best ozone value
Using the first guess ozone, N-values are calculated at all TOMS
wavelengths. Differences between these values and the measured
N-values, called the residuals r(i), are then used as a basis for
correcting the total ozone value for possible wavelength dependencies
in the reflectivity and other residual instrument characterization
effects. The wavelength dependent residual is modeled for each
wavelength i as: r(i) = s(i) * (OZ - OZ0) + b * (i - 380)
where s(i) is the sensitivity of N(i) due to changes in total ozone,
OZ is the desired ozone value, OZ0 the first guess ozone value, and b
is a constant. This equation explicitly makes use of the 380 nm
wavelength, and when used with two other wavelengths (hence the
designation triplet ) results in a new estimate for the total
ozone. The choice of triplet is dictated by the total path length
associated with the IFOV, with the A-, B- and C-triplets consisting of
the A-, B- and C-pair wavelengths plus 380 nm. Finally, a simple
linear latitudinal mixing is used to obtain the "best ozone" value for
path lengths less than 1.5, while for higher path lengths a somewhat
more complicated technique is used which requires consistency between
two different triplets. A more rigorous treatment can be found in McPeters et al. (1996).
-
-
- Raw measurements and image location data were obtained
by the Ozone Processing Team (OPT) at Goddard Space Flight Center and
merged to produce radiance data tapes called Raw Units Tape-TOMS
(RUT-T). A RUT-T tape contains the uncalibrated TOMS radiance
measurements at the 6 specified wavelengths for each field-of-view
along each orbit. It also contains solar, satellite, and earth
reference data, plus housekeeping data. Other ancillary data needed as
input to the processing include terrain height and information
pertaining to the presence of clouds and snow/ice. Terrain height is
obtained from the National Meteorological Center (NMC) on a 0.5 by 0.5
degree grid, and interpolated to the TOMS IFOV to obtain the average
ground pressure after converting from height using the U.S. Standard
Atmosphere. Cloud information, which in Version 6 was based upon a
climatology derived from the THIR instrument aboard Nimbus-7, is now
based upon the ISCCP climatology. Snow/ice probabilities are obtained
from the Air Force Global Weather Center on a polar stereographic
projection, from which a monthly snow/ice indicator field mapped to a
1 degree by 1 degree grid is created for use in the TOMS retrievals.
Radiance data on the TOMS RUT-T tapes are used to derive total ozone,
reflectivity and other useful parameters such as a sulfur dioxide
index (an indicator of volcanic eruptions) for each individual
IFOV. These are stored as a level 2 data product in both binary format
for internal purposes within the TOMS processing center, and in
Hierarchical Data Format for general distribution to the public by the
DAAC.
-
- Several changes were made in the TOMS processing which
resulted in improved estimates of total ozone compared to the earlier
Version 6 results. These include:
- implementation of a
new method to account for long-term drift in ozone due to variations
in instrument sensitivity with time (see Special
Corrections/Adjustments for more information)
- determination
of a new wavelength calibration, using pre-launch calibration data,
which removed long-standing biases between coincident SBUV and
TOMS-derived total ozone measurements.
- use of a 2-layer model
employing ISCCP climatology to characterize partially clouded scenes
when accounting for surface reflectivity effects in the determination
of total ozone
- use of triplets of wavelengths (rather than pairs
as in Version 6 to solve for ozone while simultaneously accounting for
residual effects that are assumed linear with wavelength, such as the
wavelength dependence of the surface reflectivity arising from the
effects of dust and/or sea glint. See Derivation
Techniques and Algorithms for a more detailed description.
-
improved latitudinal weighting scheme at higher path lengths (i.e.,
high solar zenith angles as encountered in the polar regions).
-
implementation of an improved sulfur dioxide index to eliminate an
offset appearing in the data in the absence of SO2.
Refer
to the Nimbus-7 Total Ozone Mapping Spectrometer
(TOMS) Data Products User's Guide (1996) for more details.
