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  5.     <title>UTas ePrints - Lewis Ponds, a hybrid carbonate and volcanic-hosted polymetallic massive sulphide deposit, New South Wales, Australia</title>
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  13.     <meta content="Agnew, M.W." name="eprints.creators_name" />
  14. <meta content="Large, R.R." name="eprints.creators_name" />
  15. <meta content="Bull, S.W." name="eprints.creators_name" />
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  17. <meta content="Ross.Large@utas.edu.au" name="eprints.creators_id" />
  18. <meta content="S.Bull@utas.edu.au" name="eprints.creators_id" />
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  20. <meta content="2007-09-12" name="eprints.datestamp" />
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  23. <meta content="Lewis Ponds, a hybrid carbonate and volcanic-hosted polymetallic massive sulphide deposit, New South Wales, Australia" name="eprints.title" />
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  25. <meta content="260100" name="eprints.subjects" />
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  27. <meta content="Volcanic-hosted massive sulphide, Carbonate-hosted replacement, Sulphide textures, Limestone, Lachlan Fold Belt, Hill End Trough, Australia" name="eprints.keywords" />
  28. <meta content="Abstract The Lewis Ponds Zn-Pb-Cu-Ag-Au deposit,
  29. located in the eastern Lachlan Fold Belt, central
  30. western New South Wales, exhibits the characteristics
  31. of both volcanic-hosted massive sulphide and carbonate-
  32. hosted replacement deposits. Two stratabound
  33. massive to disseminated sulphide zones, Main and
  34. Toms, occur in a tightly folded Upper Silurian
  35. sequence of marine felsic volcanic and sedimentary
  36. rocks. They have a combined indicated resource of
  37. 5.7 Mt grading 3.5% Zn, 2.0% Pb, 0.19% Cu, 97 g/t
  38. Ag and 1.9 g/t Au. Main Zone is hosted by a thick
  39. unit of poorly sorted mixed provenance breccia,
  40. limestone-clast breccia and quartz crystal-rich sandstone,
  41. whereas Toms Zone occurs in the overlying
  42. siltstone. Pretectonic carbonate-chalcopyrite-pyrite
  43. and quartz-pyrite stringer veins occur in the footwall
  44. porphyritic dacite, south of Toms Zone. Strongly
  45. sheared dolomite-chalcopyrite-pyrrhotite veins directly
  46. underlie the Toms massive sulphide lens. The mineralized
  47. zones consist predominantly of pyrite, sphalerite
  48. and galena. Paragenetically early framboidal, dendritic
  49. and botryoidal pyrite aggregates and tabular pyrrhotite
  50. pseudomorphs of sulphate occur throughout the
  51. breccia and sandstone beds that host Main Zone, but
  52. are rarely preserved in the annealed massive sulphide
  53. in Toms Zone. Main and Toms zones are associated
  54. with a semi-conformable hydrothermal alteration
  55. envelope, characterized by texturally destructive chlorite-,
  56. dolomite- and quartz-rich assemblages. Dolomite,
  57. chlorite, quartz, calcite and sulphides have
  58. selectively replaced breccia and sandstone beds in the
  59. Main Zone host sequence, whereas the underlying
  60. porphyritic dacite is weakly sericite altered. Vuggy and
  61. botryoidal textures resulted from partial dissolution of
  62. the dolomite-altered sedimentary rocks and unimpeded
  63. growth of base metal sulphides, carbonate and quartz
  64. into open cavities. The intense chlorite-rich alteration
  65. assemblage, underlying Toms Zone, grades outward
  66. into a weak pervasive sericite-quartz assemblage with
  67. distance from the massive sulphide lens. Limestone
  68. clasts and hydrothermal dolomite at Lewis Ponds are
  69. enriched in light carbon and oxygen isotopes. The
  70. dolomite yielded delta 13 CVPDB values of -11 to +1 per mil and delta 18O VSMOW values of 6 to 16per mil. Liquid-vapour fluid inclusions in the dolomite have low salinities (1.4-7.7 equiv. wt% NaCl) and homogenization temperatures
  71. (166-232 degrees C for 1,000 m water depth). Dolomitization
  72. probably involved fluid mixing or fluid-rock interactions
  73. between evolved heated seawater and the limestone-bearing facies, prior to and during mineralization.
