ETOPO1 Global Relief Model converted to PanMap layer format

Amante, Christopher; Eakins, Barry W.

doi:10.1594/pangaea.769615

Cited by 85 publications

(21 citation statements)

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“…Adjacent to the coast, bathymetry less than 300 m deep, is obtained from the 3 arc sec Coastal Relief Model (http://www.ngdc.noaa.gov/mgg/coastal/crm.html). Deep ocean (depth > 300 m) bathymetry data are obtained from the 1 arc min ETOPO1 Global Relief Model [Amante and Eakins, 2009]. Raw elevation and bathymetry data referenced to different vertical datum are converted to the same vertical coordinate system (NAVD88) using the V-Datum program [Yang et al, 2008].…”

Section: Model Descriptionmentioning

confidence: 99%

Impact of sea level rise on tidal range in Chesapeake and Delaware Bays

2017

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Coastal inundation is affected not only by rising mean sea level but also by changing tides. A numerical model is developed to investigate how sea level rise and coastline changes may impact tides in two coastal‐plain estuaries, Chesapeake Bay and Delaware Bay. Despite their different tidal characteristics, the two estuaries display similar responses to the sea level rise and shoreline management scenarios. When hypothetic sea walls are erected at the present coastline to prevent low‐lying land from flooding, tidal range increases, with greater amplification in the upper part of the two estuaries. When low‐lying land is allowed to become permanently inundated by higher sea level, however, tidal range in both estuaries decreases. Analyses of the tidal energy budget show that the increased dissipation over the shallow water and newly inundated areas compensates for the reduced dissipation in deep water, leading to smaller tidal range. The changes in the tidal range are not proportional to the changes in the mean sea level, indicating a nonlinear tidal response to sea level rise. The ratio of tidal range change to sea level rise varies between −0.05 and 0.1 in Chesapeake Bay and between −0.2 and 0.25 in Delaware Bay. The model results suggest a potential adaptation strategy that uses inundation over low‐lying areas to reduce tidal range at up‐estuary locations.

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Section: Model Descriptionmentioning

confidence: 99%

Impact of sea level rise on tidal range in Chesapeake and Delaware Bays

2017

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“…The thick dashed white line denotes the intraslab aseismic zone. Topography data is retrieved from ETOPO1 Global Relief Model (Amante & Eakins, 2009). Inset map marks the position of our study region.…”

mentioning

confidence: 99%

Impact of the Juan Fernandez Ridge on the Pampean Flat Subduction Inferred From Full Waveform Inversion

Gao

Yuan

Heit

et al. 2021

Geophysical Research Letters

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“…The data were derived from the Archiving, Validation, and Interpretation of Satellite Oceanographic (AVISO) dataset, with a horizontal resolution of 0.258 and temporal resolution of 1 day (Ducet et al 2000). Bathymetry data with 1/608 spatial resolution derived from ETOPO1 (Amante and Eakins 2009) were used for calculating the topographic gradient. The bathymetry data were smoothed with a scale of ∼30 km to remove small topographic variations.…”

Section: Datamentioning

confidence: 99%

Deep-Current Intraseasonal Variability Interpreted as Topographic Rossby Waves and Deep Eddies in the Xisha Islands of the South China Sea

Shu

Wang

Xue

et al. 2022

Journal of Physical Oceanography

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Strong subinertial variability near a seamount at the Xisha Islands in the South China Sea was revealed by mooring observations from January 2017 to January 2018. The intraseasonal deep flows presented two significant frequency bands, with periods of 9–20 days and 30–120 days, corresponding to topographic Rossby waves (TRWs) and deep eddies, respectively. The TRW and deep eddy signals explained approximately 60 % of the kinetic energy of the deep subinertial currents. The TRWs at the Ma, Mb, and Mc moorings had 297, 262, and 274 m vertical trapping lengths, and ∼43, 38, and 55 km wavelengths, respectively. Deep eddies were independent from the upper layer, with the largest temperature anomaly being >0.4°C. The generation of the TRWs was induced by mesoscale perturbations in the upper layer. The interaction between the cyclonic-anticyclonic eddy pair and the seamount topography contributed to the generation of deep eddies. Owing to the potential vorticity conservation, the westward-propagating tilted interface across the eddy pair squeezed the deep-water column, thereby giving rise to negative vorticity west of the seamount. The strong front between the eddy pair induced a northward deep flow, thereby generating a strong horizontal velocity shear because of lateral friction and enhanced negative vorticity. Approximately four years of observations further confirmed the high occurrence of TRWs and deep eddies. TRWs and deep eddies might be crucial for deep mixing near rough topographies by transferring mesoscale energy to small scales.

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ETOPO1 Global Relief Model converted to PanMap layer format

Cited by 85 publications

References 0 publications

Impact of sea level rise on tidal range in Chesapeake and Delaware Bays

Impact of sea level rise on tidal range in Chesapeake and Delaware Bays

Impact of the Juan Fernandez Ridge on the Pampean Flat Subduction Inferred From Full Waveform Inversion

Deep-Current Intraseasonal Variability Interpreted as Topographic Rossby Waves and Deep Eddies in the Xisha Islands of the South China Sea

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