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Journal articles on the topic 'Lachlan Orogen'

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Author: Grafiati

Published: 10 December 2022

Last updated: 20 February 2023

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1

Glen, R. A., S. Meffre, and R. J. Scott. "Benambran Orogeny in the Eastern Lachlan Orogen, Australia." Australian Journal of Earth Sciences 54, no. 2-3 (March 2007): 385–415. http://dx.doi.org/10.1080/08120090601147019.

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2

Collins, William J., Hui-Qing Huang, Peter Bowden, and A. I. S. Kemp. "Repeated S–I–A-type granite trilogy in the Lachlan Orogen and geochemical contrasts with A-type granites in Nigeria: implications for petrogenesis and tectonic discrimination." Geological Society, London, Special Publications 491, no. 1 (May 3, 2019): 53–76. http://dx.doi.org/10.1144/sp491-2018-159.

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AbstractThe classical S–I–A-type granites from the Lachlan Orogen, SE Australia, formed as a tectonic end-member of the accretionary orogenic spectrum, the Paleozoic Tasmanides. The sequence of S- to I- to A-type granite is repeated at least three times. All the granites are syn-extensional, formed in a dominantly back-arc setting behind a single, stepwise-retreating arc system between 530 and 230 Ma. Peralkaline granites are rare. Systematic S–I–A progressions indicate the progressive dilution of an old crustal component as magmatism evolved from arc (S-type) to proximal back-arc (I-type) to distal back-arc (A-type) magmatism. The alkaline and peralkaline A-type Younger granites of Nigeria were generally hotter and drier than the Lachlan A-type granites and were emplaced into an anhydrous Precambrian basement during intermittent intracontinental rifting. This geodynamic environment contrasts with the distal back-arc setting of the Lachlan A-type granites, where magmatism migrated rapidly across the orogen. Tectonic discrimination diagrams are inappropriate for the Lachlan granites, placing them in the wrong settings. Only the peralkaline Narraburra suite of the Lachlan Orogen fits the genuine ‘within-plate’ setting of the Nigerian A-type granites. Such discrimination diagrams require re-evaluation in the light of an improved modern understanding of tectonic processes, particularly the role of extensional tectonism and its geodynamic drivers.

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3

Wilkins, Colin, and Mike Quayle. "Structural Control of High-Grade Gold Shoots at the Reward Mine, Hill End, New South Wales, Australia." Economic Geology 116, no. 4 (June 1, 2021): 909–35. http://dx.doi.org/10.5382/econgeo.4807.

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Abstract The Reward mine at Hill End hosts structurally controlled orogenic gold mineralization in moderately S plunging, high-grade gold shoots located at the intersection between a late, steeply W dipping reverse fault zone and E-dipping, bedding-parallel, laminated quartz veins (the Paxton’s vein system). The mineralized bedding-parallel veins are contained within the middle Silurian to Middle Devonian age, turbidite-dominated Hill End trough forming part of the Lachlan orogen in New South Wales. The Hill End trough was deformed in the Middle Devonian (Tabberabberan orogeny), forming tight, N-S–trending, macroscopic D2 folds (Hill End anticline) with S2 slaty cleavage and associated bedding-parallel veins. Structural analysis indicates that the D2 flexural-slip folding mechanism formed bedding-parallel movement zones that contained flexural-slip duplexes, bedding-parallel veins, and saddle reefs in the fold hinges. Bedding-parallel veins are concentrated in weak, narrow shale beds between competent sandstones with dip angles up to 70° indicating that the flexural slip along bedding occurred on unfavorably oriented planes until fold lockup. Gold was precipitated during folding, with fluid-flow concentrated along bedding, as fold limbs rotated, and hosted by bedding-parallel veins and associated structures. However, the gold is sporadically developed, often with subeconomic grades, and is associated with quartz, muscovite, chlorite, carbonates, pyrrhotite, and pyrite. East-west shortening of the Hill End trough resumed during the Late Devonian to early Carboniferous (Kanimblan orogeny), producing a series of steeply W dipping reverse faults that crosscut the eastern limb of the Hill End anticline. Where W-dipping reverse faults intersected major E-dipping bedding-parallel veins, gold (now associated with galena and sphalerite) was precipitated in a network of brittle fractures contained within the veins, forming moderately S plunging, high-grade gold shoots. Only where major bedding-parallel veins were intersected, displaced, and fractured by late W-dipping reverse faults is there a potential for localization of high-grade gold shoots (>10 g/t). A revised structural history for the Hill End area not only explains the location of gold shoots in the Reward mine but allows previous geochemical, dating, and isotope studies to be better understood, with the discordant W-dipping reverse faults likely acting as feeder structures introducing gold-bearing fluids sourced within deeply buried Ordovician volcanic units below the Hill End trough. A comparison is made between gold mineralization, structural style, and timing at Hill End in the eastern Lachlan orogen with the gold deposits of Victoria, in the western Lachlan orogen. Structural styles are similar where gold mineralization is formed during folding and reverse faulting during periods of regional east-west shortening. However, at Hill End, flexural-slip folding-related weakly mineralized bedding-parallel veins are reactivated to a lesser degree once folds lock up (cf. the Bendigo zone deposits in Victoria) due to the earlier effects of fold-related flattening and boudinage. The second stage of gold mineralization was formed by an array of crosscutting, steeply W dipping reverse faults fracturing preexisting bedding-parallel veins that developed high-grade gold shoots. Deformation and gold mineralization in the western Lachlan orogen started in the Late Ordovician to middle Silurian Benambran orogeny and continued with more deposits forming in the Bindian (Early Devonian) and Tabberabberan (late Early-Middle Devonian) orogenies. This differs from the Hill End trough in the eastern Lachlan orogen, where deformation and mineralization started in the Tabberabberan orogeny and culminated with the formation of high-grade gold shoots at Hill End during renewed compression in the early Carboniferous Kanimblan orogeny.

