Volcanological and tectono-magnetic evolution of the cadia-forest reefs region, southern Molong volcanic belt, Australia
Squire, RJ (2001) Volcanological and tectono-magnetic evolution of the cadia-forest reefs region, southern Molong volcanic belt, Australia. PhD thesis, University of Tasmania.
The Ordovician to early Early Silurian volcanic successions of the Caclia - Forest Reefs
region in the southern Molong volcanic belt, NSW, comprise the products of at least
two intrabasinal volcanic centres and one or more extrabasinal or basin margin centres.
The Forest Reefs Volcanics include volcaniclastic apron deposits that onlapped and
partially buried the underlying feldspathic turbidites of the Coombing and Wcemalla
Formations. Pillow lavas of the Mt Pleasant Basalt Member are included in the Forest
Reefs Volcanics, and represent the first manifestation of shoshonitic volcanism in the
Cadia - Forest Reefs region, associated with development of a broad volcano.
Shoshonitic magmatism was interrupted by regional uplift during the late Eastonian
( -449-447 Ma), resulting in extensive limestone formation and
synchronous/subsequent emplacement of widespread, but small volume adakitic
intrusions (Copper Hill-type Dacite). Regional subsidence in the Bolindian led to
deposition of the coarse volcaniclastic apron deposits of the upper FRV, which
unconformably overlie the lower FRV. Voluminous shoshonitic magmatism in the early
Llandovery (about 440-437 Ma) resulted in the broadly synchronous emplacement of
the evolved shoshonitic lavas and shallow intrusions of the Nullawonga Latite Member,
and the high-K calc-alkaline to shoshonitic hypabyssal intrusions. Volcanism in the
Cadia - Forest Reefs region was generally non-explosive, and no evidence exists to
support the existence of a large, subaerial collapse caldera. Instead, the shallow
intrusions and lavas of the Nullawonga Latite Member represent the initial (pre-cone)
growth stages of a submarine traehyandcsite cone. Magmatic hydrothermal fluids
associated with emplacement of the evolved, early IJandovery, equigranular intrusions
produced the world-class Cadia porphyry-copper deposits.
The high-K calc-alkaline and shoshonitic volcanic and intrusive rocks in the Cadia -
Forest Reefs region have distinctive arc-type geochemistry very similar to the lavas and
intrusions forming the Pliocene Tavua Caldera in Viti Levu, Fiji. However, the Pliocene
shoshonitic rocks at Tavua Caldera were emplaced following cessation of arc
magmatism when the arc moved into an extensional phase. By analogy with the Pliocene tectonic setting in Fiji, the arc-like signature of the Late Ordovician and early
Llandovery magmas of the Cadia - Forest Reefs region may be due to pre-processing of
the mantle above a subduction zone prior to extension and fragmentation of arc
lithosphere that led to generation of the subduction-modified shoshonite-dominated
magmas. The adakitic Copper Hill-type Dacite may be the due to a change in arc
polarity, involving subduction of hot back-arc basin crust to the west (present-day coordinates)
beneath the arc.
The quartz-rich turbidites of the Adaminaby and Bendoc Groups are juxtaposed against
the feldspathic successions of the Coombing Formation at the southern margin of the
Molong volcanic belt. Differences in stmctural and metamorphic histories, overlapping
biostratigraphic ages (at least Gil to Ea3, -461-448 Ma), abrupt changes in rock-type
along strike and the lack of evidence for mixing or interfingering between the quartzrich
and feldspathic successions, all strongly suggest that the contact between them is a
fault. Similar structural and metamorphic histories are recorded in D3 event of the
Adaminaby and Bendoc Groups and the D1 event of the Coombing Formation.
Therefore, the initial juxtaposition of the quartz-rich and feldspathic successions is
probably recorded by the high-strain fabrics and upper greenschist facies metamorphic
assemblages associated with the D2 event in the Adaminaby and Bendoc Groups. These
structural and metamorphic characteristics are consistent with the juxtaposing structure
being a large extensional fault.
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|Deposited On:||23 Jul 2012 13:33|
|Last Modified:||04 Sep 2012 11:58|
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