Etudes et évaluation de processus océaniques par des hiérarchies ...
Etudes et évaluation de processus océaniques par des hiérarchies ... Etudes et évaluation de processus océaniques par des hiérarchies ...
238 64 CHAPTER 11. SOLUTION OF EXERCISES Exercise 16: (x r ,y r ) = R(cos(ωt), sin(ωt)), (u r ,v r ) = ωR(− sin(ωt), cos(ωt)) ∂ t (u r ,v r ) = −ω 2 R(cos(ωt), sin(ωt)) putting it together: ((−ω 2 R − fωR − f 2 /4R) cos(ωt), (−ω 2 R − fωR − f 2 /4R) sin(ωt)) = 0, which is satisfied if and only if ω = −f/2 Exercise 17: now the centrifugal force is balanced by the slope of the free surface and we have ((−ω 2 R − fωR) cos(ωt), 0 which is satisfied if and only if ω = −f (compare to previous exercise)! Exercise 28: tel-00545911, version 1 - 13 Dec 2010 The potential energy released per unit length (in the transverse direction): E pot = 2 1 2 ρgη2 0 ∫ ∞ 0 (1 − (1 − exp(−x/a)))dx = 3 2 ρgη2 0a. (11.4) The kinetic energy in the equilibrium (final) solution per unit length (in the transverse direction): E kin = 2 1 ∫ ∞ 2 ρHg2 η0(fa) 2 −2 exp(−2x/a)dx = 1 2 ρgη2 0a. (11.5) 0 So energy is NOT conserved during the adjustment process. Indeed waves transport energy from the region where the adjustment occurs to ±∞. Exercise 30: Calculus tells us that: d dt ( ) ζ + f = 1 H + η d (ζ + f) − ζ H + η dt + f d (H + η) 2 dt η. So take ∂ x of eq.(5.39) and substract ∂ y of eq. (5.38) to obtain: After some algebra one obtains: and eq. (5.40) gives ∂ t ∂ x v +∂ x (u∂ x v) + ∂ x (v∂ v v) + f∂ x u + g∂ xy η −∂ t ∂ y u −∂ y (u∂ x u) − ∂ y (v∂ v u) + f∂ y v − g∂ xy η = 0. d dt (ζ + f) = −(ζ + f)(∂ xu + ∂ y v), d dt η = −(H + η)(∂ xu + ∂ y v), putting this together gives the conservation of potential vorticity.
239 65 Exercise 32: The moment of inertia is L = Iω = mr 2 /2ω = mρV/(4π)ω/H where we used, that the volume V of a cylinder is given by V = 2πr 2 H. As the mass and the volume are constant during the stretching of flattening process we obtain that conservation of angular momentum implies that ω/H is constant. Exercise 38: The (kinetic) energy is given by: E = α(U 2 + V 2 ), where the constant α = Aρ/(2H) is the horizontal surface area times the density divided by twice the layer thickness. ∂ t E = α(∂ t U 2 + ∂ t V 2 ) = α2(U∂ t U+V ∂ t V ) using eqs. (6.13) and (6.13) we obtain ∂ t E = α(fV U+Uτ x −fUV ) = 0, as the velocity is perpendicular to the forcing, that is, U = 0. tel-00545911, version 1 - 13 Dec 2010 Exercise 41: Summing the first and the third line of the matrix equation gives U 1 + U 2 = 0, summing the second and the fourth line of the matrix equation gives f(V 1 + V 2 ) = τ x . Eliminating U 2 and V 2 in the first and third equation we obtain: ˜rU 1 − fV 1 = τ x fU 1 + ˜rV 1 = (r/f)τ x . with ˜r = r(H 1 + H 2 )/(H 1 H 2 ) solving this equations give: U 1 = rτ x f 2 + ˜r 2 1 H 1 V 1 = − rτ x f 2 + ˜r 2(f r + U 2 = − rτ x f 2 + ˜r 2 1 V 2 = H 1 rτ x ˜r f 2 + ˜r 2 fH 1 ˜r fH 2 )
- Page 193 and 194: 187 3.6. HEAT CAPACITY 13 tel-00545
- Page 195 and 196: 189 3.7. CONSERVATIVE PROPERTIES 15
- Page 197 and 198: 191 Chapter 4 Surface fluxes, the f
- Page 199 and 200: 193 4.2. FRESH WATER FLUX 19 water.
