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Figure 6. Hovmiller diagram of (a) composite SSH anomalies and (b) composite SST anomalies for lags —20 to 80 relative to phase 1 of the MJO, averaged between 2 and 4°N and 2 and 4°S for November—April. The shading interval is as shown in the legends in cm and °C, respectively. In (b), the total surface heat flux is contoured at 12 Wm”, the negative contour is dashed, and the zero contour is omitted. The solid diagonal lines represent the propagation of the downwelling Rossby wave in (a). This figure is available in colour online at www.interscience.wiley.com/journal/qj

Figure 6 Hovmiller diagram of (a) composite SSH anomalies and (b) composite SST anomalies for lags —20 to 80 relative to phase 1 of the MJO, averaged between 2 and 4°N and 2 and 4°S for November—April. The shading interval is as shown in the legends in cm and °C, respectively. In (b), the total surface heat flux is contoured at 12 Wm”, the negative contour is dashed, and the zero contour is omitted. The solid diagonal lines represent the propagation of the downwelling Rossby wave in (a). This figure is available in colour online at www.interscience.wiley.com/journal/qj

Related Figures (8)

Figure 1. Composite anomalies of sea surface height for phase 8 lag0. The contour and shading interval is 1 cm. Regions where the anomalies are not significant at the 95% level are masked such that only significant anomalies are visible. OLR is plotted as thick contours at +10Wm’; the negative contour is dashed. This composite passes the field significance test at the 95% confidence level. This figure is available in colour online at www. interscience.wiley.com/journal/qj
Figure 1. Composite anomalies of sea surface height for phase 8 lag0. The contour and shading interval is 1 cm. Regions where the anomalies are not significant at the 95% level are masked such that only significant anomalies are visible. OLR is plotted as thick contours at +10Wm’; the negative contour is dashed. This composite passes the field significance test at the 95% confidence level. This figure is available in colour online at www. interscience.wiley.com/journal/qj
Figure 2. Composite anomalies of sea surface height (cm) for (a) phase 2 lagO and (b) phase2 lag20d in the tropical Pacific. The shading and contour intervals are shown in the legend. Regions where the anomalies are not significant at the 95% level are hatched over such that only significant anomalies are clearly visible. Surface winds are plotted where either the u- or v-component is significant at the 95% confidence level; a scale vector of 1.5ms~! is shown. All composites pass the field significance test at the 95% confidence level. This figure is available in colour online at www.interscience.wiley.com/journal/qj
Figure 2. Composite anomalies of sea surface height (cm) for (a) phase 2 lagO and (b) phase2 lag20d in the tropical Pacific. The shading and contour intervals are shown in the legend. Regions where the anomalies are not significant at the 95% level are hatched over such that only significant anomalies are clearly visible. Surface winds are plotted where either the u- or v-component is significant at the 95% confidence level; a scale vector of 1.5ms~! is shown. All composites pass the field significance test at the 95% confidence level. This figure is available in colour online at www.interscience.wiley.com/journal/qj
Figure 3. Composite anomalies of (a) sea surface height (b) sea surface temperature for phase 3 lag 0 of the MJO in the tropical Atlantic. The shading and contour interval is (a) 0.3. cm and (b) 0.1 °C. Surface winds are plotted where either the u- or v-component is significant at the 95% confidence level; a scale vector of 1.5ms~! is shown. Regions where the anomalies are not significant at the 95% level are hatched over such that only significant anomalies are clearly visible. OLR is plotted as thick contours at +10 W m~’; the negative contour is dashed. All composites pass the field significance test at the 95% confidence level. This figure is available in colour online at www. interscience.wiley.com/journal/qj
Figure 3. Composite anomalies of (a) sea surface height (b) sea surface temperature for phase 3 lag 0 of the MJO in the tropical Atlantic. The shading and contour interval is (a) 0.3. cm and (b) 0.1 °C. Surface winds are plotted where either the u- or v-component is significant at the 95% confidence level; a scale vector of 1.5ms~! is shown. Regions where the anomalies are not significant at the 95% level are hatched over such that only significant anomalies are clearly visible. OLR is plotted as thick contours at +10 W m~’; the negative contour is dashed. All composites pass the field significance test at the 95% confidence level. This figure is available in colour online at www. interscience.wiley.com/journal/qj
