Metadata for preliminary data visualizations from cruise FK150117 The numerical simulations were preformed with the Coupled-mode Shallow Water Model (CSW; Kelly et al. 2016). The simulations have 4 vertical modes and a 1/20 degree grid, which extends from 140-172 E and 35-60 S. They employ satellite derived bathymetry (topex.ucsd.edu/marine_top/) and surface tides (TPXO; volkov.oce.orst.edu/tides/global.html). Stratification and background currents are derived from publicly available global simulations using the Hybrid Coordinate Ocean Model (HYCOM.org). The data comprises eight 30-h repeat CTD stations occupied by the R/V Falkor. And a mooring that was deployed for two months by the R/V Revelle. The mooring and data analysis were funded by an NSF Physical Oceanography grant. The data collected include temperature, salinity, and horizontal currents. The data were processed using the methods of Nash et al. (2005). Kelly et al. (2016), A Coupled-mode Shallow Water model for tidal analysis: Internal-tide reflection and refraction by the Gulf Stream, J. Phys. Oceanogr., submitted. Nash et al. (2005), Estimating Internal Wave Energy Fluxes in the Ocean, J. Atmos. Ocean. Tech., 22, pp 1551-1570. Captions for the figures are: CSW_amp_phse.png: A regional numerical model of the M2 (12.4 h period) internal tide in the Tasman Sea displays the amplitude and phase of the sea surface height. The phase may be interpreted as the time of high tide. The amplitude is shown as a sea surface displacement, because it can be directly compared with satellite observations. However, the internal tide primarily produces internal vertical displacements of the thermocline. E.g., a 1 cm surface displacement roughly corresponds to a 100 m displacement of the thermocline, which occurs at around 1000 m depth. The colored circles represent the observed amplitude and phase from each observational station. The variability in observed amplitude partially arises because of natural variability (not included in the model) and uncertainties in the measurements. Analysis of these data are ongoing. CSW_flux_v1.png: A regional numerical model of the M2 (12.4 h period) internal tide in the Tasman Sea displays the regions of internal tide generation and their energy flux. Along the Macquarie ridge, southwest of New Zealand, tidal flow over abrupt topography leads to displacements in the thermocline, which radiate away as internal waves. The regions of strongest/weakest wave generation are denoted by red/blue patches. As these internal waves propagate away from their generation region, they carry energy, which is quantified by their energy flux. The energy flux arrows have an amplitude of about 5 kW/m and point toward Tasmania. The observed energy fluxes (green arrows) have similar amplitude and direction. CSW_ridge_v1.png: The Macquarie Ridge, which extends southwest of New Zealand, is an underwater mountain range slightly taller than the rocky mountains. Where surface (traditional) tides flow over a series of peaks they generate internal waves. The hot regions in this figure show the peaks responsible for most of the internal wave generation. CSW_rms_v1.png: As the internal tide propagates across the Tasman Sea, it is swept back and forth by random background currents associated with large-scale eddies. As a result, the the internal tide's high tide, may occur slightly earlier or later than expected in some locations. In an effort to quantify this effect, a regional tide model was run with background currents from a 1/12 degree global model (HYCOM). The currents produced a 0.2 cm uncertainty in the internal tide predictions. This uncertainty did not decrease when small-scale background currents were removed, suggesting most uncertainty comes from large eddies that are more than 100 km across. As expected, a control simulation without background currents produced very small uncertainties (i.e., the internal tide always arrived at the same time).