nats 101 lecture 12 newton’s laws of motion upper-air maps and winds
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NATS 101 Lecture 12 Newton’s Laws of Motion Upper-Air Maps and Winds. Isobaric Maps. Weather maps at upper levels are analyzed on isobaric (constant pressure) surfaces. (Isobaric surfaces are used for mathematical reasons that are too advanced to include in this course!) - PowerPoint PPT PresentationTRANSCRIPT
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NATS 101
Lecture 12Newton’s Laws of MotionNewton’s Laws of Motion
Upper-Air Maps and WindsUpper-Air Maps and Winds
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Isobaric Maps
• Weather maps at upper levels are analyzed on isobaric (constant pressure) surfaces.(Isobaric surfaces are used for mathematical reasons
that are too advanced to include in this course!)
• Isobaric maps provide the same information as constant height maps, such as:
Low heights on isobaric surfaces correspond to low pressures on constant height surfaces!
Cold temps on isobaric surfaces correspond to cold temperatures on constant height surfaces!
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Isobaric Maps
Ahrens, Fig. 2, p141
504 mb504 mb
496 mb496 mb
PGF
Downhill(Constant height)
Some generalities:
1) High/Low heights on an isobar surface correspond to High/Low pressures on a constant height surface
2) Warm/Cold temps on an isobaric surface correspond to Warm/Cold temps on a constant height surface
3) The PGF on an isobaric surface corresponds to the downhill direction
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Contour Maps
How can we portray undulations of a 3D isobaric surface on a 2D plane without loss of information?
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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Consider the terrain height of an island.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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Denote the shoreline by a line. Labeled the line 0’ for zero feet above mean-sea-level.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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Raise the water level by 500’. Denote the new shoreline by another line. Labeled that line 500’
for five-hundred feet above mean-sea-level.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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Raise the water level by another 500’ to 1,000’. Labeled that line 1000’ for one thousand feet
above mean-sea-level.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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Labeled another line 1500’ above mean-sea-level.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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2000’ above mean-sea-level.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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2500’ above mean-sea-level.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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3000’ above mean-sea-level.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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3500’ above mean-sea-level.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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A 4000’ line is not needed since the island is completely submerged.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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Lower the water level back to 0’. We are left with lines every 500’ at 0’, 500’, 1000’,... above MSL
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/elevation.html
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Rotate to a top-down perspective. We can see the entire island.
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/contourlabel.html
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Extra precision could be of value, but the map starts to get busy.
If lines every 500’ is good, would lines every 250’ be better?
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Contour Maps
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/contourlabel.html
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Contours every 250’; labeled and thickened every 1250’
Map can be clarified by accentuating every few contour lines
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Contour Spacing and Gradient
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/contourspacing.html
Contours every 500’.
Note differences in the steepness of the mountain slopes.
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Contour Spacing and Gradient
http://academic.brooklyn.cuny.edu/geology/leveson/core/linksa/contourspacing.html
Contours every 500’.
Note that tight spacing of contours corresponds to steep slopes.
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Topographic MapGoogle maps
Grand Canyon Village
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570 dam contour570 dam contour
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576 dam contour576 dam contour
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570 and 576 dam contours570 and 576 dam contours
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All contours at All contours at 6 dam spacing6 dam spacing
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All contours at All contours at 6 dam spacing6 dam spacing
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-20 C and –15 C -20 C and –15 C Temp contoursTemp contours
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-20 C, –15 C, -10 C -20 C, –15 C, -10 C Temp contoursTemp contours
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All contours at All contours at 55oo C spacing C spacing
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Height contours Height contours Temps shadedTemps shaded
Region of Region of HighHigh Heights Heights RIDGERIDGE
and and WarmthWarmth
Region of Region of LowLow Heights Heights TROUGHTROUGH
and and ColdCold
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PGF
Wind
Wind doesn’t blow downhill!Wind doesn’t blow downhill!
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Do Rocks Always Roll Downhill?
Gedzelman, p 247
Upper-Level Winds
PGF
Begs the Question….
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The Empirical Evidence Shows
• Wind Direction and PGF Relationship
Winds more than 1 to 2 km above the ground are perpendicular to PGF!
Analogous a marble rolling not downhill, but at a constant elevation with lower altitudes to the left of the marble’s direction
How can we explain observations?
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Why does the wind blow?
To begin the answer to this question we first have to revisit
Sir Isaac Newton
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Newton’s Laws of Motion
• Newton’s 1st LawAn object at rest will remain at rest and an object in motion will remain at a constant velocity (same speed and same direction) if the net force exerted on it is zeroAn external force is required to speed up, slow down, or change the direction of air
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Newton’s Laws of Motion
• Newton’s 2nd LawThe net force exerted on an object equals its mass times its accelerationSum of All Forces = Mass AccelerationAcceleration = Velocity Change / TimeAcceleration = Change in Either Speed
or Direction
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Velocity, Acceleration and Force are Vectors
• Speed/Size Change
Original Velocity
New Velocity Original
Velocity
New Velocity
Acceleration and Force
Original Velocity
Original Velocity
New Velocity
New Velocity
Acceleration and Force
• Direction Change
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Uniform, Circular Motion Requires Acceleration
Original Velocity
New Velocity
Acceleration directed toward center of circle Centripetal
Original Velocity
New Velocity
Circular Path
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CENTRIPETAL CENTRIPETAL FORCEFORCE
You experience acceleration without a change in speed, for example, on a tilt-a-whirl carnival ride.
