Sturt Creek is the remnant of an early Tertiary palaeo-river system that flowed Discussion A useful summary of the modern hydrology and Quaternary stratigraphic framework of Lake Gregory is given by Halse (1990). The catchment is further inland, and today receives less average rainfall (250–500 mm a −1) than the Fitzroy catchment both catchments are strongly monsoonal. Lake Gregory is situated at the terminus of Sturt Creek, a catchment of about 65,000 km 2 on the eastern side of the Kimberley (Fig. The basin is located toward the southern limit of significant monsoon influence, where mean annual precipitation ranges from 500 to 700 mm interannual variability is high, but more than 80% of the precipitation over the catchment occurs between Initiation of monsoon rainfall in the Lake Gregory catchment The Fitzroy catchment is one of the major drainage basins of northwestern Australia, covering an area of 85,000 km 2 (Fig. Stratigraphic evidence of an early reactivation of the Australian monsoon is preserved in alluvial deposits of the Fitzroy River. A distinctive feature of the Australian Initiation of monsoon rainfall in the Fitzroy River catchment Like all low-latitude monsoon regimes, the overall controls on the Australian monsoon are complex, incompletely understood, and are linked to both regional and global scale considerations in both hemispheres (McBride, 1987 Suppiah, 1992 Webster et al., 1998). The Australian summer monsoon forms part of the more extensive southeast Asian monsoon regime, which also affects most of Indonesia, Malaysia, Papua New Guinea and the Solomon Islands (Fig. Section snippets The Australian summer monsoon: present controls and the Late Quaternary record 1), that provide clear evidence for an active monsoon as early as 14 cal ka BP. In this paper, we summarise our findings from the Fitztroy Basin and Lake Gregory, located in monsoonal northwestern Australia (Fig. However, the onset of Holocene reactivation is poorly constrained, largely because most records across northern Australia capture only the mid- to late-Holocene. The Australian monsoon is thought to be broadly paced by global glacial–interglacial variations, with limited activity during the Last Glacial Maximum (LGM), and modest reinvigoration in the Holocene (e.g. In particular, proxy records suggest that monsoon reinvigoration at the end of the last glaciation occurred rapidly despite relatively slow, linear forcing (e.g. Although systematic changes in insolation provide the dominant forcing of planetary monsoon variations, short-lived, sub-Milankovitch events in low-latitude monsoon regimes cannot be interpreted as a direct, linear response to insolation variations (Clemens et al., 1991 Sirocko et al., 1993 Wang et al., 1999). Kutzbach and Street-Perrott, 1985 Kutzbach and Guetter, 1986 Prell and Kutzbach (1987), Prell and Kutzbach (1992)). It is now well established that over glacial–interglacial time scales, differences in low-latitude monsoon activity are strongly linked to Milankovitch insolation variations (e.g.
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