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4

VandenBerg, A. H. M. "Timing of orogenic events in the Lachlan Orogen." Australian Journal of Earth Sciences 46, no. 5 (October 1999): 691–701. http://dx.doi.org/10.1046/j.1440-0952.1999.00738.x.

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5

Glen, R. A., E. Belousova, and W. L. Griffin. "Different styles of modern and ancient non-collisional orogens and implications for crustal growth: a Gondwanaland perspective." Canadian Journal of Earth Sciences 53, no. 11 (November 2016): 1372–415. http://dx.doi.org/10.1139/cjes-2015-0229.

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Non-collisional, convergent margin orogens are generally called accretionary orogens, although there may not have been horizontal accretion across the plate boundary. We revive the term non-collisional orogen and use a Gondwanaland perspective to discuss different types. On the northern margin of the Australian Plate, the New Guinea non-collisional, accretionary orogen was formed by large-scale terrane accretion across an advancing plate margin. On the eastern margin, the Southwest Pacific Orogen is a non-collisional and non-accretionary orogen, involving virtually no horizontal transfer of material across its eastward-retreating plate boundary. In the Tasmanides, the Lachlan Orogen, commonly described as an accretionary orogen, is another non-collisional, non-accretionary orogen developed behind the plate margin after major Cambrian rollback, with resultant backarc basins filled mainly by quartz-rich turbidites subsequently recycled. The outboard New England Orogen is a non-collisional but accretionary orogen, marked by the frontal accretion of continental margin arc detritus, subsequently recycled into younger arcs. The Permian to Cretaceous Rangitata Orogen of New Zealand is an ?oblique non-collisional, accretionary orogen in which Permian–Triassic sediments of the accretionary wedge have no link with inboard (near) arc terranes. Late Jurassic to Cretaceous parts were sourced by a combination of first cycle volcanogenic detritus passing through the forearc basin together with recycling of the exhumed parts of the wedge. All non-collisional orogens involve continental growth, but only the New England Orogen and to a lesser extent the New Guinea Orogen involve significant crustal growth.

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6

SPAGGIARI, C. V., D. R. GRAY, and D. A. FOSTER. "Lachlan Orogen subduction-accretion systematics revisited." Australian Journal of Earth Sciences 51, no. 4 (August 2004): 549–53. http://dx.doi.org/10.1111/j.1400-0952.2004.01073.x.

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7

McKibbin, Seann J., Bill Landenberger, and C. Mark Fanning. "First magmatism in the New England Batholith, Australia: forearc and arc–back-arc components in the Bakers Creek Suite gabbros." Solid Earth 8, no. 2 (April 5, 2017): 421–34. http://dx.doi.org/10.5194/se-8-421-2017.