  74. delta 34 SVCDT values range from 2.0 per mil to 5.0 per mil in the massive sulphide and 3.9 per mil to 7.4 per mil in the footwall carbonate-chalcopyrite-pyrite stringer veins, indicating that the hydrothermal fluid may have contained mamgatic sulphur and a component of partially reduced seawater. The sulphide mineral assemblages at
  75. Lewis Ponds are consistent with moderate to strongly
  76. reduced conditions during diagenesis and mineralization.
  77. Low temperature dolomitization of limestonebearing
  78. facies in the Main Zone host sequence created
  79. secondary porosity and provided a reactive host for
  80. fluid-rock interactions. Main Zone formed by lateral
  81. fluid flow and sub-seafloor replacement of the poorly
  82. sorted breccia and sandstone beds. Base metal
  83. sulphide deposition probably resulted from dissolution
  84. of dolomite, fluid mixing and increased fluid pH.
  85. Pyrite, sphalerite and galena precipitated from a relatively
  86. low temperature, 150-250C hydrothermal fluid.
  87. In contrast, Toms Zone was emplaced into finegrained
  88. sediment at or near the seafloor, above a zone
  89. of focused up-flowing hydrothermal fluids. Copperrich
  90. assemblages were deposited in the Toms Zone
  91. footwall and massive sulphide lenses in Main and
  92. Toms zones as the hydrothermal system intensified.During the D1 deformation, fracture-controlled fluids
  93. within the Lewis Ponds fault zone and adjacent
  94. footwall volcanic succession remobilized sulphides
  95. into syntectonic quartz veins. Lewis Ponds is a rare
  96. example of a synvolcanic sub-seafloor hydrothermal
  97. system developed within fossiliferous limestone-bearing
  98. facies. The close spatial association between limestone,
  99. hydrothermal dolomite, massive sulphide and dacite
  100. provides a basis for new exploration targets elsewhere
  101. in New South Wales." name="eprints.abstract" />
  102. <meta content="2005-03" name="eprints.date" />
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  112. <meta content="http://dx.doi.org/10.1007/s00126-004-0456-6" name="eprints.official_url" />
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  278. 88:2065-2094" name="eprints.referencetext" />
  279. <meta content="Agnew, M.W. and Large, R.R. and Bull, S.W. (2005) Lewis Ponds, a hybrid carbonate and volcanic-hosted polymetallic massive sulphide deposit, New South Wales, Australia. Mineralium Deposita, 39 (8). pp. 822-844. ISSN 0026-4598" name="eprints.citation" />
  280. <meta content="http://eprints.utas.edu.au/1899/1/Agnew%2C_Large%2C_Bull_2005_MINERAL_DEPOS.pdf" name="eprints.document_url" />
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  282. <meta content="Lewis Ponds, a hybrid carbonate and volcanic-hosted polymetallic massive sulphide deposit, New South Wales, Australia" name="DC.title" />
  283. <meta content="Agnew, M.W." name="DC.creator" />
  284. <meta content="Large, R.R." name="DC.creator" />
  285. <meta content="Bull, S.W." name="DC.creator" />
  286. <meta content="260100 Geology" name="DC.subject" />
  287. <meta content="Abstract The Lewis Ponds Zn-Pb-Cu-Ag-Au deposit,
  288. located in the eastern Lachlan Fold Belt, central
  289. western New South Wales, exhibits the characteristics
  290. of both volcanic-hosted massive sulphide and carbonate-
  291. hosted replacement deposits. Two stratabound
  292. massive to disseminated sulphide zones, Main and
  293. Toms, occur in a tightly folded Upper Silurian
  294. sequence of marine felsic volcanic and sedimentary
  295. rocks. They have a combined indicated resource of
  296. 5.7 Mt grading 3.5% Zn, 2.0% Pb, 0.19% Cu, 97 g/t
  297. Ag and 1.9 g/t Au. Main Zone is hosted by a thick
  298. unit of poorly sorted mixed provenance breccia,
  299. limestone-clast breccia and quartz crystal-rich sandstone,
  300. whereas Toms Zone occurs in the overlying
  301. siltstone. Pretectonic carbonate-chalcopyrite-pyrite
  302. and quartz-pyrite stringer veins occur in the footwall
  303. porphyritic dacite, south of Toms Zone. Strongly
  304. sheared dolomite-chalcopyrite-pyrrhotite veins directly
  305. underlie the Toms massive sulphide lens. The mineralized
