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Wave Hydrodynamics
.
Beach Terminology
The inner shelf is a friction-dominated realm where
surface and bottom boundary layers overlap.
(From Nitrouer, C.A. and Wright, L.D., Rev. Geophys., 32, 85, 1994. With permission.)
Conceptual diagram illustrating physical transport
processes on the inner shelf.
(From Nitrouer, C.A. and Wright, L.D., Rev. Geophys., 32, 85, 1994. With permission.)
Ocean Waves
Ocean waves may be classified by the generating force
(wind, seismic events, or gravitational pull of the moon),
the restoring force, (surface tension, gravity, the earth’s
rotation), or the frequency of the waves.
Idealized Ocean Wave Spectrum
Wind Waves
A wind wave is
generated by the
friction of the wind
over the water’s
surface.
As the wind blows over the surface of the water, friction and pressure
differences create small ripples in the water surface.
The wind pushes on the back side of the wave and pulls on the front,
transferring energy and momentum to the water.
As the wind continues to transfer momentum to the water, the wave
becomes higher.
Wave Growth
The area where wind waves are form and grow
is called the generation area.
Higher wind speeds mean more momentum to transfer to the water,
resulting in higher waves.
Duration is the length of time the wind is blowing. The longer the
wind blows, the higher the waves and more chaotic the seas.
The heights of the waves in the generation area are determined by three
factors: wind speed, duration, and fetch.
Fetch
Fetch is the horizontal distance that the wind blows across
the water.
Fetch is important in the early stages of wave formation, and will
control how large the wave will be at a given time.
Swell
As deep-water waves depart the generation area,
they disperse with the long waves travel faster. This sorting by wave speed creates long regular wave patterns
called swell.
Shoaling Waves
As a wave shoals (approaches the shoreline) the wave period
remains constant, causing the wavelength to decrease and the
wave height to increase.
Friction slows the bottom of the wave to while the top continues
at the same speed, causing the wave to tip forward.
When H/L, the
ratio of the wave
height to
wavelength,
reaches the
critical value of
1/7, the wave
breaks.
SEAS
Waves under the influence of
winds in a generating area
SWELL
Waves moved away from the
generating area and no longer
influenced by winds
SMALL AMPLITUDE/FIRST
ORDER/AIRY WAVE THEORY
1. Fluid is homogenous and incompressible, therefore, the density is a constant.
2. Surface tension is neglected.
3. Coriolis effect is neglected.
4. Pressure at the free surface is uniform and constant.
5. Fluid is ideal (lacks viscosity).
SMALL AMPLITUDE/FIRST
ORDER/AIRY WAVE THEORY
6. The wave does not interact with any other water motion.
7. The bed is a horizontal, fixed, impermeable boundary which implies that the vertical velocity at the bed is zero.
8. The wave amplitude is small and the wave form is invariant in time and space.
9. Waves are plane or low crested (two dimensional).
Can accept 1, 2, and 3
and relax assumptions 4-9
for most practical solutions.
WAVE CHARACTERISTICS
T = WAVE PERIOD
Time taken for two successive crests to pass a given
point in space
Definition of Terms
ELEMENTARY, SINUSOIDAL,
PROGRESSIVE WAVE
h=eta
WAVE CELERITY, LENGTH,
AND PERIOD
PHASE VELOCITY/WAVE CELERITY:
(C) speed at which
a waveform moves.
Relating wavelength and H2O depth to celerity, then
Since C = L/T, then is
NOTE: L exists on
both sides of the
equation.
DEEP WATER:
Since:
Then:
Here, Since:
Then:
When d/L >0.5 =
DEEP WATER
1. Longer waves travel faster than shorter waves.
2. Small increases in T are associated with large increases in L.
Long waves (swell) move fast and lose little energy.
Short wave moves slower and loses most energy
before reaching a distant coast.
MOTION IN A SURFACE WAVE
Local Fluid Velocities and Accelerations
(VERTICAL)
(HORIZONTAL)
Water particle displacements from mean position for
shallow-water and deepwater waves.
As waves approach a shoreline the water shallows and they change
from deepwater to transitional waves.
As water shallows the waves steepen and finally break to form surf
which surges towards the shoreline.
When surf reaches the beach it rushes up the beach face as swash
and then runs back down the slope as backwash.
Swash and backwash moves sediment up and down the beach face.
SUMMARY OF LINEAR WAVES
C = Celerity = Length/Time
Relating L (Wavelength) and D (Water Depth)
Since C = L/T, then becomes:
Since C = L/T, then becomes:
PROBLEMS
GIVEN: A wave
with a period T =
10 secs. is
propagated
shoreward from a
depth d = 200m to
a depth d = 3 m.
