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The Cobar Basin, in central New South Wales, is an Early Devonian extensional basin that formed in the western Lachlan Orogen. The basin was filled with shallow- to deep-water sequences of the Cobar Supergroup and hosts small to large polymetallic deposits. Detrital zircon geochronology and whole-rock geochemical data collected from the Amphitheatre Group of the Cobar Supergroup provide constraints on the history of basin fill and illustrate the dynamic interplay between basin provenance and mineralisation, corresponding to the evolving tectonic regime. Data reveal provenance dissimilarity between the southern and northern parts of the basin. In the south, units of the Amphitheatre Group received abundant detritus from ca 430–410 Ma magmatic rocks situated to the southwest and southeast of the basin. By contrast, the northern successions were predominately sourced from recycled Ordovician basement found to the northwest, north, northeast of the basin, along with contributions associated with the Macquarie Arc. This spatial provenance variation, however, is less significant in the younger formations: the northern and southern sequences both exhibit an increase in older recycled detritus upwards with time. This reflects a progressive modification of basin paleogeography, during the transition from rift phase to sag phase. The rift-phase basin geography is characterised by fault-restricted deposition with predominant sediments derived from local proximal sources. The subsequent sag-phase subsidence exhibits a uniform depositional system with more homogenised basin input. This provenance variation is coeval with the stratigraphically controlled mineralisation features within the Amphitheatre Group successions, implying a provenance influence on mineralisation. Data suggest the different sediment source regions have produced distinct detrital mineral compositions between the major mineral-hosting and mineral-barren formations. The enrichment of some detrital minerals in the mineral-hosting units, such as feldspar, muscovite, Ti-minerals (and carbonate), is suggested to be an important factor for mineralisation in the basin. Detrital zircon geochronology and whole-rock geochemistry illustrate the history of basin fill for the Cobar Basin. Spatial and temporal variation of basin provenance reflects a modification of basin geography, corresponding to the evolving tectonic regimes. The change in basin source regions is one of key controls on the mineralisation within the Cobar Basin. [ABSTRACT FROM AUTHOR]

It is well documented that sediments record geochemical signatures that reflect the composition and tectonic setting of the rocks providing the detritus for them. This is true of the turbidites in the Nambucca Block that record compositions that vary from basaltic to rhyodacitic but are dominantly andesitic to dacitic. They show chondrite and N-MORB patterns, characteristic of calc-alkaline, continental arc rocks, namely light REE (av. La/Yb)N = 6.3) and Th enrichment, Ti, Nb and Ta depletion, and substantial within plate components (Nb/Yb; 0.65–5.16; x = 3.15). Rare occurrences of rocks with intra-oceanic island arc affinities and felsic volcanic rocks showing tectonic fabrics occur, indicating more distal sources contributed detritus. Most detritus in the turbidites has been derived from the calc-alkaline, continental rocks of the Keepit arc, some from the subduction–accretion sequences of the Tablelands Complex. CIA [Al2O3/(Al2O3+Na2O + K2O + CaO)×100] values (48–83; x = 68) indicate that erosion of these arc sequences occurred during glacial, temperate and humid conditions at different times. Further, index of chemical variability values (0.3–1.85; x = 0.85) reveal a compositional maturity and a high percentage of clays in the source rocks suggesting a passive tectonic setting in which minimal uplift and extensive weathering took place. Metasediments in the Nambucca Block record geochemical signatures typical of calc-alkaline, continental, arc rocks. Detritus in metasediments was derived from the Keepit arc and Tablelands Complex, southern New England Orogen. Source rocks were subjected to glacial, temperate and humid conditions at different times. [ABSTRACT FROM AUTHOR]