  306. zones consist predominantly of pyrite, sphalerite
  307. and galena. Paragenetically early framboidal, dendritic
  308. and botryoidal pyrite aggregates and tabular pyrrhotite
  309. pseudomorphs of sulphate occur throughout the
  310. breccia and sandstone beds that host Main Zone, but
  311. are rarely preserved in the annealed massive sulphide
  312. in Toms Zone. Main and Toms zones are associated
  313. with a semi-conformable hydrothermal alteration
  314. envelope, characterized by texturally destructive chlorite-,
  315. dolomite- and quartz-rich assemblages. Dolomite,
  316. chlorite, quartz, calcite and sulphides have
  317. selectively replaced breccia and sandstone beds in the
  318. Main Zone host sequence, whereas the underlying
  319. porphyritic dacite is weakly sericite altered. Vuggy and
  320. botryoidal textures resulted from partial dissolution of
  321. the dolomite-altered sedimentary rocks and unimpeded
  322. growth of base metal sulphides, carbonate and quartz
  323. into open cavities. The intense chlorite-rich alteration
  324. assemblage, underlying Toms Zone, grades outward
  325. into a weak pervasive sericite-quartz assemblage with
  326. distance from the massive sulphide lens. Limestone
  327. clasts and hydrothermal dolomite at Lewis Ponds are
  328. enriched in light carbon and oxygen isotopes. The
  329. dolomite yielded delta 13 CVPDB values of -11 to +1 per mil and delta 18O VSMOW values of 6 to 16per mil. Liquid-vapour fluid inclusions in the dolomite have low salinities (1.4-7.7 equiv. wt% NaCl) and homogenization temperatures
  330. (166-232 degrees C for 1,000 m water depth). Dolomitization
  331. probably involved fluid mixing or fluid-rock interactions
  332. between evolved heated seawater and the limestone-bearing facies, prior to and during mineralization.
  333. delta 34 SVCDT values range from 2.0 per mil to 5.0 per mil in the massive sulphide and 3.9 per mil to 7.4 per mil in the footwall carbonate-chalcopyrite-pyrite stringer veins, indicating that the hydrothermal fluid may have contained mamgatic sulphur and a component of partially reduced seawater. The sulphide mineral assemblages at
  334. Lewis Ponds are consistent with moderate to strongly
  335. reduced conditions during diagenesis and mineralization.
  336. Low temperature dolomitization of limestonebearing
  337. facies in the Main Zone host sequence created
  338. secondary porosity and provided a reactive host for
  339. fluid-rock interactions. Main Zone formed by lateral
  340. fluid flow and sub-seafloor replacement of the poorly
  341. sorted breccia and sandstone beds. Base metal
  342. sulphide deposition probably resulted from dissolution
  343. of dolomite, fluid mixing and increased fluid pH.
  344. Pyrite, sphalerite and galena precipitated from a relatively
  345. low temperature, 150-250C hydrothermal fluid.
  346. In contrast, Toms Zone was emplaced into finegrained
  347. sediment at or near the seafloor, above a zone
  348. of focused up-flowing hydrothermal fluids. Copperrich
  349. assemblages were deposited in the Toms Zone
  350. footwall and massive sulphide lenses in Main and
  351. Toms zones as the hydrothermal system intensified.During the D1 deformation, fracture-controlled fluids
  352. within the Lewis Ponds fault zone and adjacent
  353. footwall volcanic succession remobilized sulphides
  354. into syntectonic quartz veins. Lewis Ponds is a rare
  355. example of a synvolcanic sub-seafloor hydrothermal
  356. system developed within fossiliferous limestone-bearing
  357. facies. The close spatial association between limestone,
  358. hydrothermal dolomite, massive sulphide and dacite
  359. provides a basis for new exploration targets elsewhere
  360. in New South Wales." name="DC.description" />
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  474.     <h1 class="ep_tm_pagetitle">Lewis Ponds, a hybrid carbonate and volcanic-hosted polymetallic massive sulphide deposit, New South Wales, Australia</h1>
