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G. Hirst and . Aken, North Pacific Subtropical 40 Water, NPSW, black curve box 1 (Figure 1)), through the 41 Sulawesi Sea and the Makassar Strait, and exits through the 42 Lombok and Ombai Straits and through the Timor Passage 43 (Figure 1) [Gordon and Fine About 90% of the ITF 44 thermocline water flows through this main route with an 45 estimated transport of 10 ± 5 Sv (1 Sv = 10 6 m 3 /s) The second route advects subthermocline water of 47 South Pacific origin through the Maluku Sea and the 48 Lifamatola Strait It has a transport of $1.5?3 Sv [Va n 49 South Pacific waters 143 depends on the specificities of internal-tide generation and 144 thus can vary strongly from one region to another In order 145 to determine the vertical distribution of internal tides (and 146 hence that of their induced dissipation and mixing), an 147 internal-tide generation model was 148 applied to several vertical sections in the most important 149 straits of the ITF. The model involves a 3D velocity field, 150 but assumes full uniformity in the along-slope direction. 151 The forcing mechanism involves three ingredients which 152 need to be prescribed: the barotropic cross-slope flux, the 153 topographic profile (uniformity is assumed in the along- 154 slope direction), and the buoyancy frequency N(z) The 155 model is linear and hydrostatic, in the horizontal cross- 156 slope direction a fourth-order central-difference scheme is 157 used (resolution of 400 m), in the vertical a Chebyshev 158 collocation method is used involving 60 polynomials. Time- 159 integration is done using a third-order Adams-Bashforth 160 scheme. We start from rest and carry out a calculation over 161 20 tidal periods; by the end, all transients have left the 162 domain of interest, and have been absorbed by sponge 163 layers placed at the outer ends. 164 [13] The bathymetry was inferred from the TOPEX data- 165 set (http://topex.ucsd.edu/cgi-bin/get_data.cgi) Buoyancy 166 frequency is set from observations and the barotropic 167 cross-slope flux is arbitrarily prescribed to a constant value. 168 The two dominant tidal components, M2 and K1, are used 169 separately. An example of the spatial distribution of the tidal 226 It uses the latest version of the NEMO/OPA Ocean 227 General Circulation model (G. Madec, NEMO = the OPA9 228 ocean engine, note du pole de modelisation The model has a 0.25° horizontal reso- 231 lution with eddy resolving capabilities which is a good 232 compromise between CPU consumption and complex 233 strait configuration. The vertical grid has 46 levels, with 234 a resolution ranging from 5 m at the surface to 250 m 235 at the bottom. Partial step for bathymetry modeling has 236 been implemented. The background vertical diffusivity is 237 0.1 cm 2 /s. The domain extends from 95°E to 145°Ei n 238 longitude and from 25°St o2 5 °N in latitude. Open bound- 239 ary conditions are provided by the reference simulation 240 ORCA025, 31 1. Introduction 32 [2] The Indonesian Throughflow (ITF) is the only low- 33 latitude passage between two oceans. Due to its strategic 34 position, it plays an important role in the global ocean and 35 climate regulation The model is forced by 241 daily climatological wind stress fields derived weekly from 242 the European Remote Sensing satellites (ERS) during the 243 period 1992 ? 2001. Surface heat fluxes and evaporation are 244 computed with bulk formulas using climatologies from the 245 ERS satellites and the Climate Prediction Center Merged 246 Analysis of Precipitation (NCEP/NCAR) for surface air 247 temperature Two addi- 258 tional experiments were performed in order to isolate the 259 influence of tidal mixing along the western route and the 260 eastern routes: TIDES-E (with tidal mixing parameterization 261 only on the eastern route), TIDES-W (with the tidal mixing 262 parameterization only in the western route), pp.256-257, 1988.

. Seas, Moreover the rest of the salty water from SPSW 387 remains confined in the Seram Sea in good agreement with 388

. Gordongerkema, the vertical distri- 419 bution of the energy dissipation is found to be proportional 420 to N 2 below the core of the thermocline and to N above The 421 model results show a maximum of energy dissipation within 422 the thermocline. The resulting vertical diffusivities vary 423 from a few cm 2 /s to a dozen of cm 2 /s. The vertical 424 diffusivity is constant bellow the core of the thermocline 425 and its average over the semi-enclosed seas is 1.5 cm 2 /s, in 426 good agreement with the independent estimation of Ffield 427 and Gordon [1992], who used an advection diffusion 428 model. This agreement suggests that the tidal energy is a 429 major source of energy to explain the strong transformation 430 of Pacific water mass within the Indonesian archipelago. 431 When applying the parameterization in the 1 = 4 ° OGCM used 432 here, the T-S properties in all the Indonesian basins, are 433 considerably improved and reach a good agreement with in 434 situ observations. This suggests that the spatial distribution 435 of the vertical diffusivity is adequately prescribed and able 436 to reproduce the heterogeneity of the mixing. In particular, 437 20% of the tidal energy is dissipated along the western route 438 and related to the very localized transformation that occurs 439 in the vicinity of the Dewakang Strait. The associated 440 salinity change is relatively modest, but it significantly 441 influences the T-S characteristics at the exits of the archi- 442 pelago as it involves 90% of the flow in the thermocline, 418 vertical section of the Indonesian straits 40% of the tidal energy is concentrated in the 444 Halmahera and Seram Seas where a major improvement of 445 the water mass occurs. Indeed, even if it concerns a minor 446 pathway its impact on the Banda Sea and the Indonesian 447 Throughflow Water T-S characteristics is predominant. 448 [26] Acknowledgments. We thank the DRAKKAR project and in 449 particular Anne-Marie Tréguier for the ITF configuration and data at open 450 boundaries condition. We also thank F. Lyard and the late and regretted 451 C. Le Provost for providing the outputs from the Tidal model. We thank, p.452, 2004.

A. Atmadipoera and M. Lengaigne, This 453 work is supported by MERCATOR-ocean (projects 100043 and 061396) 454 and by the Marine Environement and Security for the European Area 455 project (MERSEA, SIP3 CI The ocean model integrations 456 have been performed at the Institut de Développement et des Ressources en 457 Informatique Scientifique (IDRIS, project 51140 and 1396). P. Bouruet- 458 Aubertot acknowledges the Royal Netherlands Institute for Sea Research 459 for financial support to this collaboration, 2003502885.

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