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Abstract. The New England Orogen, eastern Australia, was established as an outboard extension of the Lachlan Orogen through the migration of magmatism into forearc basin and accretionary prism sediments. Widespread S-type granitic rocks of the Hillgrove and Bundarra supersuites represent the first pulse of magmatism, followed by I- and A-types typical of circum-Pacific extensional accretionary orogens. Associated with the former are a number of small tholeiite–gabbroic to intermediate bodies of the Bakers Creek Suite, which sample the heat source for production of granitic magmas and are potential tectonic markers indicating why magmatism moved into the forearc and accretionary complexes rather than rifting the old Lachlan Orogen arc. The Bakers Creek Suite gabbros capture an early ( ∼ 305 Ma) forearc basalt-like component with low Th ∕ Nb and with high Y ∕ Zr and Ba ∕ La, recording melting in the mantle wedge with little involvement of a slab flux and indicating forearc rifting. Subsequently, arc–back-arc like gabbroic magmas (305–304 Ma) were emplaced, followed by compositionally diverse magmatism leading up to the main S-type granitic intrusion ( ∼ 290 Ma). This trend in magmatic evolution implicates forearc and other mantle wedge melts in the heating and melting of fertile accretion complex sediments and relatively long ( ∼ 10 Myr) timescales for such melting.

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8

Glen, R. A., and J. L. Walshe. "Cross‐structures in the Lachlan Orogen: The Lachlan Transverse Zone example." Australian Journal of Earth Sciences 46, no. 4 (August 1999): 641–58. http://dx.doi.org/10.1046/j.1440-0952.1999.00734.x.

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9

Mortimer, N., J. M. Palin, W. J. Dunlap, and F. Hauff. "Extent of the Ross Orogen in Antarctica: new data from DSDP 270 and Iselin Bank." Antarctic Science 23, no. 3 (February 8, 2011): 297–306. http://dx.doi.org/10.1017/s0954102010000969.

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AbstractThe Ross Sea is bordered by the Late Precambrian–Cambrian Ross–Delamerian Orogen of East Antarctica and the more Pacific-ward Ordovician–Silurian Lachlan–Tuhua–Robertson Bay–Swanson Orogen. A calcsilicate gneiss from Deep Sea Drilling Project 270 drill hole in the central Ross Sea, Antarctica, gives a U-Pb titanite age of 437 ± 6 Ma (2σ). This age of high-grade metamorphism is too young for typical Ross Orogen. Based on this age, and on lithology, we propose a provisional correlation with the Early Palaeozoic Lachlan–Tuhua–Robertson Bay–Swanson Orogen, and possibly the Bowers Terrane of northern Victoria Land. A metamorphosed porphyritic rhyolite dredged from the Iselin Bank, northern Ross Sea, gives a U-Pb zircon age of 545 ± 32 Ma (2σ). The U-Pb age, petrochemistry, Ar-Ar K-feldspar dating, and Sr and Nd isotopic ratios indicate a correlation with Late Proterozoic–Cambrian igneous protoliths of the Ross Orogen. If the Iselin Bank rhyolite is not ice-rafted debris, then it represents a further intriguing occurrence of Ross basement found outside the main Ross–Delamerian Orogen.

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10

Glen, R. A. "Palaeomagnetism and Terranes in the Lachlan Orogen." Exploration Geophysics 24, no. 2 (June 1993): 247–55. http://dx.doi.org/10.1071/eg993247.

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11

Gray, D. R., D. A. Foster, and F. P. Bierlein. "Geodynamics and metallogeny of the Lachlan Orogen." Australian Journal of Earth Sciences 49, no. 6 (December 2002): 1041–56. http://dx.doi.org/10.1046/j.1440-0952.2002.00962.x.

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12

Foster, D. A., D. R. Gray, and A. H. M. Vandenberg. "Discussion and Reply: Timing of orogenic events in the Lachlan Orogen." Australian Journal of Earth Sciences 47, no. 4 (August 2000): 813–22. http://dx.doi.org/10.1046/j.1440-0952.2000.00811.x.

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13

Spaggiari, Catherine V., David R. Gray, and David A. Foster. "Ophiolite accretion in the Lachlan Orogen, Southeastern Australia." Journal of Structural Geology 26, no. 1 (January 2004): 87–112. http://dx.doi.org/10.1016/s0191-8141(03)00084-1.

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14

Glen, R. A. "Thrusts and thrust-associated mineralization in the Lachlan Orogen." Economic Geology 90, no. 6 (October 1, 1995): 1402–29. http://dx.doi.org/10.2113/gsecongeo.90.6.1402.