  475.     <p style="margin-bottom: 1em" class="not_ep_block"><span class="person_name">Agnew, M.W.</span> and <span class="person_name">Large, R.R.</span> and <span class="person_name">Bull, S.W.</span> (2005) <xhtml:em>Lewis Ponds, a hybrid carbonate and volcanic-hosted polymetallic massive sulphide deposit, New South Wales, Australia.</xhtml:em> Mineralium Deposita, 39 (8). pp. 822-844. ISSN 0026-4598</p><p style="margin-bottom: 1em" class="not_ep_block"></p><table style="margin-bottom: 1em" class="not_ep_block"><tr><td valign="top" style="text-align:center"><a href="http://eprints.utas.edu.au/1899/1/Agnew%2C_Large%2C_Bull_2005_MINERAL_DEPOS.pdf"><img alt="[img]" src="http://eprints.utas.edu.au/style/images/fileicons/application_pdf.png" border="0" class="ep_doc_icon" /></a></td><td valign="top"><a href="http://eprints.utas.edu.au/1899/1/Agnew%2C_Large%2C_Bull_2005_MINERAL_DEPOS.pdf"><span class="ep_document_citation">PDF</span></a> - Full text restricted - Requires a PDF viewer<br />2061Kb</td><td><form method="get" accept-charset="utf-8" action="http://eprints.utas.edu.au/cgi/request_doc"><input value="2394" name="docid" accept-charset="utf-8" type="hidden" /><div class=""><input value="Request a copy" name="_action_null" class="ep_form_action_button" onclick="return EPJS_button_pushed( '_action_null' )" type="submit" /> </div></form></td></tr></table><p style="margin-bottom: 1em" class="not_ep_block">Official URL: <a href="http://dx.doi.org/10.1007/s00126-004-0456-6">http://dx.doi.org/10.1007/s00126-004-0456-6</a></p><div class="not_ep_block"><h2>Abstract</h2><p style="padding-bottom: 16px; text-align: left; margin: 1em auto 0em auto">Abstract The Lewis Ponds Zn-Pb-Cu-Ag-Au deposit,&#13;
  476. located in the eastern Lachlan Fold Belt, central&#13;
  477. western New South Wales, exhibits the characteristics&#13;
  478. of both volcanic-hosted massive sulphide and carbonate-&#13;
  479. hosted replacement deposits. Two stratabound&#13;
  480. massive to disseminated sulphide zones, Main and&#13;
  481. Toms, occur in a tightly folded Upper Silurian&#13;
  482. sequence of marine felsic volcanic and sedimentary&#13;
  483. rocks. They have a combined indicated resource of&#13;
  484. 5.7 Mt grading 3.5% Zn, 2.0% Pb, 0.19% Cu, 97 g/t&#13;
  485. Ag and 1.9 g/t Au. Main Zone is hosted by a thick&#13;
  486. unit of poorly sorted mixed provenance breccia,&#13;
  487. limestone-clast breccia and quartz crystal-rich sandstone,&#13;
  488. whereas Toms Zone occurs in the overlying&#13;
  489. siltstone. Pretectonic carbonate-chalcopyrite-pyrite&#13;
  490. and quartz-pyrite stringer veins occur in the footwall&#13;
  491. porphyritic dacite, south of Toms Zone. Strongly&#13;
  492. sheared dolomite-chalcopyrite-pyrrhotite veins directly&#13;
  493. underlie the Toms massive sulphide lens. The mineralized&#13;
  494. zones consist predominantly of pyrite, sphalerite&#13;
  495. and galena. Paragenetically early framboidal, dendritic&#13;
  496. and botryoidal pyrite aggregates and tabular pyrrhotite&#13;
  497. pseudomorphs of sulphate occur throughout the&#13;
  498. breccia and sandstone beds that host Main Zone, but&#13;
  499. are rarely preserved in the annealed massive sulphide&#13;
  500. in Toms Zone. Main and Toms zones are associated&#13;
  501. with a semi-conformable hydrothermal alteration&#13;
  502. envelope, characterized by texturally destructive chlorite-,&#13;
  503. dolomite- and quartz-rich assemblages. Dolomite,&#13;
  504. chlorite, quartz, calcite and sulphides have&#13;
  505. selectively replaced breccia and sandstone beds in the&#13;
  506. Main Zone host sequence, whereas the underlying&#13;
  507. porphyritic dacite is weakly sericite altered. Vuggy and&#13;
  508. botryoidal textures resulted from partial dissolution of&#13;
  509. the dolomite-altered sedimentary rocks and unimpeded&#13;
  510. growth of base metal sulphides, carbonate and quartz&#13;
  511. into open cavities. The intense chlorite-rich alteration&#13;
  512. assemblage, underlying Toms Zone, grades outward&#13;
  513. into a weak pervasive sericite-quartz assemblage with&#13;
  514. distance from the massive sulphide lens. Limestone&#13;
  515. clasts and hydrothermal dolomite at Lewis Ponds are&#13;
  516. enriched in light carbon and oxygen isotopes. The&#13;
