Lambert azimuthal equal-area projection

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Lambert azimuthal equal-area projection of the world. The center is 0° N 0° E. The antipode is 0° N 180° E, near Kiribati in the Pacific Ocean. That point is represented by the entire circular boundary of the map, and the ocean around that point appears along the entire boundary.
The Lambert azimuthal equal-area projection with Tissot's indicatrix of deformation.

The Lambert azimuthal equal-area projection is a particular mapping from a sphere to a disk. It accurately represents area in all regions of the sphere, but it does not accurately represent angles. It is named for the Swiss mathematician Johann Heinrich Lambert, who announced it in 1772.[1] "Zenithal" being synonymous with "azimuthal", the projection is also known as the Lambert zenithal equal-area projection.[2]

The Lambert azimuthal projection is used as a map projection in cartography. For example, the National Atlas of the US uses a Lambert azimuthal equal-area projection to display information in the online Map Maker application,[3] and the European Environment Agency recommends its usage for European mapping for statistical analysis and display.[4] It is also used in scientific disciplines such as geology for plotting the orientations of lines in three-dimensional space. This plotting is aided by a special kind of graph paper called a Schmidt net.[5]


A cross sectional view of the sphere and a plane tangent to it at S. Each point on the sphere (except the antipode) is projected to the plane along a circular arc centered at the point of tangency between the sphere and plane.

To define the Lambert azimuthal projection, imagine a plane set tangent to the sphere at some point S on the sphere. Let P be any point on the sphere other than the antipode of S. Let d be the distance between S and P in three-dimensional space (not the distance along the sphere surface). Then the projection sends P to a point P′ on the plane that is a distance d from S.

To make this more precise, there is a unique circle centered at S, passing through P, and perpendicular to the plane. It intersects the plane in two points; let P′ be the one that is closer to P. This is the projected point. See the figure. The antipode of S is excluded from the projection because the required circle is not unique. The case of S is degenerate; S is projected to itself, along a circle of radius 0.[6]

Explicit formulas are required for carrying out the projection on a computer. Consider the projection centered at S = (0, 0, −1) on the unit sphere, which is the set of points (x, y, z) in three-dimensional space R3 such that x2 + y2 + z2 = 1. In Cartesian coordinates (x, y, z) on the sphere and (X, Y) on the plane, the projection and its inverse are then described by

In spherical coordinates (ψ, θ) on the sphere (with ψ the colatitude and θ the longitude) and polar coordinates (R, Θ) on the disk, the map and its inverse are given by [6]

In cylindrical coordinates (r, θ, z) on the sphere and polar coordinates (R, Θ) on the plane, the map and its inverse are given by

The projection can be centered at other points, and defined on spheres of radius other than 1, using similar formulas.[7]


As defined in the preceding section, the Lambert azimuthal projection of the unit sphere is undefined at (0, 0, 1). It sends the rest of the sphere to the open disk of radius 2 centered at the origin (0, 0) in the plane. It sends the point (0, 0, −1) to (0, 0), the equator z = 0 to the circle of radius 2 centered at (0, 0), and the lower hemisphere z < 0 to the open disk contained in that circle.

The projection is a diffeomorphism (a bijection that is infinitely differentiable in both directions) between the sphere (minus (0, 0, 1)) and the open disk of radius 2. It is an area-preserving (equal-area) map, which can be seen by computing the area element of the sphere when parametrized by the inverse of the projection. In Cartesian coordinates it is

This means that measuring the area of a region on the sphere is tantamount to measuring the area of the corresponding region on the disk.

On the other hand, the projection does not preserve angular relationships among curves on the sphere. No mapping between a portion of a sphere and the plane can preserve both angles and areas. (If one did, then it would be a local isometry and would preserve Gaussian curvature; but the sphere and disk have different curvatures, so this is impossible.) This fact, that flat pictures cannot perfectly represent regions of spheres, is the fundamental problem of cartography.

As a consequence, regions on the sphere may be projected to the plane with greatly distorted shapes. This distortion is particularly dramatic far away from the center of the projection (0, 0, −1). In practice the projection is often restricted to the hemisphere centered at that point; the other hemisphere can be mapped separately, using a second projection centered at the antipode.


The Lambert azimuthal projection was originally conceived as an equal-area map projection. It is now also used in disciplines such as geology to plot directional data, as follows.

A direction in three-dimensional space corresponds to a line through the origin. The set of all such lines is itself a space, called the real projective plane in mathematics. Every line through the origin intersects the unit sphere in exactly two points, one of which is on the lower hemisphere z ≤ 0. (Horizontal lines intersect the equator z = 0 in two antipodal points. It is understood that antipodal points on the equator represent a single line. See quotient topology.) Hence the directions in three-dimensional space correspond (almost perfectly) to points on the lower hemisphere. The hemisphere can then be plotted as a disk of radius 2 using the Lambert azimuthal projection.