-
-
- The major correction which is performed as part of the
TOMS data processing involves accurate characterization of the
diffuser plate degradation with time, which impacts the measured solar
irradiance and therefore the I/F values used to determine the total
ozone. This step is especially critical since an inaccurate
characterization can lead to artificial trends in the long-term time
series ozone measurements. The previous Version 6 algorithm used the
so-called Pair Justification Method (PJM) of
Herman et al (1991) in place of the exponential diffuser degrader
model used by Cebula et al. (1988) in the
generation of the TOMS Version 5 total ozone data. In the Version 7
methodology, time-dependent changes in instrument sensitivity are
deduced directly from the radiance measurements. Since the 4 longest
TOMS wavelengths are insensitive to ozone, discrepancies in the
reflectivity R derived from each wavelength over ocean provide a
measure of the calibration errors at these wavelengths. The instrument
sensitivity changes at the 2 shortest wavelengths are then inferred by
fitting a quadratic to the degradation determined at the longer
wavelengths.
Refer to Wellemeyer et
al. (1996) and to the Nimbus-7 Total Ozone
Mapping Spectrometer (TOMS) Data Products User's Guide (1996) for
more details.
-
- The TOMS ozone retrieval methodology is based upon a
look-up table relating radiance measurements to total ozone for
typical atmospheric conditions and satellite measurement
geometries. As such, a detailed radiative transfer code (see Dave (1964) ) was used to compute these
theoretical backscattered UV radiances as a function of solar zenith
angle, satellite view angle, relative azimuth, surface pressure, and
ozone profile shape and amount through the use of latitude-dependent,
standard climatological profiles. See Derivation
Techniques and Algorithms for more details and further references.
-
- Not available at this time.
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-
-
The ozone values derived from TOMS measurements have three types of uncertainties:
- uncertainties in the basic measurements
- uncertainties in the physical quantities used to retrieve ozone values from the measurements
- uncertainties in the mathematical procedure used to retrieve ozone values from the measurements
Each of these sources of error can be manifested in one or more of three ways:
- random errors
- time-invariant systematic errors
- time-dependent systematic errors (drifts)
See Klenk (1982) for a general description of the uncertainties in the total ozone derivation, and McPeters et al. (1996) for numerical estimates for these errors in the Version 7 TOMS data.
-
-
- Ground-based Dobson stations are used as the reference
for validating the TOMS total ozone data. Comparisons were made with a
network of 30 Dobson stations which included data from all seasons but
were weighted toward mid-northern latitudes. In general, the
measurements from the satellite- and ground-based instruments are
spatially coincident within 100 km and temporally coincident within 1
hour. Weekly means of the differences between the Dobson- and
satellite-derived total ozone measurements were calculated for the
validation. For the entire 14.5 year record of TOMS data, the mean
difference was found to be 0.5 %, with a standard deviation of 0.7
%. In addition, the overall trend in this difference amounts to about
0.2 % per decade; thus these differences are within the combined
uncertainties of the two estimation techniques.
-
-
-
- The following error estimates apply to the TOMS-derived
total ozone:
- Absolute error : +/- 2 %
- Random error :
+/- 2 % (1 sigma value)
- Drift uncertainty : +/- 1.0 % per decade
The drift error is somewhat higher at high latitudes. The
difference between the TOMS and Dobson total ozone measurements at the
time of launch is approximately 1 %, with TOMS reporting higher ozone
values. The time dependence of this bias is small and can be
approximated as linear with a slope of less than 0.2 % per decade, or
0.3 % over the 14.5 year lifetime of the TOMS instrument. The error
estimates for the reflectivity are not available at this time.
There are additional sources of error which contribute to the
uncertainty in total ozone, but which only occur for specific times,
locations, or physical conditions (such as volcanic eruptions). Please
refer to Known Problems with the Data for a
discussion of these sources.
-
- Each TOMS ozone retrieval has an associated quality
flag which if non-zero indicates the presence of SO2 contamination, an
extremely large solar zenith angle, larger than normal triplet
residues, or retrieval over the descending portion of the orbit. See Variable Description/Definition for a definition of this flag.
-
- The metadata accompanying each data file are checked
for consistency and valid ranges during the archive process. A
sampling of daily data files as well as all monthly means have been
visually examined to ensure no corruption of the data following
transfer to the DAAC. Checksums for each file are computed during the
archive process and stored in the database for future comparison upon
retrieval of the file from the archive.