  517. dolomite yielded delta 13 CVPDB values of -11 to +1 per mil and delta 18O VSMOW values of 6 to 16per mil. Liquid-vapour fluid inclusions in the dolomite have low salinities (1.4-7.7 equiv. wt% NaCl) and homogenization temperatures&#13;
  518. (166-232 degrees C for 1,000 m water depth). Dolomitization&#13;
  519. probably involved fluid mixing or fluid-rock interactions&#13;
  520. between evolved heated seawater and the limestone-bearing facies, prior to and during mineralization.&#13;
  521. delta 34 SVCDT values range from 2.0 per mil to 5.0 per mil in the massive sulphide and 3.9 per mil to 7.4 per mil in the footwall carbonate-chalcopyrite-pyrite stringer veins, indicating that the hydrothermal fluid may have contained mamgatic sulphur and a component of partially reduced seawater. The sulphide mineral assemblages at&#13;
  522. Lewis Ponds are consistent with moderate to strongly&#13;
  523. reduced conditions during diagenesis and mineralization.&#13;
  524. Low temperature dolomitization of limestonebearing&#13;
  525. facies in the Main Zone host sequence created&#13;
  526. secondary porosity and provided a reactive host for&#13;
  527. fluid-rock interactions. Main Zone formed by lateral&#13;
  528. fluid flow and sub-seafloor replacement of the poorly&#13;
  529. sorted breccia and sandstone beds. Base metal&#13;
  530. sulphide deposition probably resulted from dissolution&#13;
  531. of dolomite, fluid mixing and increased fluid pH.&#13;
  532. Pyrite, sphalerite and galena precipitated from a relatively&#13;
  533. low temperature, 150-250C hydrothermal fluid.&#13;
  534. In contrast, Toms Zone was emplaced into finegrained&#13;
  535. sediment at or near the seafloor, above a zone&#13;
  536. of focused up-flowing hydrothermal fluids. Copperrich&#13;
  537. assemblages were deposited in the Toms Zone&#13;
  538. footwall and massive sulphide lenses in Main and&#13;
  539. Toms zones as the hydrothermal system intensified.During the D1 deformation, fracture-controlled fluids&#13;
  540. within the Lewis Ponds fault zone and adjacent&#13;
  541. footwall volcanic succession remobilized sulphides&#13;
  542. into syntectonic quartz veins. Lewis Ponds is a rare&#13;
  543. example of a synvolcanic sub-seafloor hydrothermal&#13;
  544. system developed within fossiliferous limestone-bearing&#13;
  545. facies. The close spatial association between limestone,&#13;
  546. hydrothermal dolomite, massive sulphide and dacite&#13;
  547. provides a basis for new exploration targets elsewhere&#13;
  548. in New South Wales.</p></div><table style="margin-bottom: 1em" border="0" cellpadding="3" class="not_ep_block"><tr><th valign="top" class="ep_row">Item Type:</th><td valign="top" class="ep_row">Article</td></tr><tr><th valign="top" class="ep_row">Keywords:</th><td valign="top" class="ep_row">Volcanic-hosted massive sulphide, Carbonate-hosted replacement, Sulphide textures, Limestone, Lachlan Fold Belt, Hill End Trough, Australia</td></tr><tr><th valign="top" class="ep_row">Subjects:</th><td valign="top" class="ep_row"><a href="http://eprints.utas.edu.au/view/subjects/260100.html">260000 Earth Sciences &gt; 260100 Geology</a></td></tr><tr><th valign="top" class="ep_row">Collections:</th><td valign="top" class="ep_row">UNSPECIFIED</td></tr><tr><th valign="top" class="ep_row">ID Code:</th><td valign="top" class="ep_row">1899</td></tr><tr><th valign="top" class="ep_row">Deposited By:</th><td valign="top" class="ep_row"><span class="ep_name_citation"><span class="person_name">Mrs Katrina Keep</span></span></td></tr><tr><th valign="top" class="ep_row">Deposited On:</th><td valign="top" class="ep_row">12 Sep 2007</td></tr><tr><th valign="top" class="ep_row">Last Modified:</th><td valign="top" class="ep_row">23 Jan 2008 15:58</td></tr><tr><th valign="top" class="ep_row">ePrint Statistics:</th><td valign="top" class="ep_row"><a target="ePrintStats" href="/es/index.php?action=show_detail_eprint;id=1899;">View statistics for this ePrint</a></td></tr></table><p align="right">Repository Staff Only: <a href="http://eprints.utas.edu.au/cgi/users/home?screen=EPrint::View&amp;eprintid=1899">item control page</a></p>
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