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Introduction to GIS ©2008 Austin Troy. Introduction to GIS Find the Treasure? ©2008 Austin Troy.

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Presentation on theme: "Introduction to GIS ©2008 Austin Troy. Introduction to GIS Find the Treasure? ©2008 Austin Troy."— Presentation transcript:

1 Introduction to GIS ©2008 Austin Troy

2 Introduction to GIS Find the Treasure? ©2008 Austin Troy

3 Introduction to GIS The Earth’s Shape and Size ©2008 Austin Troy Only recently have we known both Estimates of shape by the ancients have ranged from a flat disk, to a cube to a cylinder to an oyster. Pythagoras was the first to postulate it was a sphere By the 5th century BCE, this was firmly established. But how big was it?

4 Introduction to GIS The Earth’s Size ©2008 Austin Troy Posidonius used the stars to determine the earth's circumference. He observed that the star Canopus could be seen just on the horizon at Rhodes (Greece) but appeared above the horizon when viewed from Alexandria, Egypt (1 st century BCE). -source: ESRI

5 Introduction to GIS The Earth’s Size ©2008 Austin Troy He calculated the angle of difference to be 7.5 degrees or 1/48th of a circle. Multiplying 48 by what he believed to be the correct distance from Rhodes to Alexandria (805 kilometers or 500 miles), Posidonius calculated the earth's circumference to be 38,647 kilometers (24,000 miles) – an error of only three percent. ” -source: ESRI

6 Introduction to GIS So, what shape IS the earth? ©2008 Austin Troy Earth is not a sphere, but an ellipsoid, because the centrifugal force of the earth’s rotation “flattens it out”. This was finally proven by the French in 1753 The earth rotates about its shortest axis, or minor axis, and is therefore described as an oblate ellipsoid Source: ESRI

7 Introduction to GIS And it’s also a…. ©2008 Austin Troy Because it’s so close to a sphere, the earth is often referred to as a spheroid: that is a type of ellipsoid that is really, really close to being a sphere These are two common spheroids used today: the difference between its major axis and its minor axis is less than 0.34%.... Source: ESRI

8 Introduction to GIS Spheroids ©2008 Austin Troy The International 1924 and the Bessel 1841 spheroids are used in Europe while in North America the GRS80, and decreasingly, the Clarke 1866 Spheroid, are used In Russia and China the Krasovsky spheroid is used and in India the Everest spheroid

9 Introduction to GIS Spheroids ©2008 Austin Troy Note how two different spheroids have slightly different major and minor axis lengths Source: ESRI

10 Introduction to GIS Scale… revisited ©2008 Austin Troy 1:2,000,000vs. 1:20,000

11 Introduction to GIS Spheroids ©2008 Austin Troy One more thing about spheroids: If your mapping scales are smaller than 1:5,000,000 (small scale maps), you can use an authalic sphere to define the earth's shape to make things more simple For maps at larger scale (most of the maps we work with in GIS), you generally need to employ a spheroid to ensure accuracy and avoid positional errors

12 Introduction to GIS Geoid ©2008 Austin Troy While the spheroid represents an idealized model of the earth’s shape, the geoid represents the “true,” highly complex shape of the earth, which, although “spheroid- like,” is actually very irregular at a fine scale of detail, and can’t be modeled with a formula (the DOD tried and gave up after building a model of 32,000 coefficients)

13 Introduction to GIS Geoid ©2008 Austin Troy It is the 3 dimensional surface of the earth along which the pull of gravity is a given constant; ie. a standard mass weighs an identical amount at all points on its surface The gravitational pull varies from place to place because of differences in density, which causes the geoid to bulge or dip below or above the ellipsoid Overall these differences are small (~100 meters)

14 Introduction to GIS Geoid ©2008 Austin Troy www.esri.com/news/arcuser/0703/geoid1of3.html The geoid is actually measured and interpolated, using gravitational measurements.

15 Introduction to GIS Spheroids and Geoids ©2008 Austin Troy We have several different estimates of spheroids because of irregularities and slight deviations that are quite variable across the Earth’s surface Before remote satellite observation, we had to use a different spheroid for different regions to account for irregularities (see Geoid) to avoid positional errors

16 Introduction to GIS Spheroids and Geoids ©2008 Austin Troy That is, continental surveys were isolated from each other, so ellipsoidal parameters were fit on each continent to create a spheroid that minimized error in that region, and many stuck with those for years

17 Introduction to GIS The Geographic Graticule/Grid ©2008 Austin Troy Once you have a spheroid, you also define the location of poles (axis points of revolution) and equator (midway circle between poles, spanning the widest dimension of the spheroid), and you then have enough information to create a coordinate grid or “graticule” for referencing the position of features on the spheroid.

18 Introduction to GIS The Geographic Graticule/Grid ©2008 Austin Troy This is a location reference system for the earth’s surface, consisting of: Meridians: lines of longitude and Parallels: lines of latitude Source: ESRI Prime meridian is at Greenwich, England (that is 0º longitude) Equator is at 0º latitude

19 Introduction to GIS The Geographic Graticule/Grid ©2008 Austin Troy This is like a planar coordinate system, with an origin at the point where the equator meets the prime meridian The difference is that it is not a Grid because grid lines must meet at right angles; this is why it’s called a graticule instead

20 Introduction to GIS The Geographic Graticule/Grid ©2008 Austin Troy Each degree of latitude represents about 110 km, although that varies slightly because the earth is not a perfect sphere

21 Introduction to GIS The Geographic Grid/Graticule ©2008 Austin Troy Latitude and longitude can be measured in degrees, minutes, seconds (e.g. 56° 34’ 30” ); minutes and seconds are base-60, like on a clock Can also use decimal degrees (more common in GIS – Why? ), where minutes and seconds are converted to a decimal Example: 45° 52’ 30” = 45.875°

22 Introduction to GIS The Geographic Grid/Graticule ©2008 Austin Troy Latitude lines form parallel circles of different sizes, while longitude lines are half-circles that meet at the poles Latitude goes from 0 to 90º N or S and longitude to 180º E or W of meridian; the 180º line is the date line Source: ESRI

23 Introduction to GIS Horizontal Datums ©2008 Austin Troy Definition: a three dimensional surface from which latitude, longitude and elevation are calculated Allows us to figure out where things actually are on the graticule since the graticule only gives us a framework for measuring, and not the actual locations Where is the origin?

