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Climate Dynamics

Climate Dynamics. 2011/01/10 R98229014 馮培寧 Kirsten Feng. Decadal Variability of the Kuroshio Extension: Observations and an Eddy-Resolving Model Hindcast. BUNMEI TAGUCHI , SHANG-PING XIE , NIKLAS SCHNEIDER , MASAMI NONAKA , HIDEHARU SASAKI , AND YOSHIKAZU SASAI.

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Climate Dynamics

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  1. Climate Dynamics 2011/01/10 R98229014 馮培寧 Kirsten Feng

  2. Decadal Variability of the Kuroshio Extension: Observations and an Eddy-Resolving Model Hindcast BUNMEI TAGUCHI, SHANG-PING XIE, NIKLAS SCHNEIDER, MASAMI NONAKA, HIDEHARU SASAKI, AND YOSHIKAZU SASAI In final form 17 October 2006

  3. Model and Data • Eddy-resolving model • Multidecadalhindcast by the OGCM for the Earth Simulator (OFES) • Domain: • 75°S to 75°N • 0.1°x0.1°x54(levels) • Condition: • NCEP–NCAR reanalysis • This paper: • (1950 spinup)1962-2003 • 28°N~45°N, 140°E~180°E • Observation • SSH: • Ocean Topography Experiment (TOPEX)/ Poseidon (T/P) • European Remote Sensing satellite (ERS-1/2) altimeter observations • Monthly Ocean Temperature: • expendable bathythermograph (XBT) • 1995~2004 • 2° lat x 5°lon

  4. Method Examines the spatiotemporal structure/ Determines this structure/ BaroclinicRossbywave Large- versus frontal-scale variability Intrinsic variability OGCM, Linear Rossby Wave Model are added here. • Variance • Leading mode and comparison with satellite altimetry • The KE jet’s signature in modal structure • Multidecadalanalysis • Recirculation variability

  5. Variance • Although the OFES simulation misses some variance, the overall agreement of the mean and interannual variance with observations encourages to look further.

  6. Leading mode and comparison with satellite altimetry

  7. The KE jet’s signature in modal structure • 2D EOF for each section. • The front gets southward and broader from its upstream to downstream. • EOF1 shows a clear dependency with the mean flow.

  8. Multidecadal analysis • The first mode primarily represents the north–south shift of the KE jet. • The second mode represents an intensification of the KE jet. PC-1 corresponds well with the zonal mean of the KE’s latitudinal position determined as the maximum u velocity at 100 m.  PC-2 tracks very well the SSH difference, the latitudinal band for the KE jet core.

  9. BaroclinicRossby wave • The linear Rossby wave model captures the temporal evolution of the OFES’s leading modes very well except a 1–2-yr phase lag behind the OFES PC-2. • The meridional structure of the Rossby wave solution, however, is quite different from that of the OFES hindcast. • The linearRossby wave models fail to reproduce the narrow modal structure as OFES and observation but display a rather broad meridional structure reflecting large-scale wind forcing. OGCM: Xie et al., 2000

  10. Large- versus frontal-scale variability • (c) = (b) –(a). • The broadscale component of the difference field in OFES represents the spinup of both the subtropical and subpolar gyres, in broad agreement with the linear Rossby wave model. (R=0.67) • The small, frontal-scale component of the SSH difference features zonally elongated, meridonally tight recirculations along the mean fronts.

  11. Broad scale Low-passed PC-2 Frontal scale West: positive East: negative The negative SSH from the east extends in to the west and replace the positive SSH at lag -6yr. The positive SSH in the east is growing and arrive to the Japanese coast (west boundary) at lag 6yr. A pair of zonally elongated recirculations with the KE front in between. This pair of anomalous recirculations alters the sign from lag 6 to 0, and again from lag 0 to 6 yr. The frontal-scale recirculation adjustments to the large-scale environmental changes are initiated by the arrival of Rossby waves.

  12. Intrinsic variability • The leading EOF modes of frontal-scale variability in the hindcast bear a remarkable resemblance to those in the climatological run. • The second EOF that differs in phase near the Oyashio Extension north of 39°N, presumably due to the difference in the mean flow structures. • The two sets of PCs are nearly identical, and it suggests the following scenario: basin-scale wind variability excites broadscaleRossby waves, which propagate westward, triggering intrinsic modes of the KE jet and reorganizing SSH variability in space.

  13. Prediction Experiment • The slow propagation of baroclinicRossby waves is a source of predictability. • The resultant time series (blue curve) closely follows the OFES hindcast as well as T/P observations for up to 9 months. • This simulation allows the prediction of the meridional position and intensity of the KE front.

  14. Summary • The first mode represents a southward shift and to a lesser degree, an acceleration of the KE jet in the early 1980s that separates two periods. • The second EOF mode represents intensity variations in the KE jet and displays quasi-decadal oscillations. • The broadscale component indeed resembles the linear Rossby wave response to wind variability while the frontal-scale variability bears a remarkable similarity to intrinsic modes of the climatological run in spatial structure. • Basin-scale wind variability excites broadscaleRossby waves, which propagate westward, triggering intrinsic modes of the KE jet and reorganizing SSH variability in space.

  15. Thank You

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