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15

Bierlein, Frank P., David R. Gray, and David A. Foster. "Metallogenic relationships to tectonic evolution – the Lachlan Orogen, Australia." Earth and Planetary Science Letters 202, no. 1 (August 2002): 1–13. http://dx.doi.org/10.1016/s0012-821x(02)00757-4.

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16

Bierlein, Frank P., and Andy R. Wilde. "Preface: Tectonics to mineral discovery—deconstructing the Lachlan Orogen." Mineralium Deposita 42, no. 5 (April 11, 2007): 433–34. http://dx.doi.org/10.1007/s00126-007-0136-4.

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17

Schaap, Thomas A., Sebastien Meffre, Joanne M. Whitakker, Matthew J. Cracknell, and Michael Roach. "Modelling the Palaeozoic tectonic evolution of the Lachlan Orogen." ASEG Extended Abstracts 2019, no. 1 (November 11, 2019): 1–5. http://dx.doi.org/10.1080/22020586.2019.12073123.

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18

Spaggiari, C. V., D. R. Gray, D. A. Foster, and C. M. Fanning. "Occurrence and significance of blueschist in the southern Lachlan Orogen." Australian Journal of Earth Sciences 49, no. 2 (April 2002): 255–69. http://dx.doi.org/10.1046/j.1440-0952.2002.00915.x.

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19

Bierlein, F. P., and S. McKnight. "POSSIBLE INTRUSION-RELATED GOLD SYSTEMS INTHE WESTERN LACHLAN OROGEN, SOUTHEAST AUSTRALIA." Economic Geology 100, no. 2 (March 1, 2005): 385–98. http://dx.doi.org/10.2113/gsecongeo.100.2.385.

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20

Direen, Nicholas G., Patrick Lyons, Russell J. Korsch, and Richard A. Glen. "Integrated geophysical appraisal of crustal architecture in the eastern Lachlan Orogen." ASEG Extended Abstracts 2001, no. 1 (December 2001): 1–5. http://dx.doi.org/10.1071/aseg2001ab030.

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21

Spaggiari, C. V., D. R. Gray, and D. A. Foster. "Blueschist metamorphism during accretion in the Lachlan Orogen, south-eastern Australia." Journal of Metamorphic Geology 20, no. 8 (October 21, 2002): 711–26. http://dx.doi.org/10.1046/j.1525-1314.2002.00405.x.

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22

Direen, Nicholas G., Lyons Patrick, J. Korsch Russell, and A. Glen Richard. "Integrated Geophysical Appraisal of Crustal Architecture in the Eastern Lachlan Orogen." Exploration Geophysics 32, no. 3-4 (September 2001): 252–62. http://dx.doi.org/10.1071/eg01252.

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23

FONTAINE, F. R., H. TKALCIC, and B. L. N. KENNETT. "Crustal complexity in the Lachlan Orogen revealed from teleseismic receiver functions." Australian Journal of Earth Sciences 60, no. 3 (April 2013): 413–30. http://dx.doi.org/10.1080/08120099.2013.787646.

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24

Spaggiari, C. V., D. R. Gray, and D. A. Foster. "Formation and emplacement of the Dolodrook serpentinite body, Lachlan Orogen, Victoria." Australian Journal of Earth Sciences 50, no. 5 (October 2003): 709–23. http://dx.doi.org/10.1111/j.1440-0952.2003.01021.x.

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25

Hough, Megan A., Frank P. Bierlein, and Andy R. Wilde. "A review of the metallogeny and tectonics of the Lachlan Orogen." Mineralium Deposita 42, no. 5 (July 4, 2006): 435–48. http://dx.doi.org/10.1007/s00126-006-0073-7.

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26

Adams, C. J., J. D. Bradshaw, and T. R. Ireland. "Provenance connections between late Neoproterozoic and early Palaeozoic sedimentary basins of the Ross Sea region, Antarctica, south-east Australia and southern Zealandia." Antarctic Science 26, no. 2 (July 18, 2013): 173–82. http://dx.doi.org/10.1017/s0954102013000461.