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-
- Due to the nature of the TOMS measurements, total ozone
values can only be derived during the sunlit portion of the
orbit. In addition, total ozone is not derived for periods of time
and ranges of latitude for which the radiances are affected by solar
eclipses.
-
- There are several problems localized in space and time which
may affect the quality of the ozone retrievals derived from TOMS
radiance measurements. These include the following:
- Volcanic effects : Sulfur dioxide (SO2) injected into the
stratosphere by volcanic eruptions such as El Chichon (1982) and
Mt. Pinatubo (1991) can cause anomalous absorption of radiation at the
TOMS wavelengths which would be interpreted as increased ozone
levels. Furthermore, conversion of gaseous SO2 to sulfuric acid
aerosol (H2SO4) results in enhanced backscattering of radiation which
would be interpreted as a decrease in ozone. An SO2 index based on the
algorithm of Krueger et al. (1995) is
included in the orbital (level 2) ozone data which serves to flag
possible volcanic contamination. These data are not included when
creating the level 3 gridded TOMS data product.
- Polar
Stratospheric Clouds : Polar Stratospheric Clouds (PSCs) occur in
the Antarctic region during winter when temperatures drop below about
-80 degrees C. The presence of these ice clouds and the resulting
enhanced backscattering of radiation can cause underestimation of the
total ozone at large solar zenith angles (> 80 degrees) in the
vicinity of 2% to 6% for typical clouds, and as much as 50% for
optically thick PSCs. These effects have not been corrected for in the
TOMS data sets.
- Sun glint : A scan angle dependence on
the order of 1% is seen in the retrieved total ozone. In the presence
of sun glint, which for TOMS occurs with the sun directly overhead
over the ocean, this is accentuated to a value near 2% from nadir to
scan extremes. This implies a value of ozone that is 1% too low at
nadir due to sun glint.
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-
Ozone retrievals for the descending portion of the orbit (ERROR_FLAG
has values between 10 and 15) taken during the summer solstice around each pole
have been found to be biased low at these extreme solar zenith angles. Users
should therefore avoid the use of data flagged as descending orbit data.
Refer to the Nimbus-7 Total Ozone Mapping Spectrometer (TOMS) Data Products User's Guide (1996) for further information on this topic.
-
-
None available for this data set.
-
Total ozone data as derived from the TOMS instrument are useful for
understanding a variety of phenomena involving both short-term
stratospheric fluctuations and long-term climate change. Stratospheric
ozone modulates the incoming (and biologically harmful) solar
ultraviolet radiation stream through absorption in much the same way
as tropospheric carbon dioxide traps outgoing infrared radiation
emitted by the Earth's surface and atmosphere. Just as an increase or
decrease of carbon dioxide in the lower atmosphere may have a climatic
impact over the long term, so too may changes in the ozone content of
the upper atmosphere. Beside the study of long-term climate change,
other specific examples of scientific applications of this data set
include the following :
- input to global solar radiation
models for use in determining the proportion of Ultraviolet-B (UV-B),
Ultraviolet-A (UV-A), and Photosynthetically Active Radiation (PAR)
penetrating the biosphere (Eck et al. (1995) )
- determination of the long-term trends in total ozone on both
regional (e.g., Antarctica) and global scales (Bowman (1988) )
- study of spatial and
temporal patterns, seasonal cycles, and interannual variability of
ozone (Bowman (1986) )
- use as a tracer
of stratospheric dynamics in the 30-40 mb region where the bulk of the
ozone resides, including correlations with wind and temperature
patterns, especially for transient phenomena such as Sudden
Stratospheric Warmings (Miller et al. (1976) )
and periodic phenomena such as the Quasi-Biennial Oscillation (QBO)
(Lait et al. (1989) )
- input to radiative
transfer models for use in providing atmospheric corrections to
satellite-observed radiances (e.g., AVHRR and CZCS) for the
determination of ocean color and vegetation indices (Gordon and Clark (1981) )
- intercomparison
and validation with results derived from other total ozone
instrumentation such as the TIROS Operational Vertical Sounder (TOVS)
(Lienesch and Pardey (1985) )
-
The Goddard DAAC will continue to support any future
reprocessings of the Nimbus-7 TOMS data. The DAAC will also provide
archive and distribution support for follow-on TOMS missions such as
Meteor-3/TOMS (TOMS/2), EP-TOMS (TOMS/3) and ADEOS TOMS (TOMS/4) as
the data become available from the producers.