Dykes are common in the wave-cut platforms along the coast from Newcastle to Sydney. According to some authors, they may be related to the opening of the Tasman Sea that commenced ca 84 Ma ago. However, there are few detailed radiogenic dating and geochemical studies to evaluate this. We attempt to resolve this by K–Ar dating of plagioclase in and geochemical studies of, basaltic dykes intruding Permo-Triassic sequences on the wave-cut platforms and Carboniferous and Permo-Triassic sequences inland. The plagioclase separated from the dykes give K–Ar ages ranging from 266 to 53 Ma with the majority older than 84 Ma indicating that most dykes were emplaced before the Tasman Seafloor formation. The dykes are generally mildly alkaline, high-Ti basalts; fewer are tholeiitic and calc-alkaline, low-Ti basalts. Strongly light rare earth element (LREE)-enriched patterns typify the former and flat, LREE-depleted or slightly to moderately enriched LREE patterns, the latter. High-Ti basalts have ocean-island-basalt-like and low-Ti basalts, calc-alkaline or mid-ocean ridge basalt (MORB)-like patterns. Most high-Ti and some low-Ti basalts show plume-like characteristics, others N-type MORB and arc-like characteristics. Dykes intruding the Carboniferous sequences show a distinct contamination signature that could be crustal or due to subduction-related metasomatism of the subcontinental lithospheric mantle. The sources of the basaltic magmas vary substantially and in places changes with time. All alkali basalts are derived from enriched asthenospheric sources at varying depths (90–147 km) and most tholeiitic, low-Ti basalts have been extracted from asthenospheric and depleted asthenospheric–lithospheric sources indicating substantial compositional heterogeneity of the mantle. Further, Nd model ages varying from Neoproterozoic (940–580 Ma) to Paleozoic (460–370 Ma) suggest variation in the age of mantle sources for the basalts. [ABSTRACT FROM AUTHOR]

The Hastings Block is a weakly cleaved and complexly folded and faulted terrain made up of Devonian, Carboniferous and Permian sedimentary and volcanic rocks. The map pattern of bedding suggests a major boundary exists that divides the Hastings Block into northern and southern parts. Bedding north of this boundary defines an upright box-like Parrabel Anticline that plunges gently northwest. Four cleavage/fold populations are recognised namely: E–W-striking, steeply dipping cleavage S1that is axial surface to gently to moderately E- or W-plunging; F1folds that were re-oriented during the formation of the Parrabel Anticline with less common N–S-trending, steeply dipping cleavage S2, axial surface to gently to moderately N-plunging F2folds; poorly developed NW–SE-striking, steeply dipping cleavage S3axial surface to mesoscopic, mainly NW-plunging F3folds; and finally,a weakly developed NE–SW-striking, steeply dipping S4cleavage formed axial surface to mainly NE-plunging F4. The Parrabel Anticline is considered to have formed during the D3deformation. The more intense development of S2and S3on the western margin of the Northern Hastings Block reflects increasing strain related to major shortening of the sequences adjacent to the Tablelands Complex during the Hunter–Bowen Orogeny. The pattern of multiple deformation we have recorded is inconsistent with previous suggestions that the Hastings Block is part of an S-shaped orocline folded about near vertically plunging axes. [ABSTRACT FROM AUTHOR]

Brittle failure is common in the Devonian to Permian rocks in the Northern Hastings Block (NHB) and is manifested by faults of different orientation and kinematic histories, but the timing of fault movement is not well defined. In this study, faults in the NHB were analysed with the map pattern of cross-cutting faults used to estimate the relative time of movement and relationship to other faults. We defined five episodes of faulting or fault reactivation that affected the NHB. The Yarras Fault System on the southwestern side of the NHB and the Parrabel Fault and related faults on the eastern side of the NHB are the two major fault systems responsible for transporting and rotating the NHB in the late Carboniferous. Faults on the eastern, northeastern and northern part of Parrabel Dome started and stopped moving after emplacement of the Hastings Block and before the intrusion of the Werrikimbe Triassic granitoids. We suggested that the movement on the major bounding faults is related to the accommodation of the NHB to the folding and cleavage development in the adjoining Nambucca Block, and is associated with the earliest part of the Hunter–Bowen Orogeny. Limited dextral movement on the extensions of the Taylors Arm Fault System caused minor displacements in the northeastern part of the NHB during the Late Triassic. Some small faults cut the Triassic granitoids or Triassic Lorne Basin sediments indicating tectonic activity continued post-Triassic. [ABSTRACT FROM PUBLISHER]