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AbstractThick successions of turbidites are widespread in the Ross–Delamerian and Lachlan orogens and are now dispersed through Australia, Antarctica and New Zealand. U-Pb detrital zircon age patterns for latest Precambrian, Cambrian and Ordovician metagreywackes show a closely related provenance. The latest Neoproterozoic–early Palaeozoic sedimentary rocks have major components, at c. 525, 550, and 595 Ma, i.e. about 40–80 million years older than deposition. Zircons in these components increase from the Neoproterozoic to Ordovician. Late Mesoproterozoic age components, 1030 and 1070 Ma, probably originate from igneous/metamorphic rocks in the Gondwanaland hinterland whose exact locations are unknown. Although small, the youngest zircon age components are coincident with estimated depositional ages suggesting that they reflect contemporaneous and minor, volcanic sources. Overall, the detrital zircon provenance patterns reflect the development of plutonic/metamorphic complexes of the Ross–Delamerian Orogen in the Transantarctic Mountains and southern Australia that, upon exhumation, supplied sediment to regional scale basin(s) at the Gondwana margin. Tasmanian detrital zircon age patterns differ from those seen in intra-Ross Orogen sandstones of northern Victoria Land and from the oldest metasediments in the Transantarctic Mountains. A comparison with rocks from the latter supports an allochthonous western Tasmania model and amalgamation with Australia in late Cambrian time.

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27

Bierlein, F. P. "POSSIBLE INTRUSION-RELATED GOLD SYSTEMS IN THE WESTERN LACHLAN OROGEN, SOUTHEAST AUSTRALIA." Economic Geology 100, no. 2 (March 1, 2005): 385–98. http://dx.doi.org/10.2113/100.2.385.

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28

Rawlinson, N., and B. L. N. Kennett. "Teleseismic tomography of the upper mantle beneath the southern Lachlan Orogen, Australia." Physics of the Earth and Planetary Interiors 167, no. 1-2 (March 2008): 84–97. http://dx.doi.org/10.1016/j.pepi.2008.02.007.

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29

Foster, David A., and David R. Gray. "Evolution and Structure of the Lachlan Fold Belt (Orogen) of Eastern Australia." Annual Review of Earth and Planetary Sciences 28, no. 1 (May 2000): 47–80. http://dx.doi.org/10.1146/annurev.earth.28.1.47.

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30

Glen, R. A., A. J. Crawford, I. G. Percival, and L. M. Barron. "Early Ordovician development of the Macquarie Arc, Lachlan Orogen, New South Wales." Australian Journal of Earth Sciences 54, no. 2-3 (March 2007): 167–79. http://dx.doi.org/10.1080/08120090601146797.

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31

Glen, R. A., R. D. Dallmeyer, and L. P. Black. "Isotopic dating of basin inversion—The Palaeozoic Cobar Basin, Lachlan Orogen, Australia." Tectonophysics 214, no. 1-4 (November 1992): 249–68. http://dx.doi.org/10.1016/0040-1951(92)90200-p.

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32

Glen, R. A., and D. Wyborn. "Inferred thrust imbrication, deformation gradients and the Lachlan Transverse Zone in the Eastern Belt of the Lachlan Orogen, New South Wales." Australian Journal of Earth Sciences 44, no. 1 (February 1, 1997): 49–68. http://dx.doi.org/10.1080/08120099708728293.

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33

Wilson, Christopher J. L., and Lawrence D. Leader. "Modeling 3D crustal structure in Lachlan Orogen, Victoria, Australia: Implications for gold deposition." Journal of Structural Geology 67 (October 2014): 235–52. http://dx.doi.org/10.1016/j.jsg.2014.01.007.

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34

Poudjom Djomani, Y., and R. A. Glen. "Geophysical evidence for 'blind' magmatism associated with Devonian rifting, Lachlan Orogen, New South Wales." ASEG Extended Abstracts 2009, no. 1 (2009): 1. http://dx.doi.org/10.1071/aseg2009ab094.

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35

Phillips, D., B. Fu, C. J. L. Wilson, M. A. Kendrick, A. M. Fairmaid, and J. MCL Miller. "Timing of gold mineralisation in the western Lachlan Orogen, SE Australia: A critical overview." Australian Journal of Earth Sciences 59, no. 4 (June 2012): 495–525. http://dx.doi.org/10.1080/08120099.2012.682738.

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36

Fergusson, C. L. "Late Ordovician to mid-Silurian Benambran subduction zones in the Lachlan Orogen, southeastern Australia." Australian Journal of Earth Sciences 61, no. 4 (May 6, 2014): 587–606. http://dx.doi.org/10.1080/08120099.2014.903858.

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37

Fergusson, C. L. "Mid to late Paleozoic shortening pulses in the Lachlan Orogen, southeastern Australia: a review." Australian Journal of Earth Sciences 64, no. 1 (January 2, 2017): 1–39. http://dx.doi.org/10.1080/08120099.2017.1273257.

