Radiometric corrections that address atmospheric effects are about removing how the atmosphere changes what the sensor sees, through things like how sunlight hits the surface and how aerosols scatter or absorb light. Adjusting for the sun’s position (sun angle) is a classic step because the illumination of the surface changes with time and geometry. Correcting for haze targets the scattering and absorption caused by aerosols in the air, which can make surfaces look lighter or blur details. Ozone depletion correction isn’t a standard, separate correction used to adjust radiance in this context. Ozone effects are handled within atmospheric radiative transfer models, using ozone as part of the overall atmosphere in those calculations, rather than as a distinct, routine correction step. In contrast, noise removal is about reducing sensor noise, not atmospheric interference, so it isn’t an atmospheric correction per se, but the question focuses on atmospheric-related corrections. Because there isn’t a standard discrete “ozone depletion correction” step, that option is not a standard atmospheric radiance correction.

A seven-parameter Helmert transformation is the way to convert coordinates from one geodetic datum to another by applying three translations, three rotations, and a scale factor. The translations shift the origin between datums, the rotations align the orientation of the two reference frames, and the scale factor accounts for a slight difference in the size of the reference ellipsoids or overall scale of the frames. Together, these seven parameters allow a 3D coordinate in one datum to be expressed accurately in another, typically written in a form like X2 = t + (1 + s) * R * X1, where t is the translation vector, s is the scale, and R represents the small rotations. This is the standard approach for datum shifts, such as moving data between NAD27, NAD83, and WGS84. It isn’t about changing heights by itself, nor about changing UTM zones (which is a projection change), nor about time differences.

The line from the Earth's center to a point on the surface defines a radius vector, and the angle that this radius vector makes with the equatorial plane is called the geocentric latitude. This name comes from using the center of the Earth as the reference point for measuring the angle. It differs from the geodetic latitude, which is defined by the angle between the equatorial plane and the normal to the reference ellipsoid at that surface point (not the line to the center). On a perfect sphere these two latitudes would coincide, but for the oblate Earth they are generally different. Astronomical latitude relates to observations of stars and the local vertical, while authalic latitude is tied to a sphere of equal area to the ellipsoid, so those definitions involve different reference constructions.

When you take a line that follows the curved surface of the Earth (a geodetic line) and project it onto a flat map, the path on the plane is a straight line only if you’re looking at the straight-line connection between the endpoints (the chord). The actual path on the curved surface is an arc, and that arc does not map to the same straight-line direction or length on the plane. To transform geodetic azimuths into grid azimuths accurately, you need to account for this difference between the curved arc and its straight-line representation on the plane. That SAMPLEadjustment is arc-to-chord correction. It bridges the geodetic arc and the plane’s chord, ensuring the grid azimuth reflects the direction you’d measure on the map.