New geochemical, metamorphic, and isotopic data are presented from high-pressure metamorphic rocks in the southern New England Orogen (eastern Australia). Conventional and optimal thermobarometry are augmented by U-Pb zircon and 40Ar/39Ar phengite dating to define pressure-temperature-time ( P-T-t) histories for the rocks. The P-T-t histories are compared with competing geodynamic models for the Tasmanides, which can be summarized as (i) a retreating orogen model, the Tasmanides formed above a continuous, west dipping, and eastward retreating subduction zone, and (ii) a punctuated orogen model, the Tasmanides formed by several arc accretion, subduction flip, and/or transference events. Whereas both scenarios are potentially supported by the new data, an overlap between the timing of metamorphic recrystallization and key stages of Tasmanides evolution favors a relationship between a single, long-lived subduction zone and the formation, exhumation, and exposure of the high-pressure rocks. By comparison with the retreating orogen model, the following links with the P-T-t histories emerge: (i) exhumation and underplating of oceanic eclogite during the Delamerian Orogeny, (ii) recrystallization of underplated and exhuming high-pressure rocks at amphibolite facies conditions coeval with a period of rollback, and (iii) selective recrystallization of high-pressure rocks at blueschist facies conditions, reflecting metamorphism in a cooled subduction zone. The retreating orogen model can also account for the anomalous location of the Cambrian-Ordovician high-pressure rocks in the Devonian-Carboniferous New England Orogen, where sequential rollback cycles detached and translated parts of the leading edge of the overriding plate to the next, younger orogenic cycle. [ABSTRACT FROM AUTHOR]

The Cambrian–Ordovician Wagonga Group contains basalts at Melville Point and Barlings Beach, 20 km south of Batemans Bay, New South Wales. At Melville Point, the succession has basal altered basalts overlain by chert and interbedded siliceous mudstone of the Wagonga Group, in turn overlain by turbidites and chert of the Adaminaby Group with a latest Cambrian to earliest Ordovician age. By contrast, at Barlings Beach, basalt is associated with highly disrupted chert (tectonic mélange), various slivers of mudstone and turbidites, and turbidites of the Adaminaby Group. Immobile elements in the basalts show consistent patterns that allow the magmatic affinity and tectonic setting to be determined in spite of pervasive hydrothermal alteration and subsequent lower greenschist facies metamorphism that accompanied strong folding and multiple foliation development. The Melville Point basalts show Ti/V ratios transitional between arc and MORB and therefore may have formed in either a forearc or backarc basin setting. However, these rocks have higher Ti/V ratios, LREE, Th and Nb than found in forearc basalts and are therefore considered to have formed in a backarc basin setting. In contrast to Melville Point, most basalts at Barlings Beach have a geochemical signature distinctive of ocean island settings like those reported from elsewhere in the Wagonga Group. We believe these rocks developed in a Cambrian backarc basin setting. In the Early to Middle Ordovician, much of the ocean basin was inundated by quartzose turbidites followed by basin destruction with accretion/underplating at a Late Ordovician–early Silurian Benambran subduction zone and formation of the Narooma Accretionary Complex. [ABSTRACT FROM AUTHOR]

Structural and K–Ar dating studies of gouge in N–S, NNE and E–W-trending faults in four locations in the Sydney–Hunter region are reported. The fault zones are manifest as joint swarms and highly brecciated zones containing gouge with authigenic illite produced as a result of fluid infiltration. Strike-slip movement accompanied by minor dip-slip, normal movement occurred on the NNE faults, with dip slip on N–S and E–W-trending faults. In this study, gouge from a NE-trending, steep, SE-dipping fault showing dip-slip movement at Cut 10, on the Hunter Expressway and from an E–W-trending, steep south-dipping, normal fault at the Westside Open Cut, Lake Macquarie have been analysed. K–Ar dating of illite and illite–smectite in fractions extracted from fault gouges in areas unaffected by a thermal overprint reveals ages varying from 166 to 119 Ma for the <2 μm and finer fractions, and a mean age ofca120 Ma for the <0.4 μm fraction. In the Sydney area and the Westside Open Cut coal mine, Lake Macquarie, the ages obtained from similar size fractions both for the gouge and for the host rocks are younger (134–76 Ma; av. <0.4 μm = 111 Ma). The data indicate influence of a thermal overprint associated with subsurface magmas emplaced during the early stages of the rifting of eastern Gondwana during the early Cretaceous. [ABSTRACT FROM PUBLISHER]

