2-b HDO - 490.6 GHz. HDO is measured using the same radiometer in a time

shared mode during roughly half of the 15 orbits per measurement day, each orbit corresponding to about 60 individual limb-scans. The measurement precision for HDO is about 20-30 % (5 ppbv), and single-profile information is obtained between 18-55 km with an altitude resolution in the order of 3-4 km.

2-b HDO - 490.6 GHz. HDO is measured using the same radiometer in a time

shared mode during roughly half of the 15 orbits per measurement day, each orbit corresponding to about 60 individual limb-scans. The measurement precision for HDO is about 20-30 % (5 ppbv), and single-profile information is obtained between 18-55 km with an altitude resolution in the order of 3-4 km.

1 Introduction. The Sub-Millimetre Radiometer (SMR) on board the Odin satellite, launched in February 2001 in a polar sun-synchronous orbit, employs 4 tunable single-sideband

Schottky-diode heterodyne receivers in the 485-580 GHz spectral range. A 1.1 m telescope is used for passive observations of thermal emissions originating from the Earth’s limb. Spectra are recorded using two high resolution auto-correlator spectrometers. Measurements are performed in a time sharing mode with astronomical observations.

In aeronomy mode, various target bands are dedicated to observations of trace constituents relevant to stratospheric / mesospheric chemistry and dynamics such as O3, ClO, N2O, HNO3, H2O, CO, and isotopes of H2O and O3. Profile information is retrieved from the spectral measurements of a limb scan by inverting the radiative transfer equation for a non-scattering atmosphere. A retrieval algorithm based on the “Optimal Estimation Method” has beenadopted for the ground segments of Odin-SMR in Sweden and in France.

The water isotope mode is specifically designed for observations of stratospheric H2O, H2O-18, and HDO using two 800MHz wide bands centred at 488.9 and 490.4 GHz. Achieved observation capabilities of the SMR radiometer for these target species are presented and examples for the global water vapour data set are given.

Potential of the Odin Sub-Millimetre Radiometer for the Study ofStratospheric Water Vapour and its Isotopes

J. Urban (1), N. Lautié (2), D. Murtagh (2), Y. Kasai (3), J. de La Noë (1), E. Dupuy (1), L. El Amraoui (1), P. Eriksson (2), U. Frisk (4), C. Jimenez (1), E. Le Flochmoën (1), M. Olberg (5), and P. Ricaud (1)

(1) Observatoire Aquitain des Sciences de l’Univers / L3AB, Floirac, France; (2) Chalmers University of Technology, Göteborg, Sweden;(3) Communications Research Laboratory, Tokyo, Japan; (4) Swedish Space Corporation, Solna, Sweden; Contact: urban@obs.u-bordeaux1.fr (5) Onsala Space Observatory, Onsala, Sweden.

Potential of the Odin Sub-Millimetre Radiometer for the Study ofStratospheric Water Vapour and its Isotopes

J. Urban (1), N. Lautié (2), D. Murtagh (2), Y. Kasai (3), J. de La Noë (1), E. Dupuy (1), L. El Amraoui (1), P. Eriksson (2), U. Frisk (4), C. Jimenez (1), E. Le Flochmoën (1), M. Olberg (5), and P. Ricaud (1)

(1) Observatoire Aquitain des Sciences de l’Univers / L3AB, Floirac, France; (2) Chalmers University of Technology, Göteborg, Sweden;(3) Communications Research Laboratory, Tokyo, Japan; (4) Swedish Space Corporation, Solna, Sweden; Contact: urban@obs.u-bordeaux1.fr (5) Onsala Space Observatory, Onsala, Sweden.

Acknowledgements: Odin is a Swedish-led satellite project funded jointly by the Swedish National Space Board (SNSB), the Canadian Space Agency (CSA), the National Technology Agency of Finland (Tekes) and the French Centre National d’Études Spatiales (CNES).

Top: the Odin satellite platform with its 1.1 m telescope, solar-panels and -shields just before the launch.

2-a H2O - 488.5 GHz. Single-profile information of

stratospheric water vapour is retrieved between 20 and 70 km with a vertical resolution in the order of 3 km and a precision of 10-20 % (0.5-1 ppmv). Measurement noise might be reduced by data averaging. The Figures show for example zonally averaged water vapour fields as observed by Odin/SMR on April 29-30 and Octobre 26-27, 2002. Odin/SMR water isotope mode measurements are performed in about weekly intervals.