-
-
- A utility program written in C called read_tomsl2.c
is available which allows a user to list all of the descriptive
information associated with all arrays in the TOMS HDF file, then
select a particular array and extract spatial subsets of the data. The
output will be in ASCII tabular format which can be printed either to
the user's terminal or to an output file. The routine makes use of the
HDF Version 3.3 release 4 libraries available either from NCSA.
The program was written and tested on a Silicon Graphics
platform and may require minor modifications for use on other unix
machines. More information can be found in the
Data
Access Information - Reading the TOMS HDF Files section of the
TOMS README which accompanies all TOMS data obtained through the DAAC
online ordering system.
In addition, the TOMS HDF files can be
viewed through NCSA's visualization package Collage, which can
be downloaded
from here.
-
- See Software Description for instructions on how
to obtain the TOMS level 2 read software and the required HDF libraries.
-
-
- GSFC DAAC Help Desk
- Code 902
- Goddard Space Flight Center
- Greenbelt, MD 20771, U.S.A.
- Phone:(301) 614-5224
- Fax:(301) 614-5268
- Email:daacuso@daac.gsfc.nasa.gov
-
-
Goddard Distributed Active Archive Center
-
- The data can be obtained via the EOSDIS Version 0
Information Management System (IMS), the local Goddard DAAC IMS, or
anonymous FTP. World Wide Web (WWW) access is also available for this
dataset. Refer to the Data Access Information - Getting the Data section of the TOMS
README for detailed information on ordering and/or downloading the
data.
-
- The Goddard DAAC will provide archive and distribution
support for the follow-on TOMS instrumentation aboard the Meteor-3,
EP, and ADEOS platforms in 1996. These products will be available via
anonymous FTP as well as through the usual DAAC ordering mechanism.
-
-
The archive HDF data are available via FTP.
-
Bhartia, P.K., et al. 1993, The effect of Mt. Pinatubo aerosols on total ozone measurements from Backscatter
Ultraviolet (BUV) Experiments. J. Geophys. Res., 98, 18547-18554.
Bowman, K.P., 1986, Interannual variability of total ozone during the breakdown of the Antarctic circumpolar
vortex, Geophys. Res. Lett., 13, 1193-1196.
Bowman, K.P., 1988, Global trends in total ozone, Science, 239, 48-50.
Cebula, R.P., H. Park, and D.F. Heath, 1988, Characterization of the Nimbus-7 SBUV radiometer for the long term monitoring of
stratospheric ozone, J. Atmos. Oceanic Technol., 5, 215-227.
Dave, J.V. 1978, Effect of aerosols on the estimate of total ozone in an atmospheric column from the
measurements of its ultraviolet radiance, J. Atmos. Sci., 35, 899-911.
Dave, J.V. 1964, Meaning of successive iteration of the auxiliary equation of radiative transfer. Astrophys. J.,
140, 1292-1303.
Eck, T.F., P.K. Bhartia, and J.B. Kerr, 1995, Satellite estimation of spectral UVB irradiance using TOMS
derived total ozone and UV reflectivity, Geophys. Res. Lett., 22(5), 611-614.
Gordon, H.R., and D.K. Clark, 1981, Clear water radiances for atmospheric correction of Coastal Zone Color Scanner imagery, Appl. Optics, 20, 4175-4180.
Herman, J.R., R. Hudson, R. McPeters, and R. Stolarski, 1991, A new self-calibration method applied to TOMS and SBUV backscattered
ultraviolet data to determine long-term global ozone change, J. Geophys. Res., 96, 7531-7545.
Heath, D.F., A.J. Krueger, H.R. Roeder, and B.D. Henderson, 1975, The Solar Backscatter Ultraviolet and Total Ozone Mapping Spectrometer (SBUV/TOMS) for Nimbus G, Opt. Eng. ,
14(4), 323-331.