This study provides new structural data that show that the Adaminaby Group is part of the Narooma accretionary complex and has been overprinted by HT/LP metamorphism associated with Middle Devonian Moruya Suite intrusions. The grade of metamorphism based on Kübler Indices is the same in the Wagonga and Adaminaby Groups at Batemans Bay inferring that these rocks were involved in the same accretionary event. White micas in slates of the Adaminaby Group record apparent K–Ar ages of 384.6 ± 7.9 Ma and 395.8 ± 8.1 Ma. These ages are believed to represent the age of Middle to Upper Devonian Buckenbowra Granodiorite. Kübler Index values indicate lower epizonal (greenschist facies) metamorphic conditions and are not influenced by heating in metamorphic aureoles of the plutons. All b cell lattice parameter values are characteristic of intermediate pressure facies conditions although they are lower in the metamorphic aureole of the Buckenbowra Granodiorite than in the country rock, defining two areas with dissimilar baric conditions. East of the Buckenbowra Granodiorite, b cell lattice parameter values outside the contact aureole (x = 9.033 Å; n = 8) indicate P = 4 kb, and assuming a temperature of 300°C, infer a depth of burial of approximately 15 km for these rocks with a geothermal gradient of 20°C/km. In the metamorphic aureole of the Buckenbowra Granodiorite, b cell lattice parameter values (x = 9.021 Å; n = 41) indicate P = 3.1 kb inferring exhumation of the Adaminaby Group rocks to a depth of approximately 11 km prior to intrusion. A geothermal gradient of 36°C/km operated in the aureole during intrusion. An extensional back-arc environment prevailed in the Adaminaby Group during the Middle to Upper Devonian. [ABSTRACT FROM AUTHOR]

White micas in slates from an imbricated sequence of deformed turbidites, and clast-in-matrix-melanges that form the Narooma accretionary complex at Batemans Bay, record apparent 40Ar/39Ar whole rock ages in the range 450 to 500 Ma, with intermediate-temperature average ages of 471 ± 13 Ma and 476 ± 11 Ma (2 standard deviations). By contrast, two K-Ar whole rock ages are 430.9 ± 8.6 Ma and 449.2 ± 9.0 Ma. Fractions (<2, 3-5 and 10-20 μm) from the same samples show a progressive increase in age with grainsize (<2 μm = 413.1 ± 8.3-404.7 ± 8.1 Ma; 3-5 μm = 417.1 ± 8.3 Ma; 10-20 μm = 434 ± 8.6-437.5 ± 8.8 Ma 2 standard deviations). The older whole rock 40Ar/39Ar ages are attributed to recoil loss of 39Ar. The cleavage forming event is believed to have occurred at ∼460-440 Ma (Upper Ordovician to Lower Silurian). The finest fractions possibly record a younger thermal event at approximately 413 Ma. Kubler Index values obtained from the Wagonga and Adaminaby Groups indicate lower epizonal (greenschist facies) metamorphic conditions. b0 lattice parameter values (x = 9.033; n = 21) are characteristic of the intermediate pressure facies series. Assuming a temperature of approximately 300°C and P = 4 kb suggests a depth of burial of approximately 15 km was reached by these rocks and that a geothermal gradient of 20°C/km operated during subduction. [ABSTRACT FROM AUTHOR]