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38

Gray, David R., David A. Foster, Chris Gray, Jim Cull, and Gary Gibson. "Lithospheric Structure of the Southeast Australian Lachlan Orogen along the Victorian Global Geoscience Transect." International Geology Review 40, no. 12 (December 1998): 1088–117. http://dx.doi.org/10.1080/00206819809465256.

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39

Watson, J. M., and D. R. Gray. "Character, extent and significance of broken formation for the Tabberabbera Zone, central Lachlan Orogen." Australian Journal of Earth Sciences 48, no. 6 (December 2001): 943–54. http://dx.doi.org/10.1046/j.1440-0952.2001.00911.x.

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40

Percival, I. G., and R. A. Glen. "Ordovician to earliest Silurian history of the Macquarie Arc, Lachlan Orogen, New South Wales." Australian Journal of Earth Sciences 54, no. 2-3 (March 2007): 143–65. http://dx.doi.org/10.1080/08120090601146789.

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41

Glen, R. A., R. Spencer, A. Willmore, V. David, and R. J. Scott. "Junee – Narromine Volcanic Belt, Macquarie Arc, Lachlan Orogen, New South Wales: components and structure." Australian Journal of Earth Sciences 54, no. 2-3 (March 2007): 215–41. http://dx.doi.org/10.1080/08120090601146805.

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42

Crawford, A. J., R. A. Glen, D. R. Cooke, and I. G. Percival. "Geological evolution and metallogenesis of the Ordovician Macquarie Arc, Lachlan Orogen, New South Wales." Australian Journal of Earth Sciences 54, no. 2-3 (March 2007): 137–41. http://dx.doi.org/10.1080/08120090701221615.

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43

Glen, R. A., I. G. Percival, and C. D. Quinn. "Ordovician continental margin terranes in the Lachlan Orogen, Australia: Implications for tectonics in an accretionary orogen along the east Gondwana margin." Tectonics 28, no. 6 (December 2009): n/a. http://dx.doi.org/10.1029/2009tc002446.

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44

Glen, R. A. "Thrust, extensional and strike-slip tectonics in an evolving Palaeozoic orogen—a structural synthesis of the Lachlan Orogen of southeastern Australia." Tectonophysics 214, no. 1-4 (November 1992): 341–80. http://dx.doi.org/10.1016/0040-1951(92)90205-k.

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45

Glen, R. A., R. J. Korsch, R. Hegarty, A. Saeed, Y. Poudjom Djomani, R. D. Costelloe, and E. Belousova. "Geodynamic significance of the boundary between the Thomson Orogen and the Lachlan Orogen, northwestern New South Wales and implications for Tasmanide tectonics." Australian Journal of Earth Sciences 60, no. 3 (April 2013): 371–412. http://dx.doi.org/10.1080/08120099.2013.782899.

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46

Fergusson, C. L., and G. P. Colquhoun. "Ordovician Macquarie Arc and turbidite fan relationships, Lachlan Orogen, southeastern Australia: stratigraphic and tectonic problems." Australian Journal of Earth Sciences 65, no. 3 (February 11, 2018): 303–33. http://dx.doi.org/10.1080/08120099.2018.1425909.

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47

Spaggiari, C. V., D. R. Gray, D. A. Foster, and S. McKnight. "Evolution of the boundary between the western and central Lachlan Orogen: implications for Tasmanide tectonics." Australian Journal of Earth Sciences 50, no. 5 (October 2003): 725–49. http://dx.doi.org/10.1111/j.1440-0952.2003.01022.x.

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48

Graeber, Frank M., Gregory A. Houseman, and Stewart A. Greenhalgh. "Regional teleseismic tomography of the western Lachlan Orogen and the Newer Volcanic Province, southeast Australia." Geophysical Journal International 149, no. 2 (May 2002): 249–66. http://dx.doi.org/10.1046/j.1365-246x.2002.01598.x.

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49

GLEN, R. A., I. R. STEWART, and I. G. PERCIVAL. "The Narooma Terrane: implications for the construction of the outboard part of the Lachlan Orogen." Australian Journal of Earth Sciences 51, no. 6 (December 2004): 859–84. http://dx.doi.org/10.1111/j.1400-0952.2004.01090.x.

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GRAY, D. R., and D. A. FOSTER. "Tectonic evolution of the Lachlan Orogen, southeast Australia: historical review, data synthesis and modern perspectives." Australian Journal of Earth Sciences 51, no. 6 (December 2004): 773–817. http://dx.doi.org/10.1111/j.1400-0952.2004.01092.x.

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