Figure 4. Composite anomalies of sea surface height for all eight phases of the MJO. The contour and shading interval is 1 cm. Regions where the anomalies are not significant at the 95% level are hatched over such that only significant anomalies are clearly visible. Surface winds are plotted where either the u- or v-component is significant at the 95% confidence level; a scale vector of 1.5ms~! is shown. OLR is plotted as thick contours at +10 W m~”; the negative contour is dashed. All composites pass the field significance test at the 95% confidence level. This figure is available in colour online at www.interscience.wiley.com/journal/qj
Figure 4. Composite anomalies of sea surface height for all eight phases of the MJO. The contour and shading interval is 1 cm. Regions where the anomalies are not significant at the 95% level are hatched over such that only significant anomalies are clearly visible. Surface winds are plotted where either the u- or v-component is significant at the 95% confidence level; a scale vector of 1.5ms~! is shown. OLR is plotted as thick contours at +10 W m~”; the negative contour is dashed. All composites pass the field significance test at the 95% confidence level. This figure is available in colour online at www.interscience.wiley.com/journal/qj
Figure 7. Hovmiller diagram of OLR anomalies for lags —20 to 80 relative to phase 1 of the MJO, for (a) November—April and (b) May—October. The contour and shading interval is shown in the legend (in W m~”). The solid diagonal lines represent the propagation of the downwelling Rossby waves in (a) November—April and (b) May—October. This figure is available in colour online at www.interscience.wiley.com/journal/qj
Figure 7. Hovmiller diagram of OLR anomalies for lags —20 to 80 relative to phase 1 of the MJO, for (a) November—April and (b) May—October. The contour and shading interval is shown in the legend (in W m~”). The solid diagonal lines represent the propagation of the downwelling Rossby waves in (a) November—April and (b) May—October. This figure is available in colour online at www.interscience.wiley.com/journal/qj
Figure 8. As Figure 6, but for May—October. This figure is available in colour online at www.interscience.wiley.com/journal/q,
Figure 8. As Figure 6, but for May—October. This figure is available in colour online at www.interscience.wiley.com/journal/q,
Figure 9. Schematic of MJO dynamical ocean feedback mechanism. This figure is available in colour online at www.interscience.wiley.com/journal/qj Our results imply that, to accurately model the MJO, the ocean dynamics may need to be simulated adequately enough to resolve the Kelvin and Rossby waves as well as the SST anomalies forced by these waves. Achieving this may resolve some of the current difficulties with modelling the MJO (Inness and Slingo, 2003). The significance of the i dynamical response has implications for the circulation, chemistry and biology of the tropical oceans. Further work is necessary to investigate such matters, in addition to determining the strength of the feedback onto the MJO. It is hoped that this paper has highlighted the importance of these questions, the answers to which may help improve our understanding of the coupled MJO system. oscillation and synoptic-scale variability over the warm pool. J. Climate 18: 2004-2020.
Figure 9. Schematic of MJO dynamical ocean feedback mechanism. This figure is available in colour online at www.interscience.wiley.com/journal/qj Our results imply that, to accurately model the MJO, the ocean dynamics may need to be simulated adequately enough to resolve the Kelvin and Rossby waves as well as the SST anomalies forced by these waves. Achieving this may resolve some of the current difficulties with modelling the MJO (Inness and Slingo, 2003). The significance of the i dynamical response has implications for the circulation, chemistry and biology of the tropical oceans. Further work is necessary to investigate such matters, in addition to determining the strength of the feedback onto the MJO. It is hoped that this paper has highlighted the importance of these questions, the answers to which may help improve our understanding of the coupled MJO system. oscillation and synoptic-scale variability over the warm pool. J. Climate 18: 2004-2020.
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OceanographyAtmospheric sciencesMadden Julian Oscillation
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