The stability of pumpellyite + actinolite or riebeckite + epidote + hematite (with chlorite, albite, titanite, quartz and H2O in excess) mineral assemblages in LTMP metabasite rocks is strongly dependent on bulk composition. By using a thermodynamic approach (THERMOCALC), the importance of CaO and Fe2O3 bulk contents on the stability of these phases is illustrated using P–T and P–X phase diagrams. This approach allowed P–T conditions of ∼4.0 kbar and ∼260 °C to be calculated for the growth of pumpellyite + actinolite or riebeckite + epidote + hematite assemblages in rocks containing variable bulk CaO and Fe2O3 contents. These rocks form part of an accretionary wedge that developed along the east Australian margin during the Carboniferous–Triassic New England Orogen. P–T and P–X diagrams show that sodic amphibole, epidote and hematite will grow at these conditions in Fe2O3-saturated (6.16 wt%) metabasic rocks, whereas actinolite and pumpellyite will be stable in CaO-rich (10.30 wt%) rocks. With intermediate Fe2O3 (∼3.50 wt%) and CaO (∼8.30 wt%) contents, sodic amphibole, actinolite and epidote can coexist at these P–T conditions. For Fe2O3-saturated rocks, compositional isopleths for sodic amphibole (Al3+ and Fe3+ on the M2 site), epidote (Fe3+/Fe3+ + Al3+) and chlorite (Fe2+/Fe2+ + Mg) were calculated to evaluate the efficiency of these cation exchanges as thermobarometers in LTMP metabasic rocks. Based on these calculations, it is shown that Al3+ in sodic amphibole and epidote is an excellent barometer in chlorite, albite, hematite, quartz and titanite buffered assemblages. The effectiveness of these barometers decreases with the breakdown of albite. In higher- P stability fields where albite is absent, Fe2+-Mg ratios in chlorite may be dependent on pressure. The Fe3+/Al and Fe2+/Mg ratios in epidote and chlorite are reliable thermometers in actinolite, epidote, chlorite, albite, quartz, hematite and titanite buffered assemblages. [ABSTRACT FROM AUTHOR]

Structural studies in the Sydney region have revealed the presence of vertical to near-vertical, north-northeast-striking faults that are manifest as joint swarms and highly brecciated zones in which gouge of varying thickness is developed. Strike-slip movement accompanied by minor dip-slip, normal movement occurred on these faults. Timing of movement on these faults by K-Ar dating of illite and illite-smectite in fractions extracted from fault gouges, was attempted. These dates were compared with dates obtained from the host-rocks. K-Ar ages determined from the 2-10 μm to <0.1 μm fractions produced from the gouge and host-rocks, range from 159.5 ± 3.2 to 106.6 ± 2.1 Ma (n = 26). In <0.5 μm fractions extracted from the gouges that are less contaminated by detrital phases, K-Ar ages vary from 138 ± 4.4 to 106.5 ± 2.1 Ma (mean 121 Ma; n = 6) which are similar to ages obtained from host-rocks in the Sydney region. The similarity in age between the host rocks and gouge suggests that the K-Ar system has been reset. The resetting is attributed to a thermal event at ca 120 Ma related to the underplating of felsic intrusions associated with early stages of breakup of East Gondwana. Subsequent to this event, dykes of Early Eocene age (K-Ar whole-rock: 51.0 ± 1.1 Ma) exploited north-northeast-striking faults and subsequently developed brecciated margins. These observations and the fact that gouge formed before the thermal event suggests that movement took place on north-northeast-striking faults prior to 120 Ma and after 51 Ma. [ABSTRACT FROM AUTHOR]

Gouges formed in north-northeast-striking fault zones of the Sydney region and associated host-rocks were investigated by XRD, SEM, TEM and optical microscopy in order to determine their mineralogy. XRD studies reveal that illite, illite-smectite, kaolinite, quartz and dickite are present in varying proportions. Kubler Indices (0.54-0.71) and low smectite contents in illite-smectite (<10% smectite) in most gouges and host-rocks, indicate the assemblages formed at temperatures between 120 and 150°C. Those at the Heathcote Road, Lucas Heights location formed at lower temperatures (<100°C). SEM images of the clays in host sublitharenites and gouges show a variety of sizes and habits that reflect variations in fluid temperature and rate of crystallisation. SEM studies also reveal that detrital quartz grains exhibit overgrowths and etch pits of varying density, size and shape that are more strongly developed in the gouges than in the host-rocks. These features are thought to be related to higher fluid/rock ratios brought about by major ingress of fluids into the fault zones. The mineral assemblage present and the features exhibited are believed to have formed in response to a thermal event associated with the early stages of the breakup of Gondwana. [ABSTRACT FROM AUTHOR]

