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**Dynamics III: Earth rotation L. Talley SIO 210 Fall, 2014**

Earth reference frame Geoid Rotation definitions Centrifugal force Coriolis force Inertial motion READING: DPO: Chapter 7.2.3, 7.5.1 Stewart chapter 7.6, 9.1 Tomczak and Godfrey chapter 3, pages 29-35 Talley SIO 210 (2014)

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**The Earth as a reference frame**

Coordinate system for most oceanography: Local Cartesian (x,y,z), ignoring sphericity West-east (“zonal”) x –direction (positive eastwards) South-north (“meridional”) y-direction (positive northwards) Down-up (“vertical”) z-direction (positive upwards) Add diagram Talley SIO 210 (2014)

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**An aside on the Earth’s reference frame for pressure: the geoid**

When we calculate horizontal pressure gradients, they are relative to a “level” surface along which the pressure gradient vanishes (no force, no motion) Earth’s mass is not distributed evenly AND Earth is not a perfect ellipsoid. That is, the “level” surface is not locally “flat”. The surface of constant pressure, i.e. along which the gravitational force has no changes, is the “geoid” Good geoid site Talley SIO 210 (2014)

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Geoid Earth’s mass is not distributed evenly AND Earth is not a perfect ellipsoid 200 meter variation Geoid map using EGM96 data, from Talley SIO 210 (2014)

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Geoid Earth’s mass is not distributed evenly AND Earth is not a perfect ellipsoid Talley SIO 210 (2014)

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Rotating coordinates The Earth is rotating. We measure things relative to this “rotating reference frame”. Quantity that tells how fast something is rotating: Angular speed or angular velocity = angle/second 360° is the whole circle, but express angle in radians (2 radians = 360°) For Earth: 2 / 1 day = 2 / 86,400 sec = x 10-4 /sec Also can show = v/R where v is the measured velocity and R is the radius to the axis of rotation (therefore v = R) At home: calculate speed you are traveling through space if you are at the equator (radius of earth is about 6371 km), then calculate it at 30N as well. (Do some geometry to figure out the distance from the axis at 30N.) At home: calculate speed you are traveling through space if you are at the equator (radius of earth is about 6371 km), then calculate it at 30N as well. (Do some geometry to figure out the distance from the axis at 30N.) R Talley SIO 210 (2014)

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**Rotating coordinates R**

Vector that expresses direction of rotation and how fast it is rotating: vector pointing in direction of thumb using right-hand rule, curling fingers in direction of rotation R Talley SIO 210 (2014)

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**Centripetal and Centrifugal forces**

(now looking straight down on the rotating plane) Centripetal force is the actual force that keeps the ball “tethered” (here it is the string, but it can be gravitational force) Centrifugal force is the pseudo-force (apparent force) that one feels due to lack of awareness that the coordinate system is rotating or curving centrifugal acceleration = 2R (outward) (Units of m/sec2) Talley SIO 210 (2014)

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**Effect of centrifugal force on ocean and earth**

Centrifugal force acts on the ocean and earth. It is pointed outward away from the rotation axis. Therefore it is maximum at the equator (maximum radius from axis) and minimum at the poles (0 radius). = x 10-4 /sec At the equator, R ~ 6380 km so 2R = .032 m/s2 Compare with gravity = 9.8 m/s2 Centrifugal force should cause the equator to be deflected (0.032/9.8) x 6380 km = 21 km outward compared with the poles. (i.e. about 0.3%) A = 6000 km; omega = 2pi/86400 sec = 7.292e10-4/sec Omega2 a cos(latitude) = 3.17 cm/sec2 x cos(latitude) Compare 3.17 with gravity of 980 cm/sec2 Earth surface should be 0.3% farther out at equator = 20 km Talley SIO 210 (2014)

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**Effect of centrifugal force on ocean and earth**

Radius: Equatorial 6, km Polar 6, km Mean 6, km (From wikipedia entry on Earth) The ocean is not 20 km deeper at the equator, rather the earth itself is deformed! We bury the centrifugal force term in the gravity term (which we can call “effective gravity”), and ignore it henceforth. Calculations that require a precise gravity term should use subroutines that account for its latitudinal dependence. Return here – need to state that at the equator, centrigufal force reduces the effective gravity the most Talley SIO 210 (2014)