The force is directed toward the center of the wheel.
An equal an opposite (fictitious) centrifugal force is exerted by the inertia of your body on the wheel—so you stay put and don’t fall off even when upside down.
Important when considering curved flows, as well see later…
CENTRIFUGAL CENTRIFUGAL FORCEFORCE
Centripetal Force
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Newton’s 2nd law can be used to derive a governing equation for atmospheric motion
The simplified form in the horizontal that we’ll consider has four terms. By understanding how each of these terms works, we’ll be able to explain why the
wind blows.
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Simplified equation of horizontal atmospheric motion
(1) (2) (3) (4)
Total Force = 1ρΔpd
+ 2ΩVsinφ+V2
r+ Fr
Term Force Cause
1 Pressure gradient force Spatial differences in pressure
2 Coriolis force Rotation of the Earth
3 Centripetal force Curvature of the flow
4 Friction force Acts against direction of motion due to interaction with surface
FOCUS ON FIRST TWO TODAY…FOCUS ON FIRST TWO TODAY…
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Force BalanceWhat we’re looking for in the equation of motion is the condition where the forces exactly balance—or the sum of the forces is equal to zero.
When this happens, there is no net acceleration and the wind speed is constant, by Newton’s first law.
0 = Pressure gradient force + Coriolis force + Centripetal Force + Friction
0 = Pressure gradient force + Coriolis force Geostrophic Balance
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Pressure gradient force
Definition: Force to the difference in pressure (Δp) over a distance (d). (In the equation ρ is the density of air)
d
pΔρ1
The pressure gradient force is directed perpendicular to lines of constant pressure (isobars), toward lower pressure.
1
ρΔpd
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Strength of the pressure gradient force
How strong the pressure gradient is depends on distance between the areas of high and low pressure, or how close the lines of constant pressure are spaced.
Strong pressure gradient: Isobars are close together
Weak pressure gradient: Isobars are far apart.
WEAK WEAK PRESSURE PRESSURE GRADIENTGRADIENT
STRONG STRONG PRESSUREPRESSUREGRADIENTGRADIENT
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The pressure gradient force is why the wind blows, but you need the other
terms to complete the picture…
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Upper Level Chart for Surface
Arctic Air Outbreak (300-mb)
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PRESSURE PRESSURE GRADIENT AT GRADIENT AT
DENVERDENVER
LOWLOWHIGHHIGH
Observations for upper level winds:
Wind DOES NOT follow the pressure gradient.
Wind runs parallel to the lines of constant height (i.e. isobars).
Strength of the wind IS related to the closeness, or packing, of the isobars.
For example, compare the wind speed at Denver (105 knots) to some of the surrounding upper air observations, like Albuquerque.
NEED AT LEAST ONE OF THE OTHER THREE FACTORS TO ACCOUNT FOR WIND MOTION
DENVERDENVER105 knots105 knots
ALBUQUERQUEALBUQUERQUE90 knots90 knots
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Coriolis Force φsinVΩ2
Definition: Apparent force due to rotation of the Earth (Ω). Depends on the speed (V) and the latitude (Φ).
Causes apparent deflection in reference of an observer at a fixed point on Earth
Gaspard Coriolis
2ΩVsinϕ
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Coriolis force on a merry-go-round
From perspective of person NOT on the merry-go-round, path of ball is straight.
From perspective of person on merry-go-round, path of ball deflects. It accelerates. This is an apparent (fictitious) force.
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Life on a Rotating Platform
• From perspective of person not on merry-go-round, path of ball is straight.
• From perspective of person on merry-go-round, path of ball deflects to left. There is an apparent force.
(left click picture for animation) World Weather Project 2010 Courtesy of M. Ramamurthy U of Illinois, Urbana-Champaign Merry Go Round Link
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Rotation of the Earth (from the polar perspective)
NORTHERN HEMISPHERE SOUTHERN HEMISPHERE
COUNTERCLOCKWISE ROTATIONDeflection to the right
CLOCKWISE ROTATIONDeflection to the left
(Getzelman)
SAME IDEA AS THE MERRY-GO-ROUND!
deflectiondeflection
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Coriolis Effect: An Apparent Force
Cannonball follows a straight path to an observer in space
Earth rotates counter-clockwise underneath cannonball (in Northern Hemisphere)
Cannonball appears to deflect to the right to an observer on earth
Shot misses Paris to the right
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Coriolis Force and Latitude
All three airplanes travel in a straight line with respect to an outside observer (from space).
The largest deviation, or deflection to the right, with respect to an observer on Earth occurs for the one traveling closest to the pole.
The higher the latitude, the greater the Coriolis force. Accounted for by the sine term in the mathematical expression.
