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UpperUpper--Ocean Processes Ocean Processes and Airand Air--Sea Interaction in Sea Interaction in the Indonesian Seasthe Indonesian Seas
Janet Sprintall, Janet Sprintall, Scripps Institution of Oceanography, USAScripps Institution of Oceanography, USA
Arnold L. Gordon, Asmi M. Napitu, Arnold L. Gordon, Asmi M. Napitu, LDEO, USALDEO, USA
Ariane KochAriane Koch--LarrouyLarrouy, LEGOS, France, LEGOS, France
Susan E. WijffelsSusan E. Wijffels, CSIRO, Australia, CSIRO, Australia
the Indonesian Seas and the Indonesian Seas and ThroughflowThroughflow (ITF)(ITF)
• the only tropical inter-ocean exchange site (~15 Sv)• transports heat and freshwater from Pacific into Indian Ocean• pressure gradient between Pacific (high) and Indian Ocean (low) (Wyrtki, 1987)• ascending branch of Walker Circulation• closely coupled to the Australasian Monsoon system, MJO, ENSO and IOD• extends across Indo-Pacific warm pool • many many islands, deep basins, wide and shallow marginal seas• mixing from strong tides and enhanced air-sea heat and freshwater fluxes
• the only tropical inter-ocean exchange site (~15 Sv)• transports heat and freshwater from Pacific into Indian Ocean• pressure gradient between Pacific (high) and Indian Ocean (low) (Wyrtki, 1987)• ascending branch of Walker Circulation• closely coupled to the Australasian Monsoon system, MJO, ENSO and IOD• extends across Indo-Pacific warm pool • many many islands, deep basins, wide and shallow marginal seas• mixing from strong tides and enhanced air-sea heat and freshwater fluxes
Strong Mixing
Koch-Larrouy et al. (2007)Sprintall et al., (2014)
Signatures of theSmax in the thermocline and Smin in the Intermediate layer disappear quickly in the Indonesian seas through vigorous mixing from tides, air-sea interaction and complexbathymetry to form cool and fresh Indonesian Seas Water masses
Regional T-S Plots (color coded by depth)
Processes that Drive SST Variability
Kida and Richards, JGR, 2009Kida and Wijffels, JGR, 2012
February
August
SE Monsoon: Wind driven upwelling and Arafura shelf-break cools SST
NW Monsoon: Also large P -> high R/O warms SST by limiting latent heat release & mixing. Freshwater caps trap heat in near surface
Annual SST: Monsoon driven upwelling not the whole story!
Seasonal SST: Role of the ITF in Summer
Kida and Wijffels, JGR, 2012
Standard Deviation Note weak seasonality in Flores Sea. What other processes are important to SST here?
Flores Sea: Control NO-ITF
Heat balance shows in austral summer, lateral advection warms SST while vertical mixing and Q cools SST, i.e the ITF impacts SST by advection of warm water
Resolving Mixing is Important
Models that include tides can reproduce the rainfall (Δ20%), SST (Δ2oC) and heat flux (Δ20 Wm-2) patterns observed in the Indonesian Seas than those without
Koch-Larrouy et al (2010)Kida and Wijffels (2012) Jochem and Potemra (2008)Sprintall et al. (2014)
Annual SST and precipitation differences in coupled simulations with/without tides
OLR (Rainfall)
Intraseasonal SST
Largest intraseasonal SST variance (55-60%) found in Banda Sea, Timor Sea, and in the Sulawesi Sea.
Napitu, Gordon and Pujiana, submitted, 2014
Contribution of intraseasonal variability to total SST variance
Intraseasonal SSTCoherence of SST and OLR at intraseasonal timescales.
Highest amplitude in Banda Sea and Timor Sea
OLR leads SST by 1-2 weeks
Napitu, Gordon and Pujiana, submitted, 2014
Mixing Impact on Intraseasonal OLR
Koch-Larrouy et al (in prep)
Std dev OLR bandpass filtered (30-1d)
OBS
CTL
TIDES
Coupled model with tidal parameterization reduced intraseasonal variability in good agreement with observations
Indo-Pacific MJO Surface Forcing
Drushka, Sprintall, Gille and Wijffels, J. Climate, 2012
OLR U-WND STRESS Qo MJO Composites (Nov-Apr) based on Wheeler and Hendon (2004) Index
Active MJO phase convective cells (OLR<0) lead strong westerly wind anomalies in Indian Ocean (esp. IAB in phases 5-7) but are more aligned in Pacific, and so have different impacts on the SST and mixed layer.