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Coriolis effect Inertial motion: motion in a straight line relative to the fixed stars Coriolis effect: apparent deflection of that inertially moving body just due to the rotation of you, the observer. Coriolis effect deflects bodies (water parcels, air parcels) to the right in the northern hemisphere and to the left in the southern hemisphere add this reference and animations Talley SIO 210 (2014)

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**Coriolis effect look on youtube for countless animations**

add this reference and animations Talley SIO 210 (2014)

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Coriolis force Additional terms in x, y momentum equations, at latitude horizontal motion is much greater than vertical) x-momentum equation: -sinv = -f v y-momentum equation: sinu = f u f = sinis the “Coriolis parameter”. It depends on latitude (projection of total Earth rotation on local vertical) Talley SIO 210 (2014)

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**Coriolis force f = sinis the “Coriolis parameter”**

= 1.414x10-4/sec At equator (=0, sin=0): f = 0 At 30°N (=30°, sin=0.5): f = 0.707x10-4/sec At north pole (=90°, sin=1): f = 1.414x10-4/sec At 30°S (=-30°, sin=-0.5): f = x10-4/sec At north pole (=-90°, sin=-1): f = x10-4/sec Edited 11/3/14 Talley SIO 210 (2014)

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**Complete force (momentum) balance with rotation**

Three equations: Horizontal (x) (west-east) acceleration + advection + Coriolis = pressure gradient force + viscous term Horizontal (y) (south-north) Vertical (z) (down-up) acceleration +advection (+ neglected very small Coriolis) = pressure gradient force + effective gravity (including centrifugal force) + viscous term Full equations in words Talley SIO 210 (2014)

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**Final equations of motion (momentum equations in Cartesian coordinates)**

x: u/t + u u/x + v u/y + w u/z - fv = - (1/)p/x + /x(AHu/x) + /y(AHu/y) +/z(AVu/z) (7.11a) y: v/t + u v/x + v v/y + w v/z + fu = - (1/)p/y + /x(AHv/x) + /y(AHv/y) +/z(AVv/z) (7.11b) z: w/t + u w/x + v w/y + w w/z (+ neglected small Coriolis) = - (1/)p/z - g + /x(AHw/x) + /y(AHw/y) +/z(AVw/z) (7.11c) (where g contains both actual g and effect of centrifugal force) Full equations for the physics-based students in class. The class is not responsible for knowing these full equations. The “g” term includes centrifugal force. The neglect of Coriolis in the z-momentum equation is called the “traditional approximation”.. Talley SIO 210 (2014)

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**Coriolis in action in the ocean: Observations of Inertial Currents**

D’Asaro et al. (1995) DPO Fig. 7.4 Surface drifters in the Gulf of Alaska during and after a storm. Note the corkscrews - drifters start off with clockwise motion, which gets weaker as the motion is damped (friction) Talley SIO 210 (2014)

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Inertial currents Balance of Coriolis and acceleration terms: push the water and it turns to the right (NH), in circles. What is the inertial period? Equator => infinite since f = 0 Poles 2pi/f = DPO Fig. S7.8a Talley SIO 210 (2014)

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**Inertial currents: periods**

sin() Coriolis parameter f = 2sin() Inertial period T = 2π/f = latitude Talley SIO 210 (2014)

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**Inertial currents: force balance**

Three APPROXIMATE equations (all other terms are much smaller): Horizontal (x) (west-east) acceleration + Coriolis = 0 Horizontal (y) (south-north) Vertical (z) (down-up) (hydrostatic) (not important for this solution) 0 = pressure gradient force + effective gravity That is: x: u/t - fv = 0 y: v/t + fu = 0 Solution: solve y-eqn for u and substitute in x eqn (or vice versa). Solutions are velocity circles: u = Uosin(ft) and v = Uocos(ft) where Uo is an arbitrary amplitude Equations (bottom) not required for class. Talley SIO 210 (2014)

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**Inertial currents: relation to internal waves**

Energy in inertial oscillations (which are wind-forced) as measured by surface drifters (Elipot et al., JGR 2010) Talley SIO 210 (2014)

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AOSS 321, Winter 2009 Earth System Dynamics Lecture 6 & 7 1/27/2009 1/29/2009 Christiane Jablonowski Eric Hetland cjablono@umich.edu ehetland@umich.edu.

AOSS 321, Winter 2009 Earth System Dynamics Lecture 6 & 7 1/27/2009 1/29/2009 Christiane Jablonowski Eric Hetland cjablono@umich.edu ehetland@umich.edu.

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