Zero at equator (sin 0° = 0)Maximum at poles (sin 90° = 1)
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Coriolis force and speed
The Coriolis force is proportional to the wind speed.
The faster the speed (or velocity), the greater the amount of Coriolis force.
Note also the dependence on latitude here.
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Coriolis Force vs. Wind Direction
NORTHERN HEMISPHERE SOUTHERN HEMISPHERE
WINDWIND
CORIOLIS FORCECORIOLIS FORCE(TO RIGHT)(TO RIGHT)
WIND
CORIOLIS FORCECORIOLIS FORCE(TO LEFT)(TO LEFT)
Coriolis forceCoriolis force acts perpendicular (at a right angle) to the wind wind directiondirection, to the right or left depending on which hemisphere.
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Key Points: Coriolis Force
• Introduced to account for the earth’s rotation.• Only deflects a moving object.
Never changes the speed of an object.• Zero if the velocity of an object relative to the
earth’s surface is zero.• Zero at the equator.
For given speed, it is maximum at the poles.
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Geostrophic Adjustment
A. Parcel at rest initially accelerates toward lower pressure.
B. Coriolis Force rotates parcel to right in NH.
C. As parcel speeds up, Coriolis Force increases.
D. Eventually (about a day), PGF equals CF and flow is parallel to isobars.
(left click picture to animate) World Weather Project 2010 Courtesy of M. Ramamurthy U of Illinois, Urbana-Champaign
Animate Picture
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Geostrophic Wind
Positions 1 and 2:
Pressure gradient forcePressure gradient force accelerates the parcel towards the low pressure.
Coriolis forceCoriolis force acts to the right of the velocityvelocity of the parcelof the parcel, making it curve to the right.
PARCEL RELEASED
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Positions 3 and 4:
Pressure gradient force continues to accelerate the parcel towards the low pressure.
As the velocity of the parcelvelocity of the parcel increases, the Coriolis forceCoriolis force increases, making the parcel continue to curve to the right.
Geostrophic Wind
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Position 5: FINAL STATE
Pressure gradient forcePressure gradient force is balanced by the Coriolis forceCoriolis force.
Velocity of the parcelVelocity of the parcel is constant (no acceleration). Direction is parallel to the isobars.
FINAL STATE is called geostrophic balance.
Geostrophic Wind
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Geostrophic Wind
Pressure gradient forcePressure gradient force is equally balanced by the Coriolis forceCoriolis force, so net force is zero.
Wind speed and direction (velocity)Wind speed and direction (velocity) is constant (no acceleration).
Direction of wind is parallel to the isobars, or lines of constant pressure.
WINDWIND
CORIOLIS FORCECORIOLIS FORCE
PRESSURE GRADIENTPRESSURE GRADIENTFORCEFORCE
Isobar 1
Isobar 2
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WINDWIND
CORIOLIS FORCECORIOLIS FORCE
PRESSURE GRADIENTPRESSURE GRADIENTFORCEFORCE
Isobar 1
Isobar 2
WINDWIND
PRESSURE GRADIENTPRESSURE GRADIENTFORCEFORCE
Isobar 2
Isobar 1
WEAKGEOSTROPHIC
WIND
Isobars far apart
STRONGGEOSTROPHIC
WIND
Isobars close together
CORIOLIS FORCECORIOLIS FORCE
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PRESSURE PRESSURE GRADIENT GRADIENT
FORCEFORCE
Geostrophic Wind and Upper Level Charts
CORIOLIS CORIOLIS FORCE FORCE
GEOSTROPHIC GEOSTROPHIC WIND WIND
Winds at upper levels are pretty close to being geostrophic:
Wind is parallel to isobars
Wind strength dependents on
how close together isobars are
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GEOSTROPHY:No centripetal force or friction
Simplified equation of horizontal atmospheric motion
Term Force Cause
1 Pressure gradient force Spatial differences in pressure
2 Coriolis force Rotation of the Earth
3 Centripetal force Curvature of the flow
4 Friction force Acts against direction of motion due to interaction with surface
(1) (2) (3) (4)
XTotal Force = 1ρΔpd
+ 2ΩVsinϕ +V2
r+ Fr
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Do Rocks Always Roll Downhill?
Gedzelman, p 247
Upper-Level Winds
PGF
Not if the Hill is Big Enough!
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Fundamental Concepts for Today
• Rotation of Earth
Geocentric =Accelerated Frame of Reference• Introduce Coriolis “Force”
Apparent Force to Account for Deflection Depends on Rotation, Latitude, Wind Speed
• Geostrophic Balance and Wind
Balance Between PGF and Coriolis Force Geostrophic Wind Blows Parallel to Contours About One Day Required to Reach Balance
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Assignment Next LectureSurface Wind,Vertical Air Motions
• Reading - Ahrens3rd: 155-1624th: 157-1645th: 158-164
• Problems - HW05 D2L (Due Wed. Mar. 3)3rd-Pg 162: 6.23, 6.244th-Pg 164: 6.23, 6.245th-Pg 165: 6.24, 6.25