10_deep_circulation

10_deep_circulation - DeepOceanCirculation GS222 Lecture10

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Deep Ocean Circulation GS222 Lecture 10
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Overview - this lecture Driving force of deep ocean circulation Deep water formation and upwelling Conservative tracers (temperature and salinity) Temperature and salinity diagrams
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Deep ocean circulation Density and pressure gradients drive circulation in the  deep ocean density = mass/volume once density of surface water is greater than  water below, sinking occurs water will reach a density equilibrium level and  spread horizontally, in response to gradients in  pressure Density-driven circulation often called thermohaline  (thermo – heat, haline – salt) Wind-driven currents dominate ocean circulation in  the near-surface H L
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Seawater density and sigma-t σ t = [ ρ (T,S,P) – 1 ] * 1000 Density varies as a function of temperature, salinity, and pressure σ t (sigma-t) is shorthand for ρ (density) and eliminates the unnecessary digits e.g. σ t =(1.025 g cm -3 – 1) * 1000 = 25
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Will warm, low latitude water be more or less dense than  cold, high latitude water? Why is low latitude surface water warmer than high  latitude surface water?
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Seawater density vs. Temp. Freshwater density = 1.0 g/cm 3 Seawater density ~ 1.028 g/cm 3
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27 water depth Low Latitude At low latitudes, there is a well- developed pycnocline (zone of rapid change in density with water depth). σ
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10_deep_circulation - DeepOceanCirculation GS222 Lecture10

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