24 Introduction to GIS Horizontal Datums ©2008 Austin Troy Hence, a datum provides a frame of reference for placing specific locations at specific points on the spheroid Defines the origin and orientation of latitude and longitude lines. A datum is essentially the model that is used to translate a spheroid into locations on the earth

25 Introduction to GIS Horizontal Datums ©2008 Austin Troy A spheroid only gives you a shape—a datum gives you locations of specific places on that shape. Hence, a different datum is generally used for each spheroid Two things are needed for datum: spheroid and set of surveyed and measured points

26 Introduction to GIS Geoid and the vertical datum ©2008 Austin Troy There is also a vertical datum, based on the geoid The geoid serves as the earth’s reference elevation when “sea level” is inadequate, which it is in many cases because the sea is not everywhere and because the sea can be affected by wind or weather The geoid provides the reference elevation from which vertical measurements can be taken.

27 Introduction to GIS Surface-Based Datums ©2008 Austin Troy Prior to satellites, datums were realized by connected series of ground-measured survey monuments A central location was chosen where the spheroid meets the earth: this point was intensively measured using pendulums, magnetometers, sextants, etc. to try to determine its precise location. Originally, the “datum” referred to that “ultimate reference point.” Eventually the whole system of linked reference and subrefence points came to be known as the datum.

28 Introduction to GIS Surface Based Datums ©2008 Austin Troy Starting points need to be very central relative to landmass being measured In NAD27 center point was Mead’s Ranch, KS

29 Introduction to GIS Surface Based Datums ©2008 Austin Troy NAD27 resulted in lat/long coordinates for about 26,000 survey points in the US and Canada. Limitation: requires line of sight, so many survey points were required Problem: errors compound with distance from the initial reference. This is why central location needed for first point

30 Introduction to GIS Surface Based Datums ©2008 Austin Troy c These were largely done without having to measure distances. How? Using high-quality celestial observations and distance measurements for the first two observations, could then use trigonometry to determine distances. a b A With b and c and A known, we can determine a’s location through solving for B and C by the law of sines B=A(sin(b))/(sin(a)) B C D E Mead’s Ranch Secondary Measured point

31 Introduction to GIS ©2008 Austin Troy

32 Introduction to GIS Satellite Based Datums ©2008 Austin Troy With satellite measurements the center of the spheroid can be matched with the center of the earth. Satellites started collecting geodetic information in 1962 as part of National Geodetic SurveyNational Geodetic Survey This gives a spheroid that when used as a datum correctly maps the earth such that all Latitude/Longitude measurements from all maps created with that datum agree. Rather than linking points through surface measures to initial surface point, measurements are linked to reference point in outer space

33 Introduction to GIS Common Datums ©2008 Austin Troy Previously, the most common spheroid was Clarke 1866; the North American Datum of 1927 (NAD27) is based on that spheroid, and has its center in Kansas. NAD83 is the new North American datum (for Canada/Mexico too) based on the GRS80 geocentric spheroid. It is the official datum of the USA, Canada and Central America World Geodetic System 1984 (WGS84) is a newer spheroid/datum, created by the US DOD; it is more or less identical to Geodetic Reference System 1980 (GRS80). The GPS system uses WGS84.

34 Introduction to GIS Lat/Long and Datums ©2008 Austin Troy These pre-satellite datums are surface based. A given datum has the spheroid meet the earth in a specified location somewhere. Datum is most accurate near the touching point, less accurate as move away (remember, this is different from a projection surface because the ellipsoid is 3D) Different surface datums can result in different lat/long values for the same location on the earth. So, just giving lat and long is not enough!!!

35 Introduction to GIS Lat/Long and Datums ©2008 Austin Troy Lat/long coordinates calculated with one datum are valid only with reference to that datum. This means those coordinates calculated with NAD27 are in reference to a NAD27 earth surface, not a NAD83 earth surface. Example: the DMS control point in Redlands, CA is -117º 12’ 57.75961”, 34º 01’ 43.77884” in NAD83 and -117º 12’ 54.61539”, 34º 01’ 43.72995” in NAD27

36 Introduction to GIS Datum Shift ©2008 Austin Troy NAD83 is superior to NAD27 because: NAD83 is more accurate and NAD27 can result in a significant horizontal shift When we go from a surface-oriented datum to a spheroid-based datum, the estimated position of survey benchmarks improves; this is called datum shiftdatum shift That shift varies with location: 10 to 100 m in the cont. US, 400 m in Hawaii, 35 m in Vermont Click here for an example from Peter DanaClick here

37 Introduction to GIS Datum Shift Example ©2008 Austin Troy source;: http://gallery.geocaching.com.au/Maps/DatumShifthttp://gallery.geocaching.com.au/Maps/DatumShift

38 Introduction to GIS Datum Shift Example ©2008 Austin Troy


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