2-a H2O - 488.5 GHz. Single-profile information of

stratospheric water vapour is retrieved between 20 and 70 km with a vertical resolution in the order of 3 km and a precision of 10-20 % (0.5-1 ppmv). Measurement noise might be reduced by data averaging. The Figures show for example zonally averaged water vapour fields as observed by Odin/SMR on April 29-30 and Octobre 26-27, 2002. Odin/SMR water isotope mode measurements are performed in about weekly intervals.

2-c δD (HDO). The zonal mean depletion of stratospheric deuterium with

respect to its isotopic ratio in Standard Mean Ocean Water (SMOW) of 1.5576×10-4

can be derived from the Odin/SMR measurements of H2O and HDO. This variation is usually expressed using δ-notation: δD = { (2[HDO]/[H2O] - R0) / R0 }×100 [%], where R0 is a standard isotope ratio (e.g. SMOW). The Figures show preliminary results obtained for April 29-30 and October 26-27, 2002. A maximum depletion in the order of 60 % is observed in the lower stratosphere of the tropics and δD increases with altitude above. Results are in qualitative agreement with 1-d and 2-d model calculations [e.g. Ridal, JGR, 2001; Bechtel & Zahn, ACPD, 2003] simulating δD as function of the relative contributions of the different sources of stratospheric water vapour such as methane oxidation and transport through the tropical tropopause.

2-c δD (HDO). The zonal mean depletion of stratospheric deuterium with

respect to its isotopic ratio in Standard Mean Ocean Water (SMOW) of 1.5576×10-4

can be derived from the Odin/SMR measurements of H2O and HDO. This variation is usually expressed using δ-notation: δD = { (2[HDO]/[H2O] - R0) / R0 }×100 [%], where R0 is a standard isotope ratio (e.g. SMOW). The Figures show preliminary results obtained for April 29-30 and October 26-27, 2002. A maximum depletion in the order of 60 % is observed in the lower stratosphere of the tropics and δD increases with altitude above. Results are in qualitative agreement with 1-d and 2-d model calculations [e.g. Ridal, JGR, 2001; Bechtel & Zahn, ACPD, 2003] simulating δD as function of the relative contributions of the different sources of stratospheric water vapour such as methane oxidation and transport through the tropical tropopause.

3 Discussion. For a more quantitative interpretation of the Odin/SMR measurements, the accuracy of the

H2O, HDO, and H2O-18 data has to be determined, which is a function of various instrumental (calibration accuracy, antenna and sideband suppression knowledge) and spectroscopic uncertainties. Most critical spectroscopic errors are for example the pressure broadening parameters of the target lines, which will have to be determined by laboratory experiments.

3 Discussion. For a more quantitative interpretation of the Odin/SMR measurements, the accuracy of the

H2O, HDO, and H2O-18 data has to be determined, which is a function of various instrumental (calibration accuracy, antenna and sideband suppression knowledge) and spectroscopic uncertainties. Most critical spectroscopic errors are for example the pressure broadening parameters of the target lines, which will have to be determined by laboratory experiments.

29-30 April 2002 29-30 April 2002 26-27 October 200226-27 October 2002

H2O

H2O

HD

OH

DO

δD (

HD

O)

δD (

HD

O)

H2O

-18

H2O

-18

δ18O

(H

2O-1

8)δ18

O (

H2O

-18)

2-d H2O-18 - 489.1 GHz. A H2O-18 line is measured

simultaneously with H2O. The single-profile precision is in the order of 20-30 % ( 3 ppbv) and the altitude resolution is 3-4 km. Information is obtained between approximately 20 and 60 km.

2-d H2O-18 - 489.1 GHz. A H2O-18 line is measured

simultaneously with H2O. The single-profile precision is in the order of 20-30 % ( 3 ppbv) and the altitude resolution is 3-4 km. Information is obtained between approximately 20 and 60 km.

2-e δ18O (H2O-18). Chemical and physical isotope

fractionation also affects the isotopic ratio of 18O/16O in stratospheric water vapour. The Figures show observed zonal mean variations of δ18O = { ([H2O-18]/[H2O-16] - R0) / R0 } × 100 [%].

2-e δ18O (H2O-18). Chemical and physical isotope

fractionation also affects the isotopic ratio of 18O/16O in stratospheric water vapour. The Figures show observed zonal mean variations of δ18O = { ([H2O-18]/[H2O-16] - R0) / R0 } × 100 [%].