are best understood by comparing them to the corresponding direct (or forward) problems. In direct problems we have an input which we run through some kind of process to get an output. We know what the input is and we also know what the process is, so we can figure out what the output will be.
For inverse problems we reverse the order. Now we have a given output and some idea of what kind of process acted on it, and possibly some information about the input. Our task is to figure out what the input was which resulted in this output.
One might ask if the inverse problem is equivalent to a direct problem if we know the process exactly, so that we could then simply run the process backwards. Unfortunately this is rarely possible since most processes cannot be reversed. As a simple example one could consider the process which takes two numbers X and Y, and gives the sum X+Y. But if we are given some number Z and are asked to determine which X and Y sum to this Z, we would quickly find that there are many possible solutions without any other restrictions on the allowed inputs.
An other example is to find missing integers, of the grid given here, such that the sum of each row and column is the integer given in the picture. This toy problem is closely connected to medical imaging modality known the X-ray tomography. Each tissue type attenuates the X-ray beams differently and in principle the total attenuation of a beam, traveling trough a body, is the sum of attenuation coefficients multiplied by the depth of corresponding tissue. Thus to figure out the structure of the body we can try to solve an inverse problem of X-ray tomography, which is to recover the attenuation coefficient at each location, from the total attenuations of X-ray beams traveling through the body.
Geometric inverse problem in seismology
For example, consider Earth or some other solid body with a variable speed of wave propagation. The travel time of a wave between two points defines a natural non-Euclidean distance between the points. This is called the travel time metric and it corresponds to the distance function of a Riemannian / Finsler manifold.
A classical inverse problem is to determine the wave speed inside an object when we know the travel times between the boundary points. This problem is an idealization of the geophysical problem where the structure of the Earth is to be found from the travel times of first arrivals of the earthquakes through the Earth. Moreover, measuring the wavefronts of elastic waves scattered from discontinuities inside the Earth, one obtains information on the broken geodesics in the Riemannian metric. Thus seismic measurements give information on the internal structure of the Earth. Almost all of our knowledge of the deep Earth is obtained using such data.