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Lecture 7 – Gravity and Related Issues. GISC-3325 11 February 2008. Scheduling Issues. Next class and lab will be on OPUS and GPS processing using OPUS. Next week I will be out. Monday or Wednesday (18 and 20 Feb) will be first exam. Chapters 1-4 and all lectures and labs

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scheduling issues
Scheduling Issues
  • Next class and lab will be on OPUS and GPS processing using OPUS.
  • Next week I will be out. Monday or Wednesday (18 and 20 Feb) will be first exam.
    • Chapters 1-4 and all lectures and labs
  • Lab 3 – BM recovery: due 25 February 2008.
slide3

Lab 2: Problem

How do I get this to work?

which model to use
Which model to use?
  • NAVD88 - Modeled Gravity uses a model developed for the NAVD88 adjustment rather than current gravity values.
slide12

Review of Height Systems

  • Helmert Orthometric
  • NAVD 88
  • local gravity field ( )
  • single datum point
  • follows MSL
earth s gravity field from space
Earth’s Gravity Field from Space
  • Satellite data was used for global models
    • Only useful at wavelengths of 700 km or longer
  • Lower wavelength data from terrestrial or marine gravity of varying vintage, quality and geographic coverage

Terrestrial and marine gravity data in NGS data base.

gravity
Gravity
  • Static gravity field
    • Based on long-term average within Earth system
  • Temporally changing component
    • Motion of water and air
    • Time scale ranges from hours to decades.
  • Mean and time variable gravity field affect the motion of all Earth space vehicles.
g ravity r ecovery a nd c limate e xperiment
Gravity Recovery And Climate Experiment

www.csr.utexas.edu/grace/gravity/

slide20

Orbit inclination: 89.048 degrees

Eccentricity: 0.000775

Semi-major axis: 6,849,706.754m

Distance between satellites: 222,732.810 m

how does grace work
How does GRACE work?
  • Motion of two satellites differ because they are at different positions in space.
  • When the lead SV approaches a higher gravity mass it accelerates as it moves beyond it decelerates.
  • Distance changes between SVs is measured precisely.
slide24

GRS 80 defined not only by geometric but also physical parameters (gravity).

From www.dgfi.badw.de/geoidis/REFS/grs80.html

gravitational acceleration
Gravitational Acceleration
  • The magnitude of acceleration (b) due to the Earth’s mass on the surface using a spherical geometric reference surface (R) is:
    • b = GM/R2
centrifugal acceleration
Centrifugal Acceleration
  • Direction is always perpendicular outward from the spin axis.
  • It is a function of angular velocity of the Earth squared and the distance from the point of interest on the surface of the sphere to the axis of rotation.
  • ω = 7292115e-11rad sec-1
  • We can compute this value as ratio of degrees over time.
magnitude of centrifugal acceleration
Magnitude of centrifugal acceleration
  • Varies from equator to poles.
  • Compute magnitude by velocity squared times the distance from the point of interest to the spin axis.
gravitational attraction
Gravitational Attraction
  • Is the vector sum of gravitational and centrifugal acceleration.
  • The actual acceleration of gravity varies from place to place, depending on latitude, altitude, and local geology.
  • By agreement among physicists, the standard acceleration of gravity gn is defined to be exactly 9.80665 meters per second per second (m s-2), or about 32.174 05 feet per second per second.
more mind numbing detail
More mind-numbing detail…
  • At latitude p, a conventional value of the acceleration of gravity at sea level is given by the International Gravity Formula,
    • g = 978.0495 [1 + 0.0052892 sin2(p) - 0.0000073 sin2 (2p)] cm per second per second (cm s-2).
  • The mean Earth gravity is about 981 000 mGal (the well-known 9.81 m/s2), varies from 978,100 mGal to 983,200 mGal from Equator to pole due to the Earth\'s flattening and rotation.
gravitational potential
Gravitational Potential
  • Magnitude of the potential is the work that must be done by gravity to move a unit mass from infinity to the point of interest.
  • Is dependent on position within the gravitation field.
equipotential surfaces
Equipotential Surfaces
  • Surface having constant gravity potential NOT constant gravity.
    • Also known as level surfaces or geopotential surfaces.
  • Surfaces are perpendicular at all points of the plumb line (gravity vector).
  • A still lake surface is an equipotential surface.
    • It is not horizontal but curved.
slide35

Image from Featherstone, W, “Height Systems and Vertical Datums” Spatial Science, Vol 51 No. 1, June 2006

properties of equipotential surfaces
Properties of equipotential surfaces
  • They are closed continuous surfaces that never cross one another.
  • They are formed by long radius arcs. Generally without abrupt steps.
  • They are convex everywhere.
geopotential number
Geopotential Number
  • C (geopotential number) – is a value derived from the difference in gravity potential between an equipotential surface of interest and the geoid.
  • Represents the work required to move a 1kg mass from the geoid to the geopotential surface at the point of interest.
  • C is numerically similar to the elevation of the point in meters.
leveling issues
Leveling Issues
  • Height
    • The distance measured along a perpendicular between a point and a reference surface.
  • Raw leveled heights
    • Non-unique. Depending on the path taken a different height will be determined for the same point. They have NO physical relevance.
geopotential numbers
Geopotential Numbers
  • Geopotential numbers
    • Unique, path-independent
    • Geopotential number (C) at a point of interest (p) is the difference between the potential on the geoid and potential at the point.
      • C = W0-Wp
slide42

Leveled Height vs. Orthometric Height

 h = local leveled differences

H = relative orthometric heights

Equipotential Surfaces

B

Topography

 hAB

=  hBC

A

C

HA

HC

HAChAB + hBC

Reference Surface (Geoid)

Observed difference in orthometric height, H, depends on the leveling route.

orthometric height
Orthometric Height
  • Vertical distance from the geoid to the point of interest. (along curved plumb line).
  • Orthometric height (H) may be determined from H = geopotential number / mean gravity along plumb line
    • We use assumptions about mass density to estimate mean gravity.
dynamic heights
Dynamic Heights
  • Takes the geopotential number at a point and divides it by a constant gravity value.
  • The constant value used in the US is the normal gravity value at 45 degrees N latitude
    • 980.6199 gals
cc area dynamic heights
CC area Dynamic Heights

NAVD 88 and dynamic heights differ by only 1 mm at this station.

dynamic heights1
Dynamic Heights

NAVD 88 = 2026.545 m

DYN Hght= 2023.109

Difference = 3.436 m

dynamic height problems
Dynamic Height Problems
  • Dynamic height corrections applied to spirit-leveled height differences can be very large (several meters) if the chosen gravity value is not representative for the region of operation.
slide52

ITRF96/GRS-80 ellipsoid surface

NAD 83 datum

G99BM

G99SSS

GEOID99

MSL

SST

global geopotential surface

Average of 52 cm

NAVD 88 datum

NOTE: heights are not to scale

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