We illustrate with an example how the OGGM workflow is applied to the Tasman Glacier in New Zealand. Here we describe shortly the purpose of each processing step, while more details are provided in the other sections:

The glacier outlines extracted from the RGI are projected onto a local gridded map of the glacier (Fig. a). Depending on the glacier’s location, a suitable source for the topographical data is downloaded automatically (here SRTM) and interpolated to the local grid. The map’s spatial resolution depends on the size of the glacier.
The glacier centerlines are computed using a geometrical routing algorithm and then filtered and slightly adapted modified to become glacier “flowlines” with a fixed grid spacing (Fig. c).
Catchment areas and widths
The geometrical widths along the flowlines are obtained by intersecting the normals at each grid point with the glacier outlines and the tributaries’ catchment areas. Each tributary and the main flowline has a catchment area, which is then used to correct the geometrical widths so that the flowline representation of the glacier is in close accordance with the actual altitude-area distribution of the glacier (Fig. d, note that the normals are now corrected and centred).
Climate data and mass-balance
Gridded climate data (monthly temperature and precipitation) are interpolated to the glacier location and corrected for altitude at each flowline’s grid point. A carefully calibrated temperature-index model is used to compute the mass-balance for any month in the past.
Ice thickness inversion
Using the mass-balance data computed above and relying on mass-conservation considerations, an estimate of the ice flux along each glacier cross-section can be computed. by making assumptions about the shape of the cross-section (parabolic or rectangular) and using the physics of ice flow, the model computes the thickness of the glacier along the flowlines and the total volume of the glacier (Fig. e).
Glacier evolution
A dynamical flowline model is used to simulate the advance and retreat of the glacier under preselected climate time series. Here (Fig. f), a 120-yrs long random climate sequence leads to a glacier advance.