with sand moving with flooding waters. From this we know that the swamp area was close to the coastline, and then due to sea level rise in the area, flooded over burying the kerogen. The fluvial channelization continued for some time, and created a larger channel, originally thought to be a boudin. This is disproved however by channelization in the upper parts of the formation. At periods of higher sea level herein, the sandstone was covered by muddy shales and these layers are distinguishable due to the fact that they are able to grow trees. Once the normal faulting has occurred, the kerogen becomes cracked, allowing coalification to take place. Pyrite present in the system would be removed from the beds and transported by the hydrothermal fluids as the iron(II) cation with dissolved sulfur in solution. This is the source of iron in the hydrothermal fluid. Warang Sandstone The Warang Sandstone is a litharenite sandstone unit within the gorge consisting of Early to Mid-Triassic fluvial channel deposits. One of the most interesting parts of the formation occurs at the contact between the Warang Sandstone and Betts Creek Beds. In this area the sandstone has been fractured by a strike-slip fault system that has encouraged the release of the underlying hydrothermal fluids sourced from the Betts Creek Beds. Due to the leaching that has happened of the sandstone units below, the iron(II) must accrete somewhere, and this has happened along the faults, creating very dense, ferric build up in the sandstone pores. Moving upwards from where the shearing outcrops, the destination of the fluids becomes apparent in an area that initially appears to have been folded however this is not the case at all. As the sandstone becomes fractured, it gets broken into segments, a sort of sedimentary box. These begin to trap the hydrothermal fluids, most especially the ferric components and the remaining solution escapes as water. The resulting “folded” pattern is in fact a boxwork concretion, and shows how the fluid has arrived at that point. From this point upwards, the more distinct fluvial channels are present in abundance. These are primarily fine grained sandstone with infill of more coarse grained material. Interbedded mudstone and shale layers become compressed by the overlying sediments and these compress to become load structures. The channels contain finely laminated mud clasts that have been carried through, and due to being softer sediments, these