Editorial Type:
Article
Article Type:
Research Article

Tracking Down the ENSO Delayed Oscillator with an Adjoint OGCM

Geert Jan van Oldenborgh KNMI, De Bilt, the Netherlands

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Gerrit Burgers KNMI, De Bilt, the Netherlands

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Stephan Venzke Max-Planck Institut für Meteorologie, Hamburg, Germany

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Christian Eckert Max-Planck Institut für Meteorologie, Hamburg, Germany

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Ralf Giering Department of Earth, Atmospheric, and Planetary Sciences, Massachusetts Institute of Technology, Cambridge, Massachusetts

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Print Publication:
01 Jul 1999
DOI:
https://doi.org/10.1175/1520-0493(1999)127<1477:TDTEDO>2.0.CO;2
Page(s):
1477–1496
Restricted access

Abstract

According to the delayed-oscillator picture of ENSO, a positive SST anomaly in the eastern tropical Pacific will cause westerly wind anomalies closer to the date line to first give a positive feedback, and later, via planetary wave reflection at the western boundary, a negative feedback. The aim of this study is to follow a chain of sensitivities that lead to a delayed-oscillator mechanism in a general circulation model. To this end, the adjoint of such an ocean model is used for studying sensitivities of ENSO indices.

The ocean model used in this study is the Hamburg Ocean Primitive Equation (HOPE) ocean general circulation model. Its adjoint has been constructed using the Adjoint Model Compiler. Applied to a scalar function computed with a forward model run, an adjoint run goes back in time and calculates sensitivities as the derivatives of this function to forcing fields or ocean state variables at earlier times.

Results from six adjoint runs are reported, tracing the sensitivities of the NINO3 and NINO3.4 indices in October 1987, December 1987, and December 1988, as simulated by a Pacfic-only version of HOPE forced by ECHAM-3 fluxes.

The sensitivities to sea level can be followed back in time for more than a year. They are nonlocal: patterns propagate back in time that are identified as adjoint Kelvin and n = 1, 2, and 3 Rossby waves, with speeds compatible with those obtained from model density profiles. Both the first and the second baroclinic modes seem to play a role. In contrast, the model sensitivities to heat flux, zonal surface currents, and SST are local and decay in about a month.

The sensitivities to the wind stress agree with the wave interpretation of the sea-level sensitivities, but only the n = 1 Rossby wave is visible. Going back in time, the sensitivity to westerly anomalies along the equator changes sign, in agreement with the delayed-oscillator picture.

Finally, a statistical atmosphere model is used to convert sensitivities to wind stress at a given time to sensitivities to SST through the atmosphere at that time. Focusing on the sensitivities to the ENSO index region itself at an earlier time then closes the circle. These sensitivities have a natural interpretation as delayed-oscillator coefficients and show the expected behavior of a positive sensitivity in the recent past changing to a negative sensitivity at longer lags. However, the strength of these feedbacks, and hence the relevance of this mechanism in ENSO simulated in HOPE, cannot be determined accurately.

Corresponding author address: Dr. Geert Jan van Oldenborgh, KNMI, KS/OO, P.O. Box 201, NL-3730 AE De Bilt, the Netherlands.

Email: oldenbor@knmi.nl

Abstract

According to the delayed-oscillator picture of ENSO, a positive SST anomaly in the eastern tropical Pacific will cause westerly wind anomalies closer to the date line to first give a positive feedback, and later, via planetary wave reflection at the western boundary, a negative feedback. The aim of this study is to follow a chain of sensitivities that lead to a delayed-oscillator mechanism in a general circulation model. To this end, the adjoint of such an ocean model is used for studying sensitivities of ENSO indices.

The ocean model used in this study is the Hamburg Ocean Primitive Equation (HOPE) ocean general circulation model. Its adjoint has been constructed using the Adjoint Model Compiler. Applied to a scalar function computed with a forward model run, an adjoint run goes back in time and calculates sensitivities as the derivatives of this function to forcing fields or ocean state variables at earlier times.

Results from six adjoint runs are reported, tracing the sensitivities of the NINO3 and NINO3.4 indices in October 1987, December 1987, and December 1988, as simulated by a Pacfic-only version of HOPE forced by ECHAM-3 fluxes.

The sensitivities to sea level can be followed back in time for more than a year. They are nonlocal: patterns propagate back in time that are identified as adjoint Kelvin and n = 1, 2, and 3 Rossby waves, with speeds compatible with those obtained from model density profiles. Both the first and the second baroclinic modes seem to play a role. In contrast, the model sensitivities to heat flux, zonal surface currents, and SST are local and decay in about a month.

The sensitivities to the wind stress agree with the wave interpretation of the sea-level sensitivities, but only the n = 1 Rossby wave is visible. Going back in time, the sensitivity to westerly anomalies along the equator changes sign, in agreement with the delayed-oscillator picture.

Finally, a statistical atmosphere model is used to convert sensitivities to wind stress at a given time to sensitivities to SST through the atmosphere at that time. Focusing on the sensitivities to the ENSO index region itself at an earlier time then closes the circle. These sensitivities have a natural interpretation as delayed-oscillator coefficients and show the expected behavior of a positive sensitivity in the recent past changing to a negative sensitivity at longer lags. However, the strength of these feedbacks, and hence the relevance of this mechanism in ENSO simulated in HOPE, cannot be determined accurately.

Corresponding author address: Dr. Geert Jan van Oldenborgh, KNMI, KS/OO, P.O. Box 201, NL-3730 AE De Bilt, the Netherlands.

Email: oldenbor@knmi.nl

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