Klenk, K.F., P.K. Bhartia, A.J. Fleig, V.G. Kaveeshwar, R.D. McPeters, and P.M. Smith, 1982, Total ozone determination from the Backscattered Ultraviolet (BUV) Experiment, J. Appl. Meteor., 21, 1672-1684.
Krueger, A.J., L.S. Walter, P.K. Bhartia, C.C. Schnetzler, N.A. Krotkov, I. Sprod, and G.J.S. Bluth, 1995, Volcanic sulfur dioxide
measurements from the Total Ozone Mapping Spectrometer instruments, J. Geophys. Res., 100, 14057-14076.
Lait, L.R., M.R. Schoeberl, and P.A. Newman, 1989, Quasi-biennial modulation of the Antarctic ozone depletion, J. Geophys. Res., 94, 559-571.
Lienesch, J.H., and P.K.K. Pardey, 1985, "The use of TOMS data in evaluating and improving the total
ozone from TOVS measurements", Rep. NOAA-TR-NESDIS-23, Issue 22, 3814-3828.
Liou, K.-N., 1980, An Introduction to Atmospheric Radiation, Academic Press, New York.
Madrid, C. R. (ed.), 1978, The Nimbus 7 User's Guide,
Goddard Space Flight Center, National Aeronautics and Space Administration.
McPeters, R., and W.D Komhyr. 1991, Long-term changes in the Total Ozone Mapping Spectrometer relative
to world standard Dobson Spectrometer 83. J. of Geophys. Res., 96, 2987-2993.
McPeters, R.D., et al., 1996, Nimbus-7 Total Ozone
Mapping Spectrometer (TOMS) Data Products User's Guide, NASA Reference
Publication 1384, National Aeronautics and Space Administration, Washington, D.C.
Miller, A.J., R.M. Nagatani, K.B. Labitzke, E. Klinker, K. Rose, and D.F. Heath, 1976, Stratospheric ozone transport during the
mid-winter warming of December 1970-January 1971, paper presented at Joint
Symposium on Atmospheric Ozone, Dresden, Germany, August 9-16, 1976.
Wellemeyer, C., S.L. Taylor, G. Jaross, M.T.
DeLand, C.J. Seftor, G. Labow, T.J. Swissler, and R.P. Cebula, 1996, "Final
Report on Nimbus-7 TOMS Version 7 Calibration", NASA Contractor Report,
National Aeronautics and Space Administration, Washington, D.C.
-
-
Not Available at this time.
-
-
- ADEOS Advanced Earth Observing System
- AVHRR Advanced Very High Resolution Radiometer
- CFC ChloroFluoroCarbon
- CPOZ Compressed Ozone
- CZCS Coastal Zone Color Scanner
- DAAC Distributed Active Archive Center
- DAT Digital Audio Tape
- DU Dobson Unit
- EOS Earth Observing System
- EOSDIS EOS Data and Information System
- EP Earth Probe
- FTP File Transfer Protocol
- GSFC Goddard Space Flight Center
- HDF Hierarchical Data Format
- HDSBUV High Density Solar Backscatter Ultraviolet
- HDTOMS High Density TOMS
- IFOV Instantaneous Field-of-View
- ISCCPInternational Satellite Cloud Climatology Project
- IMS Information Management System
- NASA National Aeronautics and Space Administration
- NCSA National Center for Supercomputer Applications
- NMC National Meteorological Center
- OPT Ozone Processing Team
- PAR Photosynthetically Active irRadiance
- PJM Pair Justification Method
- QBO Quasi-Biennial Oscillation
- RUT-T Raw Units Tape - TOMS
- SBUV Solar Backscatter Ultraviolet
- SDS Scientific Data Set
- SSBUV Shuttle Solar Backscatter Ultraviolet
- THIR Temperature Humidity Infrared Radiometer
- TIROS Television and InfraRed Observation Satellite
- TOMS Total Ozone Mapping Spectrometer
- TOVS TIROS Operational Vertical Sounder
- UV UltraViolet
- UV-A Ultraviolet-A
- UV-B Ultraviolet-B
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