This result is upheld by the perception that few scarps don't proceed from the Nullarbor Plain toward the ca. 2 Ma (James et al. 2006) Roe Plain surface.
Two traced scarp cause displacement of the Roe Plain surface vertically by about 5 m individually as show in figure 7b and seem to connect into one scarp when traced towards the Nullarbor Plain margin. Estimated vertical slip rate in the order of 2.5 m/Ma is acquired, or two times that number supposed that it is accepted that the scarps join into one single fault at depth. This coincides to dip- slip rates of about 3.5 – 7.0 m/Ma for a fault dipping at 45°.
Therefore, vertical displacement over the Roe Plain scarp at the point it cuts the Nullarbor Plain surface is in the order of 15 to …show more content…
1995; Hillis and Reynolds 2003). This is conceivable that the scarp record identifies with the last 5-10 Ma, as opposed to the last 15 Ma.
Present- day and ongoing tectonism is evident on the northwestern area of Eyre Peninsula. This is display by recurring and dated fault scarps formed on granite hills in the Gawler Craton (Twidale and Bourne, 2000a). Most of the scarps are reverse type, while a few others are thrust faults formed at local scale. A study by K.R. Miles (1952a) on northeastern Eyre Peninsulahas has identified surfaces bearing a calcrete duricrust of Pleistocene or Holocene age being affected by faults. A view of one of these offset is seen in an old mine tunnel to actually be a reverse fault type (Dunham, …show more content…
Toward north is a reverse type fault bearing Pleistocene gravel across folded Proterozoic deposit is revealed near Terowie (Love et al., 1995, p. 270). Also confirmed on the north-eastern piedmont of the Flinders Ranges is severe folding of Miocene silcrete and related faulting, furthermore, and in slight magnitude, within the highland (Coats et al, 1969).
On the northern Flinders ranges the east-plunging Mt Babbage thrust has conveyed Mesoproterozoic rock across Late Pleistocene and Holocene alluvia (Love et al., 1995, p. 270). Amid the 1986 quake (Crone et al, 1997), low scarps were created at Marryat River, close Kulgera on the South Australia-Northern Domain fringe. Moving further toward the north in the Tennant Creek region, the quake which took place in 1994 created a succession of low scarps akin to reverse faulting (Crone et al, 1997).
As we move far from the topographic hub of the Flinders Ranges neotectonic deformation become more unobtrusive (Figure 9a). Toward the west, neotectonism is very much recorded on various faults on the upper east Eyre Peninsula (e.g. Crone et al. 2003 and Robert 2007) (Figure 9b), the Yorke
Two traced scarp cause displacement of the Roe Plain surface vertically by about 5 m individually as show in figure 7b and seem to connect into one scarp when traced towards the Nullarbor Plain margin. Estimated vertical slip rate in the order of 2.5 m/Ma is acquired, or two times that number supposed that it is accepted that the scarps join into one single fault at depth. This coincides to dip- slip rates of about 3.5 – 7.0 m/Ma for a fault dipping at 45°.
Therefore, vertical displacement over the Roe Plain scarp at the point it cuts the Nullarbor Plain surface is in the order of 15 to …show more content…
1995; Hillis and Reynolds 2003). This is conceivable that the scarp record identifies with the last 5-10 Ma, as opposed to the last 15 Ma.
Present- day and ongoing tectonism is evident on the northwestern area of Eyre Peninsula. This is display by recurring and dated fault scarps formed on granite hills in the Gawler Craton (Twidale and Bourne, 2000a). Most of the scarps are reverse type, while a few others are thrust faults formed at local scale. A study by K.R. Miles (1952a) on northeastern Eyre Peninsulahas has identified surfaces bearing a calcrete duricrust of Pleistocene or Holocene age being affected by faults. A view of one of these offset is seen in an old mine tunnel to actually be a reverse fault type (Dunham, …show more content…
Toward north is a reverse type fault bearing Pleistocene gravel across folded Proterozoic deposit is revealed near Terowie (Love et al., 1995, p. 270). Also confirmed on the north-eastern piedmont of the Flinders Ranges is severe folding of Miocene silcrete and related faulting, furthermore, and in slight magnitude, within the highland (Coats et al, 1969).
On the northern Flinders ranges the east-plunging Mt Babbage thrust has conveyed Mesoproterozoic rock across Late Pleistocene and Holocene alluvia (Love et al., 1995, p. 270). Amid the 1986 quake (Crone et al, 1997), low scarps were created at Marryat River, close Kulgera on the South Australia-Northern Domain fringe. Moving further toward the north in the Tennant Creek region, the quake which took place in 1994 created a succession of low scarps akin to reverse faulting (Crone et al, 1997).
As we move far from the topographic hub of the Flinders Ranges neotectonic deformation become more unobtrusive (Figure 9a). Toward the west, neotectonism is very much recorded on various faults on the upper east Eyre Peninsula (e.g. Crone et al. 2003 and Robert 2007) (Figure 9b), the Yorke