The River Red Gum Forests study area, by design,encompasses particular biogeographic regions whichmostly carry river red gum or associated vegetationtypes. Because biological features are strongly correlatedwith geomorphological systems, the study area mostlyencompasses the Northern Riverine Plainsgeomorphological region (Map 3.1). Only small areas ofother regions—the North West Dunefields and Plains,the Eastern Uplands and Western Uplands occur thestudy area (and Rees 2000; see Rowan 1990).Northern Riverine PlainsThe Northern Riverine Plain is an extensive alluvial plainassociated with the Murray River and its tributaries,which extends north from the Western and EasternUplands of the Great Dividing Range to the River Murray.It can be divided into an upland fringing slope with lowresidual hills, a plain crossed by palaeochannels andmodern rivers such as the Loddon, Avoca andCampaspe, and the major alluvial terrace and floodplaininfilledtroughs of the Goulburn and Murray rivers.Concentrations of lake and lunette systems, such as theKerang Lakes, Avoca Marshes and Kow Swamp, occurintermittently across its surface.Much of the plain is made up of Quaternary alluvialdeposits of clay, silt sand and gravel (Shepparton andCoonambidgal Formations), forming broad fansextending and widening northwards from the uplandsedge. The sediments were laid down in a fluvial systemof floodplains and river channels, and in scatteredshallow lakes and wind-blown dunes. The depositsextend from upland valleys such as the Loddon andOvens and coalesce into an almost continuous mantleacross the study area. Leveed channels of several agesare present, sometimes forming ridges above the generalelevation of the plains, and may have source-borderingdunes. Higher terraces and aprons of uncertain ageoccur along the southern edge adjoining the uplands. Inplaces, low rocky ridges of older basement rocks, suchas the Terrick Terrick hills, rise above the plains.Features of floodplain evolution and development can becategorised as modern streams, prior streams, ancestralrivers and lakes and lunettes (e.g. Bowler et al. 1978;Pels 1964; Rutherfurd 1990). Modern streams are thechannels and swamps of the present-day river system(described in more detail under ‘River Murray Evolution’,below), with generally narrow channels and well-definedlevee banks and floodplains. Some, such as theCampaspe, have alluvial terraces. Lakes and swamps liein cut-off meanders or avulsion channels across thefloodplains.Prior streams are the traces of older rivers characterisedas low ridges of silt and sand—former natural leveebanks—that lie adjacent to shallow, meanderingdepressions of the former river channels. Often thesechannels are perched higher than the present floodplainand may be a great distance from present rivers.Typically, prior streams do not carry surface water, exceptin high flow conditions, and both channels and leveesare broken where they have been partly eroded by laterevents.Ancestral rivers are old, abandoned channels that lacklevee banks, are incised into the surface of the plain,and are partly filled with alluvium. They are associatedwith and often crossed by the modern rivers and mayact as floodways during high water flow. Many arewider than those of the present-day rivers, have coarsesand and gravel, and have much larger meanders,indicating they formed at times of much greater riverdischarge. Modern rivers often form a meander withinthe larger meander pattern of these ancestral rivers.Lakes on the riverine plain have formed in three ways, ascut-off meanders and abandoned channels, deflation(wind-eroded) hollows, and as tectonic depressions.Many of these lakes are composite and fed bygroundwater. Associated with shallow lakes are lunettes,crescent-shaped dunes composed of clay, silt and finesand typically along the eastern shoreline. Some aresingle, but many form complex systems that record thegradual decrease in the size of the adjoining lake (e.g.palaeo-Lake Kanyapella, see Box 3.2). Most of thelunette sediment consists of clay and fine sand blownfrom the lake floor during dry conditions.The alluvial terraces and floodplains of the modern rivers(Coonambidgal Formation—see Map 3.1) often havesource-bordering dunes on the northeastern sides ofchannels, formed from fine sand deposited by the sameriver in times of greater flow. Several former courses ofthe major rivers, such as the Murray and Goulburn, aremarked by extensive meander belts and occur in shallowdepressions incised below the plains. These featuresindicate several phases of channel and dune activity,with many dunes forming along the Murray River duringthe last major dry glacial period. River channels withwide sandy point bars persisted into the Holocene, butformation of dunes along the river ceased as the climatewarmed.The final episode of river deposition after the glacial andperiglacial conditions is present along the length of theRiver Murray and its tributaries. The current channel ofthe Murray River may be only a few hundred years old inmany places. Some areas on the riverine plain, such asbetween Tragowel and Pine Grove, have only rarechannels and no source-bordering dunes. Much of thecentral and eastern parts of the plain are overlain by ashallow mantle of calcareous wind-blown deposits (orparna) comprising silt and clay aggregates.Near Echuca, movement along the Cadell Fault dammedthe River Murray to produce palaeo-Lake Kanyapellaaround 30,000 years ago (see Box 3.2 Bowler 1978;Cupper & White 2003; Page et al. 1991; Rutherfurd &Kenyon 2005). Other faults (such as the Echuca SouthFault) cross the alluvial deposits and alter the earlierleveed stream channels, allowing a chronologicalsequence of channels to be mapped (see Rutherfurd &Kenyon 2005). However some previously postulated‘faults’ e.g. Leaghur Fault, are now regarded as erosionalfeatures, as evidence for displacement or movementcannot be found.Hattah Lakes is the most extensive lake system along theRiver Murray, where a series of about 21 interconnectedlakes and wetlands formed in a depression at theeasternmost limit of the Sunset Country dunefields(Figure 3.2). The lakes are surrounded by longitudinaldunes of the Woorinen Formation and sub-parabolicdunes of the Lowan Sands. Water is supplied to the<strong>Discussion</strong> <strong>Paper</strong>21
lakes by flooding from Chalka Creek:—an anabranch ofthe River Murray. Several of these lakes lie on the floorof the pre-existing Hattah ‘Mega-lake’ (in the order of50 square km in size), which is bordered to the east by alarge lunette (Kotsonis et al. 1999; Macumber 1978).The large size of the palaeo-lake, combined with highriver discharge in the past, suggests that it containedfreshwater, and developed during the pre-glacial wetterclimates with significantly more surface water in theMurray Basin. Hattah Mega-lake is entrenched at atopographic level similar to the upper river terrace in thisarea, and probably developed from an old meander cutoffon this terrace.Sub-parabolic dunes completely cover the high levelterrace at Hattah Lakes and partially cover the HattahMega-lake floor, indicating that dune encroachmentoccurred at similar times to lunette formation and afterthe drying-out of the lake. The presence of sourceborderingdunes and sub-parabolic dunes on the lowlevel terrace suggests a high level of wind activity duringdeposition of this terrace. The present fluvial regimelacks source-bordering dunes and truncates sandy duneson older terraces, indicating that dune mobility hadceased when this river system became active about15,000 years ago. Within the Hattah Mega-lake, thisreduction in aeolian activity was accompanied by aFigure 3.2 Air Photo of the Hattah lakes complex.NowingiTarpaulin IslandReference AreaRetailBendCalder HighwayChalka CreekReference AreaChalka CreekHattahVisitor CentreMurray Valley HighwayLEGENDRoadsStudy Area BoundaryLakesReference AreaHattah-Kulkyne National Park BoundaryHattah Mega-lake22 River Red Gum Forests Investigation 2006
Change language