Download Flood Routing 2 Flood Wave Movement

Flood Routing 2
Review of Energy Conservation
Energy Grade Line
Gradually Varied Flows, Head Loss
Runge-Kutta Routing
Review of Conservation of Energy
• Conservation of energy says you can’t create
energy or destroy it. You can only shuffle it
around into various places. You can store
energy as:
• --mechanical energy (energy of motion)
• --potential energy (energy of position)
• --molecular energy (pressure)
• --chemical energy
• --heat
Components for incompressible, frictionless water
• Movement (kinetic) energy:
• Potential (height)energy:
• where h is the height above some reference
elevation and M is the mass.
• Pressure (P) has units of force per unit area. It
is a measure of the molecular energy. To give it
units of energy , multiply by a unit volume, v. Discussion: work
Bernoulli Equation
• So, if we ignore heat (friction), we can make
an expression for conservation of energy:
• The total energy doesn’t change from place 1
to place 2, although it may change form.
• We assumed no heat changes due to friction,
and water is incompressible
Alternate forms of Bernoulli
• Mass is an extensive property, its value depends
on the amount of matter. Instead divide mass M
by the unit volume v to get the density r of the
fluid:
• Density is an intensive property, i.e. it doesn’t
depend on the amount of matter present.
• Now we have Cons. of Energy per unit volume.
Alternative forms of Bernoulli 2
• Water is incompressible, so the fluid density ρ
is a constant, and gravity acceleration g is a
constant. Define another constant gamma, as
γ = ρg . Divide by γ = ρg and rewrite the
equation:
Units are now depth, and each term is called head, a height.
Energy Head
• In fluid dynamics, energy head is a concept that
relates the energy in an incompressible fluid to the
height of an equivalent static column of that fluid.
From Bernoulli's Principle, the total energy at a
given point in a fluid is the energy associated with
the movement of the fluid, plus energy from
pressure in the fluid, plus energy from the height of
the fluid relative to an arbitrary datum.
Energy heights in Hydrology - Pressure
• Energy head is expressed in units of height such as meters or
feet. What is the physical meaning of this height? For the
pressure term, It’s the height to which pressurized water
would rise in a well. Remember, the water isn’t moving.
• Pressure as weight (a force) of water above per unit area
Energy lengths in Hydrology – movement
• For the Kinetic Energy velocity head, it’s the
height the water would rise to — if it hit a
vertical wall—the faster the water is moving,
the higher it will rise.
1/2 rV2
P
Pitot (left)and static pressure gages
Energy lengths in Hydrology
height
• The Potential Energy elevation head is the
difference in height from one place to some
datum.
• We often divide the elevation head into two pieces, the
elevation of the channel bottom above some datum
(maybe sea level, for example) z, and the depth of the
water, d. h just equals z + d.
Open Channels
• In unconfined flows (open channel flows), water
is open to the sky.
• There can be no large pressure differences
between one section of the stream and another,
so we can be rid of the pressure term. With
potential energy head h divided into depth d
and height above datum z, Bernoulli becomes:
Energy Grade Line
• The constant “height” that all of these things reach, a
measure of the total energy in the system is called the
energy grade line (EGL). Up to now, it has been horizontal,
meaning that no energy has left the system. However, we
haven’t dealt with another form of energy—heat.
Example: h = d + z decreases, velocity increases
Frictional Head Losses
• Energy is being lost as heat because the flowing water
comes in contact with the channel sides, causing friction.
This lost energy is called frictional head loss hf. It results in
the energy grade line having a slight (always negative)
slope.
upstream
downstream
Detention Basin Routing
• The amount of outflow from a detention basin
depends on the height of the water, as you recall
from Homework 1 and your test. The greater the
depth portion of elevation head, the faster the water
flows out of the spillway with velocity V2.
• Potential Energy at the reservoir surface is converted
to Kinetic Energy of motion in water released to the
atmosphere at the outlet spillway.
Notice the pressure is the same, atmospheric, at 1 & 2
Also the mass dropping at 1 is the mass leaving at 2
So V2 is square root of 2gh
Detention Basin Routing
• Consider some reservoir or lake. We’d like to
know how inflow flood water will be
attenuated during its passage through the
reservoir. The method starts by stating the
same continuity equation we’re used to:
where H is the head in the reservoir. For standing water
(like in a reservoir) H is just the depth.
solve top equation for dS, subs in bottom left,
divide both sides by A(H)
The Storage Function and STAGE
• The storage S in the reservoir is some
measured function of the depth H and the
area A, and the change in storage with depth
is:
Combining this with
yields
This is a differential equation
Mult both sides by
Dt, subs D for d
Finite Difference Methods
• From here, we can do the same finite differencing
technique we did for the Muskingum method, and:
•
where A(Hn) is the surface area for a particular
depth H. This is the form we use when we convert
from flow rate, say cfs, to depth, say inches.
First Order Method
Calculate
deriv=slope project
line to t n+1
Because each differential equation for reservoir storage is made of different curve fits,
we usually couldn’t solve the actual differential equation exactly. Instead we use Numerical Methods.
• In a first-order (Euler) solution, a finite
increment Dt is chosen,
a slope is projected,
• and Hn is known so
• This method has large error if Dt is large.
Second Order Method
•
•
•
•
Step 1: Calculate First order estimate DH1,
Step 2: use DH1 to estimate DH2 (eqn. lower left)
Step 3: use average of DH1 and DH2 for DH
Step 4: Hn+1 = Hn + DH
Notice Step 1 uses the slope at tN
The Step 2 line to get DH2 is the slope
at t N+1 projected back to tN
Fourth-order Runge-Kutta Methods
• Runge-Kutta methods follow the same
reasoning with more steps. The equation is:
• and
We look up I(t) in our input hydrograph, and we calculate O(H) and A(H)from a curve fit
• The constants k are iterative evaluations of
f(t,H).
I at this time, O at this H, A at this H
An Example
• As usual we’ll go through an example, then
you will do a similar homework problem.
• For simplicity, we will look at problems with
straight sides, so Area doesn’t change with
height