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28 Cards in this Set
- Front
- Back
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Heat budget |
Qt = Qs - (Qb + Qe + Qh) + Qz |
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Wien's and Stefan Boltzman |
lambda = b/k Wien: wavelength = inversely proportional to temperature Qb = ck^4 SB: Qb (back radiation) is temp^4 |
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Qh and Qe |
Qh = rhoA*Cs* Cd*U10 Sensible heat: rho air, specific heat air, bulk Latent heat: rho air, latent heat of vapor, bulk Qe = rhoA*Le*Cl*U10 VERY HARD |
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heat content |
H^ = Cw*rho*deltaT specific heat of water = 4186 j/kgºc |
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heat flux |
Qt = (H^*h)/t h = height of mixed layer |
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Continuity |
0 = 1/rho* DP/Dt + du/dx + dv/dy + dw/dz mass + volume |
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langrangian (following flow ) |
DP/Dt = drho/dt + u*drho/dx + v*drho/dy + w*drho/dz
local term plus advective |
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depth averaged continuity |
hdu = dn/dt surface height of water* x velocity = change that was replaced below (waves) |
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Ficks law; spatially changing |
Fc = -Kc*dc/dx ; stuff moving back and forth F^2c/dt = -Kc*d^2c/dx^2 ; as stuff moves, speed of stuff moves
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conservation of tracers (molecular)
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dS/dt = -uds/dx ... +kc *d^2S/dx^2 ...
advection terms, diffusivity terms |
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conservation of tracers (turbulent) |
dS/dt = -uds/dx... d/dx*Az*dS/dz vertical more important than horizontal can't pull out coefficient; turbidity may change |
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Basin equations |
Cons of volume: Vi + R +P = E + Vo Tres = vol/flux in Cons of salt: ViSiRhoi = VoSoRhoo |
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Hydrostatic balance |
dP/dz = -rhoG P = rho*g*n(h) |
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speeds of 2 horizontal pressure gradients |
SS slope du/dt = -gS/L : accel = -g*elevaton/distance its over
du/dt = -g (rho2 - rho1)h/rho*L |
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equation of motion (5)
(force balance on rotating earth) |
x: drho/dt + u*drho/dx + v*drho/dy + w*drho/dz - FV = -1/pdP/dx + mol & d/dx*Az*du/dz
y = +FU
z = no coriolis, -g on right side
cons volume
cons of mass: continuity = diffusivity
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reynolds number |
udu/dx: Kc*du/dx: U^2/L: Kc U/L^2 Re = UL/V
v = turbidity of substance, water = 10^-6 advection vs molecular small number means molecular important |
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rossby number |
udu/dx : fv: U^2/L:FU Ro = U/fL
advective to coriolis; large for turbulence to matter; (only when small L or very fast U)
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Ekman |
fv: d/dz*Az*du/dz; fU: Az*U/H^2 Ek = Kz/fH^2 coriolis to turbulence terms ~ 1
advection only important in shallow depths |
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geostrophic balance |
-fv = -1/rho*dP/dx; - fv = -g*dn/dx; fv = g*S/L
all that's left is coriolis and pressure; coriolis dependent on slope of sea (height over distance) |
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internal oscillation |
d^2u/dt^2 = -f^2 sine/cos
sea spontaneously started by wave |
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coriolis parameter |
f = 2omegasin (lat) ~ 10^-4 |
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wind stress |
Tx = PaCdU10
linearly decrease in speed with depth w/otu coriolis with coriolis integrated transport 90ºR
vertical change in geostrophic speed from horizontal change in density |
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geostrophic shear |
f*dv/dz = -g/rho*drho/x forget this horizontal density changes lead to vertical geostrophic speed changes
NH: if density decreases eastward, speed increases northward |
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tidal driven estuary flow |
du/dt = -g*dn/dx +Az d^2u/dz^2
accel = slope of surface + turbulent gradient (Friction) |
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subtidal estuary flow |
barotropic + baroclinic = turbulent friction gdn/dx - g/rho*dp/dx*Z = Az d^2u/dz2 |
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strength of estuary density stratification (strength of river input) |
udS/dx = Kz d^2S/dz^2
velocity *mixing = strength of river input |
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potential vorticity |
PV = (f + relative)/H |
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relative vorticity |
dv/dx - du/dy |