Serpentinites along the boundaries of the Hastings Block, southern New England Orogen, eastern Australia, contain S, C and C' structures that provide information on the kinematic history of faults bounding the block. The serpentinite bodies at Yarras on the western boundary of the Hastings Block within the Ralfes Creek, Taylors Creek and Old Highway-Yarras Mountain Trail Faults display dominantly sinistral strike-slip or oblique-slip movement. Serpentinite bodies between these faults record dextral strike-slip and oblique-slip movement histories as well as sinistral strike-slip or oblique-slip and rare normal, dip-slip movement. The Mt George Serpentinite consists of a northeast-oriented section folded and displaced by movement on a west-northwest section of the Peel-Manning Fault System. Serpentinite structures suggest the west-northwest section initially underwent dextral strike-slip, which reoriented the northeast-oriented section, and subsequently sinistral strike-slip movement. Preliminary studies of serpentinites elsewhere around the periphery of the Hastings Block indicate localised effects due to readjustment of the block during its interaction with the Nambucca Block on its northern margin. The structures observed in the serpentinites are thought to have occurred during and after the Hunter-Bowen Orogeny and prior to stitching of the accretionary-subduction and forearc by the 228 Ma Werrikimbe Caldera. [ABSTRACT FROM AUTHOR]

The Tia Complex is located in the southern New England Orogen of eastern Australia and provides a detailed record of the structural-metamorphic evolution of an ancient accretionary prism. This record is characterized by six stages of deformation that were accompanied by a transition from moderate-pressure-low-temperature to low-pressure-high-temperature metamorphism. The composition of jadeitic pyroxene (subduction), magnesioriebeckite (exhumation), and actinolite (heating) have been used to model P-T conditions during these structural events, which range from P = 6.3-6.7 kbar and T = 320-350°C (subduction) to 1.5-2.0 kbar and 400-420°C (heating). On the basis of new structural and metamorphic data combined with preexisting age data, the evolution of this accretionary prism can be divided into two main stages: (1) blueschist formation and exhumation and (2) elevated heat flow and anatexis. To explain these features, a new model is presented that requires (1) wedge underthrusting and rear wedge extension associated with a stationary subduction hinge and (2) subduction hinge migration resulting in the relocation of the accretionary wedge onto the upper plate and heating during exposure to the mantle wedge. To explain the event chronology preserved in the Tia Complex, both extensional collapse and subduction hinge migration models are required. [ABSTRACT FROM AUTHOR]

40Ar/39Ar dating of slate and phyllite in the Nambucca Block, southern New England Orogen, indicates that deformation took place between 264 and 260 Ma. These data further show that indentation of the Early Permian turbidite successions by the southward-moving Coffs Harbour Orocline ceased at this time. Folding of the Sakmarian to Sarginian sequences in the Silver Spur Basin (294.6 - 275.6 Ma) during the megafolding event constrains the formation of the Texas Orocline to be post-ca 276 Ma. The presence of brachiopod faunas indicates that orocline formation commenced in the early Kungurian (ca 273 Ma) during the early stages of the Hunter - Bowen Orogeny. Thus, development of the Texas and Coffs Harbour Oroclines took place within a period of 13 million years, from 273 to 260 Ma. Oblique convergence is believed to be responsible for the formation of the Texas and Coffs Harbour Oroclines and associated constrictional structures during the Hunter - Bowen Orogeny. Slip on a dextral, strike-slip fault formed during convergence, buckled and rotated the meridional-trending arc - forearc - subduction complex to form north-northwest-trending, Z-shaped megafolds. [ABSTRACT FROM AUTHOR]

Carboniferous to Lower Permian successions along the western border of the Tamworth Belt between Wallabadah and Muswellbrook were remapped to clarify the stratigraphy and establish a boundary between the Werrie and Rouchel blocks. The boundary, located at the Waverley Fault, separates Carboniferous sequences containing different formations and volcanic members. SHRIMP AS3 dating of volcanic members indicates that successions within the Rouchel and Gresford blocks were deposited, uplifted and eroded at different times. The lacustrine Woodton Formation in the Werrie block, previously considered Carboniferous, is earliest Permian (Asselian) from palaeobotanical and SHRIMP AS3 evidence. Stratigraphic and palaeoenvironmental differences between the Werrie and Rouchel blocks suggest that they were not directly juxtaposed during the greater part of the Carboniferous, supporting palaeomagnetic evidence that blocks within the Tamworth Belt are allochthonous. Superposition of the western extremity of the Waverley Fault by Lower Permian (Sakmarian) formations and intrusion of folded and faulted Devonian to Lower Permian successions by the Barrington Tops Granodiorite ( ca 280 Ma) indicate that the Werrie, Rouchel and Gresford blocks were subjected to tectonism before the Late Permian Hunter – Bowen Orogeny. [ABSTRACT FROM AUTHOR]

