4. Northern Riverine Plain (RP)
4.2.1 - Plains with leveed channels, sometimes source-bordering dunes (Tatura, Naneela)
4.2.2 - Plains without leveed channels (Tragowel, Pine Grove)
4.2.3 - Plains with lakes and depressions with lunettes (Lake Mokoan, Bael Bael, Lake Tutchewop)
|The older alluvial plains are not normally subject to flooding. All of the soils on these plains are derived from sediments deposited mainly during the Pleistocene (Late Neogene), which are collectively known as the Shepparton Formation. The sediments are believed to come from two sources: riverine deposits from distributary and divergent streams originating from the uplands and second and minor deposition of aeolian sediments or “parna” blown in from the west. Terraces, alluvial fans and aprons of uncertain age occur along the edge of the uplands (4.3) and are generally higher in the landscape than the older alluvial plains.|
Parna differs from loess in America, Europe and Asia in that it is calcareous and more clayey. During the Pleistocene, the climate cycled between pluvial (high rainfall) and arid phases. Alluvial deposition mostly occurred during periods of aridity, as soil fixed by vegetation in the uplands during the wetter periods became mobilised. At peaks of aridity, parna was blown in by prevailing winds from the west. Areas of parna near or at the surface are recognised east of the Loddon River but are not apparent in the western parts of the older alluvial plains around Horsham.
It is convenient to subdivide the older alluvial plains into three subdivisions on the basis of easily recognisable landscape features, plains with leveed channels associated with now defunct stream systems known as prior streams (4.2.1), plains without leveed channels (4.2.2) and lakes and basins with lunettes within the older alluvial plains (4.2.3).