Variations in Q (QLH) more closely follow wind stress magnitude
MLD Response to MJO Forcing
Drushka, Sprintall, Gille and Wijffels, J. Climate, 2012
MLD MLD-T • Argo data MLD amplitudes ~ 10 m• Largest signal in IAB ~0.6C• No profiles available in Indonesian
seas
• Spatial patterns resemble t and Q• Active MJO: diabatic cooling &
wind stirring cause MLD deepening and cooling
• Suppressed MJO: Surface warming and light winds lead to MLD shoaling and warming
• MLD-T lags Q by one phase, i.e., consistent with model that Q drives MLD-T
Barrier Layer (BL) Influence on MJO
Drushka, Sprintall and Gille, JGR, 2014
THIN BL THICKHeat Flux
Precip
Wind Stress
Zonal V
Temperature
•Thin BL:- 15% stronger heat flux and wind stress; 10% stronger P; higher MLD-T; deeper isothermal layer
•Thick BL:- entrainment cooling during MJO reduced so MJO drives weaker SST anomaly
•Modulation of SST by BL thickness can have significant consequences for response of ocean to MJO and in turn, the feedbacks of ocean to atmosphere on MJO time scales
Summary
• SST and upper ocean characteristics in the Indonesian Seas are the product of several competing processes (both atmospheric and oceanic driven) over many time scales
• Response may be to local (winds, tides, inertial waves, air-sea interaction) and remote (Kelvin waves) forcing
• Mixing is important! The efficiency of mixing processes depends on stratification, bathymetry and the background oceanic and atmospheric large-scale conditions that vary across the Indonesian seas.
Few Direct Observations of Mixing in Indonesian Seas
shear
strain
dissipation rate
diapycnal diffusivity
• Near-inertial phase lines evident in shear and strain, leading to pulses of mixing every 4.4 days, the wave period
• Turbulence mixing occurs when low Ri=N2/S2 (base of MLD)
• At time of observations, local winds were light -> down-ward propagating internal wave likely generated 3 weeks prior and ~200 km away.
Alford and Gregg, JGR, 2001
Direct measure of vertical mixing : INDOMIX
CTDIndirectOverturnThorpe method
AboveStraits
Banda SeaFar field
Nearfield
VMPdirectDissipationMeasurement
Koch-Larrouy, Atmadipoera, van Beek, Madec, Aucan, Lyard, Grelet, and Souhart, submitted DSR, 2015
Discussion Issues• Mixing Processes:
– Where does mixing occur? At what depths? Seasonal preference?• Impact of the ITF advection stream on SST and air-sea interaction
– if ITF absent or significantly reduced, may enhance the zonal SST gradient• Shallow versus Deep Basins?• Precipitation and presence of barrier layer?
– Large P -> high R/O warms SST by limiting latent heat release & mixing. Also freshwater caps can trap heat in near surface
– Presence of a barrier layer may significantly affect SST anomalies. • SST gradients in response to MJO forcing
– zonal SST gradient in response to seasonal migration across Indonesia and its atmospheric convective activity (convective limit at SST ~27.5C)
• Diurnal variability in SST and surface layer?• Strong vs. Weak Wind scenarios?• Regional variability within Indonesian Seas? EEZ Issues? Use of ROV?• What is the impact on biology? Ecosystem/fisheries interest and also might
feedback via solar absorption to SST• Need in situ SST and MLD observations within Indonesian Seas to validate
remotely sensed data and model output
MJO Driven Deep Vertical Motions
Drushka, Sprintall and Gille, JGR, 2014
MJO composite dT/dz at thermocline depth shows eastward propagation of 0.5C anomaly along the equator at speed of ~2 m/s consistent with Kelvin wave speed (and slower than 5 m/s propagation speed of MJO)
Nov-Apr Mean T along equator
T Anomaly at Thermocline Depth
ITF: Influence on CirculationITF: Influence on Circulation
Song, Gordon and Visbeck, JGR, 2004
• ITF cools and freshensthrough mixing in the Indonesian Seas and also the Indian Ocean thermocline [on isopycnals] relative to the ambient thermocline. cool
Low salinity
ITF
Temperature on sigma-0 = 25.0, upper thermocline
Salinity on sigma-0 = 25.0, upper thermocline
freshwater input
IndonesianMix-Master
Seasonal SST: The role of Mixing
Kida and Wijffels, JGR, 2012
SST(CTRL-NO_TIDE)
Annual
February
SST(NOWind-NOWindTide)
February
• Along shelf-break- enhanced bottom mixing lifts the thermocline and enables intrusion of thermocline water onshore.• Shallow seas -water column well mixed so vertical mixing does not result in enhanced cooling.
North Nusa Tenggara: well mixed thermocline water from Makassar intrudes below and upwells to cool SST in NW monsoon. NE Ekman flow advects this to Banda Sea.
MJO Driven MLD Heat Budgets
Drushka, Sprintall, Gille and Wijffels, J. Climate, 2012
dT/dt Q Horadv Vertent• Mixed layer temperature variations
driven by anomalous Q• Central I.O. rapid deepening of
MLD during onset of active MJO induces entrainment cooling
• No entrainment cooling in WPAC despite MLD deepening is related to barrier layer (water below MLD is same T and so no net cooling).
• Using a fixed MLD overestimates heat budget by 40% during active MJO (i.e. using a slab MLD will overestimate the T changes forced by MJO -> important consideration for models simulating MJO temperature and air-sea interaction associated with MJO
• Large error bars!• Event to event variation!
Barrier Layers Influence SST
Drushka, Sprintall and Gille, JGR, 2014
THIN BL
THICK BL
Difference
• MJO composite surface temperature anomalies are stronger when BL is thin
• Modulation of SST by BLT can have significant consequences for response of ocean to MJO and feedbacks of ocean to atmosphere on MJO time scales