Serpentinite mélange in the Peel-Manning Fault System, southern New England Fold Belt hosts tectonic blocks of varying size and lithology. One of the largest occurs at Woodsreef, northern New South Wales, as multiply deformed amphibole schists recording at least three phases of deformation (D1-D3). They have a peralkaline, composition (molecular Na2O+K2O = 0.083-0.189; Al2O3 = 0.046–0.130) and contain aegirine, quartz, albite, arfvedsonite and less common actinolite, neptunite, aenigmatite and bafertisite, as well as relict pre-D1 aegirine. The Zr/TiO2 and Nb/Y ratios suggest that the protoliths had originally basaltic to basaltic andesite composition, indicating that they have been altered to a rock of peralkaline composition. Chondrite normalised patterns ((Ce/Yb)N = 4.98-9.36), Hf/3-Th-Ta, Hf/3-Th-Nb/16 and Y/15-La/10-Nb/8 discrimination diagrams, and rock/MORB plots indicate that the protoliths had a calc-alkaline, are composition. 143Nd/144Nd data (∈Nd(500) = 2.8-3.3: -4.8; ∈Nd(500) = 2.0-2.5; -5.8) imply that they have been derived from isotopically mildly depleted and enriched sources. Single-grain 40Ar-39Ar dating of felsic and mafic fractions from one sample, produces ages of 1200–1100 Ma (albite-quartz vein) and 335.2 ± 2.1 Ma, 332 ± 3.7Ma and 291 ± 3.7Ma (arfvedsonite-rich matrix). The Neoproterozoic age obtained from the felsic fraction is attributed to the presence of excess 40Ar in quartz and albite, and the 291 Ma age to partial resetting. The 335-332 Ma ages are interpreted as cooling ages related to uplift after subduction. The basalts and basaltic andesites underwent alteration either within a volcanic pile or during subduction after collision with a ?west-dipping subduction zone at the proto-Gondwana margin. With continuing subduction, they were recrystallised and deformed in the deeper levels of the subduction zone, producing aegirine with up to 38% jadeite in solid solution. Replacement of the high-P assemblages by lower P/high-T arfvedsonite-bearing assemblages then took place during uplift at ca 334 Ma. [ABSTRACT FROM AUTHOR]

Geological mapping in the Carroll–Nandewar region near the northwestern margin of the Tamworth Belt has identified an Upper Carboniferous to Lower Permian succession, the Willuri Formation, containing coarse volcaniclastic sediments and interbedded dacitic to rhyolitic pyroclastics, lavas and a possible dome or coulée. The Currangandi Group (new) accommodates Upper Carboniferous volcaniclastic formations in the northern Tamworth Belt, including the Willuri Formation. Volcanic rocks in the Willuri Formation are distributed in four stratigraphically distinct, intertonguing or overlapping packages: the Kaputar, Piney Range, Tulcumba and Gunnan packages. According to SHRIMP (AS3) dating most of the succession ranges in age from ca 320 to ca 308 Ma (Namurian–Westphalian). Dacitic and rhyolitic lavas, apparently in sequence with the succession on the northwestern part of Tulcumba Ridge, are 297–287 Ma or younger (Early Permian). They appear to disconformably overlie the Carboniferous succession and could be either part of the Willuri Formation or related to the Boggabri Volcanics. Volcanic centres near Maules Creek (Kaputar centre) and Wean (Wean centre) appear to have been the sources for volcanics in the Kaputar package and most parts of the Rocky Creek region to the northeast, and the Tulcumba and probably the Piney Range packages, respectively. In the Gunnan package a single major ignimbrite was derived from a volcanic centre in the Werrie pyroclastic field, but the provenance of other pyroclastics is unknown. Correlations based on SHRIMP ages and the distribution of pyroclastics indicate that the Willuri Formation is equivalent to most of the Currabubula Formation in the Werrie Syncline, and to the Rocky Creek Conglomerate and Lark Hill Formation in the Rocky Creek region. Boundaries of the Werrie and Rocky Creek pyroclastic fields are adjusted to incorporate a new pyroclastic field based on the Wean volcanic centre and covering the Tulcumba and Piney Range packages of the Willuri Formation. [ABSTRACT FROM AUTHOR]