FIND: C and L at
d = 200m and
d = 3m.
WAVE ENERGY AND POWER
Kinetic + Potential = Total Energy of Wave System
Kinetic: due to H2O particle velocity
Potential: due to part of fluid mass being above trough.
(i.e. wave crest)
WAVE ENERGY FLUX
(Wave Power)
Rate at which
energy is
transmitted in the
direction of
progradation.
Summary of
LINEAR (AIRY) WAVE THEORY:
WAVE CHARACTERISTICS
Regions of validity for various wave theories.
HIGHER ORDER THEORIES
1. Better agreement between theoretical and
observed wave behavior.
2. Useful in calculating mass transport.
HIGHER ORDER WAVES ARE:
• More peaked at the crest.
• Flatter at the trough.
• Distribution is skewed above SWL.
Comparison of second-order Stokes’ profile with linear
profile.
USEFULNESS OF
HIGHER ORDER THEORIES
MASS TRANSPORT VELOCITY = U(2)
The distance
a particle is
displaced
during one
wave period.
NB: Mass transport in the direction of propagation.
HIGHER ORDER WAVES
Stokes
• Takes wave height to 2nd order (H ) and higher
• Useful in higher energy environments
2
2nd order approximate wave profile is:
If H/L is small, then profile can be represented by linear wave theory
For deep H2O – Eq. reduces to:
THIRD ORDER APPROX. (Wave Velocity)
NB. If (H/L) is small, use linear wave theory equation.
TERM: Peaks crests
Flattens troughs
Conforms to shallow H2O wave profile
VELOCITY OF A WAVE GROUP
WAVE GROUP/WAVE TRAIN
Speed not equal to wave travel for individual waves
GROUP SPEED = GROUP VELOCITY (Cg).
INDIVIDUAL WAVE SPEED = Phase velocity or wave
celerity.
Waves in DEEP or TRANSITIONAL WATER
In SHALLOW WATER
K = .4085376 YT = 1.065959
Keulegan and Patterson (1940) Cnoidal Wave Theory
SI Units (m) Wave Height = .25 Wave Period = 2 WaterDepth = 1.1
Deep Water Length = 6.24 Present Length = 3.757897 Elliptical Modulus = .4085376
Net Onshore Displacement Umass = Mass Transport Velocity
Time U(T) UMassSediment
Transport
Airy Wave Theory LO = 6.24 L = 5.783304
T = 2s
H = 0.25m
D = 1.5m
NB. Umass
Symmetry
Time U(T) UMassSediment
Transport
Airy Wave Theory LO = 6.24 L = 5.363072
T = 2s
H = 0.25m
D = 1.1m
Depth at which C.T.
took place
44
Deformasi Gelombang
• Breaking
• Refraction
• Diffraction
• Reflection
45
Refraction
• Waves travel more slowly in shallow water
(shallower than the wave base).
• This is called refraction
• This causes the wave front to bend so it is more
parallel to shore.
• It focuses wave energy on headlands.
46
Wave Refraction
Eu
rop
ean
Coas
t, 1
99
6
Orthogonal
Surf / Breaker
Zone
Beach
47
Wave Refraction
Seabed contour
Wave Crest
Path of crests diverge
and minimize impact of
waves on shore
Seabed contour
Wave crest
Path of crests converge and maximize
impact of waves on shore
Shallow
Deep
48
Long shore Transport
49
Wave Diffraction
50Orthogonal Wave Crest
Orthogonal
Energy Transfer
Wave Diffraction
Breakwater
Hi
Hd
r
L
b
q
Shadow Zone
Wave Diffraction
Diffraction
Coeficient
( K’ )
K’ = Hd / Hi
K’ = f (r/L, b,
q)
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Refleksi Gelombang
Eu
rop
ean
Coas
t, 1
99
6
52
Refleksi Gelombang
Untuk dinding vertikal, kedap air, dgn elevasi diatas muka air, hampir seluruh energi akan dipantulkan kembali ke laut.
Hanya sebagian saja energi yang dipantulkan jika gelombang menjalar di pantai yang agak landai
Refleksi tergantung pada kelandaian pantai, kekasaran dasar laut, porositas dinding, dan Angka Irribarren (Ir) :
tanr
i
o
IH
L
Kr = Hr / Hi
Kr = fungsi (a,
n, P, Ir)
53
Perbedaan Gelombang
WAVES – BREAKING
Dean and Dalrymple, 2002
o
o
LH
b
tan5.0
3.35.0
3.3
Suntoyo
Hp. 081230988146
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