Advanced Fluid Dynamics of The Environment- a Thin Fluid Layer Flowing Down an Incline

3 Pages·0.04 MB·English

by  Chiang C. Mei

1
Lecture Notes on Fluid Dynamics
(1.63J/2.21J)
by Chiang C. Mei, MIT
CHAPTER 2: LOW VISCOUS FLOWS
2-1-thinlayer.tex
Because of the inherent nonlinearity, most (cid:13)uid-dynamical problems must be solved by ei-
ther analytical approximations or by numerical computations. In this chapter we shall (cid:12)rst
explain the lubrication approximation, with applications to the (cid:13)ow of thin layers. Atten-
tion will then be turned to the slow (cid:13)ow past a sphere and a cylinder. Application to the
environmental pblem of aerols will be brie(cid:13)y discussed. Lastly the slow withdrawl of (cid:13)uid
from a straiti(cid:12)ed reservoir into a sink will be analyzed.
2.1 A thin (cid:13)uid layer (cid:13)owing down an incline
As our (cid:12)rst example, we consider the (cid:13)ow of a thin layer ofviscous (cid:13)uid on an inclined plane.
Referring to Figure 2.1.1, let the x(cid:0) axis coincide with the plane bed inclined at the angle
(cid:18) with respect to the horizon, and the y(cid:0) axis normal to the plane bed,
Figure 2.1.1: A thin (cid:13)uid layer (cid:13)owing down an incline plane
2.1.1 Exact equations
Continuity :
@u @v
+ = 0 (2.1.1)
@x @y
Momentum :
@u @u @u 1@p @2u @2u
+u +v = gsin(cid:18)(cid:0) +(cid:23) + (2.1.2)
@t @x @y (cid:26)@x @x2 @y2
!
and
@v @v @v 1@p @2v @2v
+u +v = (cid:0)gcos(cid:18)(cid:0) +(cid:23) + (2.1.3)
@t @x @y (cid:26)@y @x2 @y2
!
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2.1.2 Exact boundary conditions
On the rigid bottom no slipping is allowed,
u = v = 0; y = 0: (2.1.4)
The top of the (cid:13)uid layer of local depth h(x;t) is a material surface whose position is un-
known until the problem is solved. It is necessary to specify a kinematic boundary condition
concerning the motion, and two dynamic conditions concerning the stresses.
Kinematic condtion:
Since the top is a material surface,it must be always composed of the same (cid:13)uid particles.
The (cid:13)uid velocity must be tangential to the moving surface at all times. Let us describe the
top surface by
F(~x;t) = F(x;y;t) (cid:17) y(cid:0)h(x;t) = 0 (2.1.5)
Consider a surface point which is at ~x at time t, then it will move to ~x+q~ dt at time t+dt
s
where dt is a very short time interval and q~ is the velocity of the surface point. The new
s
top surface is then described by
F(~x+q~dt;t+dt) = 0
s
Taylor-expanding for small dt, we get
@F(~x;t)
2
F(~x;t)+dt +q~ (cid:1)rF(~x;t) +O(dt) = 0
s
@t
!
The (cid:12)rst term vanishes because of (2.1.5), hence
@F(~x;t)
+q~ (cid:1)rF(~x;t) = 0
s
@t
in the limit of dt = 0. Now the unit normal to the surface is
rF(~x;t)
~n =
jrF(~x;t)j
and the normal component of the surface velocity is q~ (cid:1)~n. Since the normal velocity of a
s
(cid:13)uid particle q~ on the surface must be equal to the normal velocity of the surface at the
same point,
q~ (cid:1)rF(~x;t) q~(cid:1)rF(~x;t)
s
=
jrF(~x;t)j jrF(~x;t)j
it follows that
@F(~x;t)
+~q (cid:1)rF(~x;t) = 0 (2.1.6)
@t
This is the kinematic bounday conditon on the top (cid:13)uid surface. Substituting F = y (cid:0)
h(x;t) = 0 we get the kinematic boundary condition.
@h @h
+u = v; y = h(x;t) (2.1.7)
@t @x
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Dynamic boundary conditions
Let the free surface be stress-free:
(cid:6) = ((cid:0)p(cid:14) +(cid:28) )n = 0; i = 1;2: (2.1.8)
i ij ij j
or
(cid:6)1 = (cid:0)pn1 +(cid:28)11n1 +(cid:28)12n2 = 0 (2.1.9)
(cid:6)2 = (cid:0)pn2 +(cid:28)21n1 +(cid:28)22n2 = 0: (2.1.10)
on y = h. The unit normal vector has the components:
@h 1
n1 = (cid:0) @x ; n2 = (2.1.11)
2 2
1+ @h 1+ @h
@x @x
r r
(cid:16) (cid:17) (cid:16) (cid:17)
So far these exact boundary conditions are highly nonlinear, in part because the position
for applying these conditions are not known. As an useful consequence of (2.1.7) to be used
later, we integrate the continuity equation in depth, to get, after invoking Leibnitz’s rule
h @u @v @ h @h
+ dz = udx(cid:0)u(x;h;t) +v(x;h(x;t);t) = 0
0 @x @z! @x 0 @x
Z Z
With the help of (2.1.7), we get the depth-integrated law of mass conservation,
@h @ h @h @Q @h @(uh)
+ udx = + = + = 0 (2.1.12)
@t @x 0 ! @t @x @t @x
Z
where Q denotes the rate of volume discharge and u the depth averaged horizontal velocity
Q 1 h
u = = udy (2.1.13)
h h 0
Z