Structural studies of Lower Permian sequences exposed on wave-cut platforms within the Nambucca Block, indicate that one to two ductile and two to three brittle – ductile/brittle events are recorded in the lower grade (sub-greenschist facies) rocks; evidence for four, possibly five, ductile and at least three brittle – ductile/brittle events occurs in the higher grade (greenschist facies) rocks. Veins formed prior to the second ductile event are present in some outcrops. Further, the studies reveal a change in fold style from west-southwest-trending, open, south-southeast-verging, inclined folds (F0 1 ) at Grassy Head in the south, to east-northeast-trending, recumbent, isoclinal folds (F0 1 ; F0 2 ) at Nambucca Heads to the north, suggesting that strain increases towards the Coffs Harbour Block. A solution cleavage formed during D1 in the lower grade rocks and cleavages defined by neocrystalline white mica developed during D1 and D2 in the higher grade rocks. South- to south-southwest-directed tectonic transport and north–south shortening operated during these earlier events. Subsequently, north-northeast-trending, open, upright F2 3 folds and inclined, northwest-verging, northeast-trending F2 4 folds developed with poorly to moderately developed axial planar, crenulation cleavage (S3 and S4 ) formed by solution transfer processes. These folds formed heterogeneously in S2 throughout the higher grade areas. Later northeast–southwest shortening resulted in the formation of en échelon vein arrays and kink bands in both the lower and higher grade rocks. Shortening changed to east-northeast–west-southwest during later north-northeast to northeast, dextral, strike-slip faulting and then to approximately northwest–southeast during the formation of... [ABSTRACT FROM AUTHOR]

Geochemical studies of volcanic rocks in the Gamilaroi terrane and Calliope Volcanic Assemblage, New England Fold Belt, eastern Australia, indicate that the setting in which these rocks formed changed in both space and time. The Upper Silurian to Middle Devonian basalts of the Gamilaroi terrane show flat to slightly light rare-earth element (LREE) depleted chondrite normalised patterns, depletion of high field strength elements (HFSE) relative to N-MORB, low Ti/V and high Ti/Zr ratios, high Ni, Cr and large-ion lithophile element (LILE) contents, features characteristic of intra-oceanic island arc basaltic magmas. They are associated with low-K, less mafic volcanics, showing moderate LREE enrichment, low Nb and Y contents and Rb/Zr ratios. The depletion of HFSE in the basalts indicates that the magmas were derived from a refractory source in a supra-subduction zone setting. The presence of such a zone implies that the arc was associated with a backarc basin, the location of which was to the west where a wide backarc region existed from the Middle Silurian. This polarity of arc and backarc basin suggests that the subduction zone dipped to the west. In contrast to their older counterparts, Middle to Upper Devonian basalts of the Gamilaroi terrane have MORB-like chondrite normalised patterns and higher Ti and lower LILE contents. Moreover, they have low Ti/Zr ratios and MORB-like Ti/V ratios and HFSE contents, features typical of backarc basins. Dolerites of the Gamilaroi terrane also have predominantly backarc basin signatures. These features suggest that both the basalts and dolerites have been emplaced in an extensional environment produced during the rifting of the intra-oceanic island arc lithosphere. A progressive increase in Ti/V ratios, and TiO2 and Fe2 O3 contents at constant MgO, of stratigraphically equivalent basalts, towards the north-northwest part of the belt, is consistent with either greater extension to the north... [ABSTRACT FROM AUTHOR]

Focuses on the geology of the Lachlan Fold Belt in Australia. Information on the Lachlan Fold Belt; In-depth look at the Narooma Accretionary Complex; What has been indicated of the Bogolo Formation.