Thus the Lambert azimuthal projection lets us plot directions as points in a disk. Due to the equal-area property of the projection, one can integrate over regions of the real projective plane (the space of directions) by integrating over the corresponding regions on the disk. This is useful for statistical analysis of directional data,[6] including random rigid rotation.[8]

Not only lines but also planes through the origin can be plotted with the Lambert azimuthal projection. A plane intersects the hemisphere in a circular arc, called the trace of the plane, which projects down to a curve (typically non-circular) in the disk. One can plot this curve, or one can alternatively replace the plane with the line perpendicular to it, called the pole, and plot that line instead. When many planes are being plotted together, plotting poles instead of traces produces a less cluttered plot.

Researchers in structural geology use the Lambert azimuthal projection to plot crystallographic axes and faces, lineation and foliation in rocks, slickensides in faults, and other linear and planar features. In this context the projection is called the equal-area hemispherical projection. There is also an equal-angle hemispherical projection defined by stereographic projection.[6]

The discussion here has emphasized an inside-out view of the lower hemisphere z ≤ 0 (as might be seen in a star chart), but some disciplines (such as cartography) prefer an outside-in view of the upper hemisphere z ≥ 0.[6] Indeed, any hemisphere can be used to record the lines through the origin in three-dimensional space.

Comparison of the Lambert azimuthal equal-area projection and some azimuthal projections centred on 90° N at the same scale, ordered by projection altitude in Earth radii. (click for detail)

Animated Lambert projection[edit]

[citation needed]

Animation of a Lambert projection. Each grid cell maintains its area throughout the transformation. In this animation, points on the equator remain always on the plane.
In this animated Lambert projection, the south pole is held fixed.

Let be two parameters for which and . Let be a "time" parameter (equal to the height, or vertical thickness, of the shell in the animation). If a uniform rectilinear grid is drawn in space, then any point in this grid is transformed to a point on a spherical shell of height according to the mapping

where . Each frame in the animation corresponds to a parametric plot of the deformed grid at a fixed value of the shell height (ranging from 0 to 2). Physically, is the stretch (deformed length divided by initial length) of infinitesimal line line segments. This mapping can be converted to one that keeps the south pole fixed by instead using

Regardless of the values of , the Jacobian of this mapping is everywhere equal to 1, showing that it is indeed an equal area mapping throughout the animation. This generalized mapping includes the Lambert projection as a special case when .

Application: this mapping can assist in explaining the meaning of a Lambert projection by showing it to "peel open" the sphere at a pole, morphing it to a disk without changing area enclosed by grid cells.

See also[edit]


  1. ^ Mulcahy, Karen. "Lambert Azimuthal Equal Area". City University of New York. Retrieved 2007-03-30.
  2. ^ The Times Atlas of the World (1967), Boston: Houghton Mifflin, Plate 3, et passim.
  3. ^ "Map Projections: From Spherical Earth to Flat Map". United States Department of the Interior. 2008-04-29. Archived from the original on 2009-05-07. Retrieved 2009-04-08.
  4. ^ "Short Proceedings of the 1st European Workshop on Reference Grids, Ispra, 27-29 October 2003" (PDF). European Environment Agency. 2004-06-14. p. 6. Retrieved 2009-08-27.
  5. ^ Ramsay (1967)
  6. ^ a b c d e Borradaile (2003).
  7. ^ "Geomatics Guidance Note 7, part 2: Coordinate Conversions & Transformations including Formulas" (PDF). International Association of Oil & Gas Producers. September 2016. Retrieved 2017-12-17.
  8. ^ Brannon, R.M., "Rotation, Reflection, and Frame Change", 2018


  • Borradaile, Graham J. (2003). Statistics of Earth science data. Berlin: Springer-Verlag. ISBN 3-540-43603-0.
  • Do Carmo; Manfredo P. (1976). Differential geometry of curves and surfaces. Englewood Cliffs, New Jersey: Prentice Hall. ISBN 0-13-212589-7.
  • Hobbs, Bruce E., Means, Winthrop D., and Williams, Paul F. (1976). An outline of structural geology. New York: John Wiley & Sons, Inc. ISBN 0-471-40156-0.{{cite book}}: CS1 maint: multiple names: authors list (link)
  • Ramsay, John G. (1967). Folding and fracturing of rocks. New York: McGraw-Hill.
  • Spivak, Michael (1999). A comprehensive introduction to differential geometry. Houston, Texas: Publish or Perish. ISBN 0-914098-70-5.

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