- Page 201 and 202: 195 Chapter 5 Dynamics of the Ocean
- Page 203 and 204: 197 5.2. THE LINEARIZED ONE DIMENSI
- Page 205 and 206: 199 5.4. TWO DIMENSIONAL STATIONARY
- Page 207 and 208: 201 5.6. THE CORIOLIS FORCE 27 Whic
- Page 209 and 210: 203 5.8. GEOSTROPHIC EQUILIBRIUM 29
- Page 211 and 212: 205 5.10. LINEAR POTENTIAL VORTICIT
- Page 213 and 214: 207 5.13. A FEW WORDS ABOUT WAVES 3
- Page 215 and 216: 209 Chapter 6 Gyre Circulation tel-
- Page 217 and 218: 211 6.1. SVERDRUP DYNAMICS IN THE S
- Page 219 and 220: 213 6.2. THE EKMAN LAYER 39 In the
- Page 221 and 222: 215 6.3. SVERDRUP DYNAMICS IN THE S
- Page 223 and 224: 217 Chapter 7 Multi-Layer Ocean dyn
- Page 225 and 226: 219 7.3. GEOSTROPHY IN A MULTI-LAYE
- Page 227 and 228: 221 7.5. EDDIES, BAROCLINIC INSTABI
- Page 229 and 230: 223 Chapter 8 Equatorial Dynamics t
- Page 231 and 232: 225 Chapter 9 Abyssal and Overturni
- Page 233 and 234: 227 9.2. MULTIPLE EQUILIBRIA OF THE
- Page 235 and 236: 229 9.3. WHAT DRIVES THE THERMOHALI
- Page 237 and 238: 231 Chapter 10 Penetration of Surfa
- Page 239 and 240: 233 10.2. TURBULENT TRANSPORT 59 If
- Page 241 and 242: 235 10.5. ENTRAINMENT 61 instabilit
- Page 243: 237 Chapter 11 Solution of Exercise
- Page 247 and 248: 241 INDEX 67 Transport stream-funct
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239<br />
65<br />
Exercise 32:<br />
The moment of inertia is L = Iω = mr 2 /2ω = mρV/(4π)ω/H where we used, that the volume<br />
V of a cylin<strong>de</strong>r is given by V = 2πr 2 H. As the mass and the volume are constant during the<br />
str<strong>et</strong>ching of flattening process we obtain that conservation of angular momentum implies that<br />
ω/H is constant.<br />
Exercise 38:<br />
The (kin<strong>et</strong>ic) energy is given by: E = α(U 2 + V 2 ), where the constant α = Aρ/(2H) is the<br />
horizontal surface area times the <strong>de</strong>nsity divi<strong>de</strong>d by twice the layer thickness. ∂ t E = α(∂ t U 2 +<br />
∂ t V 2 ) = α2(U∂ t U+V ∂ t V ) using eqs. (6.13) and (6.13) we obtain ∂ t E = α(fV U+Uτ x −fUV ) =<br />
0, as the velocity is perpendicular to the forcing, that is, U = 0.<br />
tel-00545911, version 1 - 13 Dec 2010<br />
Exercise 41:<br />
Summing the first and the third line of the matrix equation gives U 1 + U 2 = 0, summing the<br />
second and the fourth line of the matrix equation gives f(V 1 + V 2 ) = τ x . Eliminating U 2 and<br />
V 2 in the first and third equation we obtain:<br />
˜rU 1 − fV 1 = τ x<br />
fU 1 + ˜rV 1 = (r/f)τ x .<br />
with ˜r = r(H 1 + H 2 )/(H 1 H 2 ) solving this equations give:<br />
U 1 =<br />
rτ x<br />
f 2 + ˜r 2 1<br />
H 1<br />
V 1 = − rτ x<br />
f 2 + ˜r 2(f r +<br />
U 2 = − rτ x<br />
f 2 + ˜r 2 1<br />
V 2 =<br />
H 1<br />
rτ x ˜r<br />
f 2 + ˜r 2 fH 1<br />
˜r<br />
fH 2<br />
)