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  5.     <title>UTas ePrints - Spatial distribution patterns of sulfur isotopes, nodular carbonate, and ore textures in the McArthur River (HYC) Zn-Pb-Ag deposit, Northern Territory, Australia</title>
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  13.     <meta content="Ireland, T." name="eprints.creators_name" />
  14. <meta content="Large, R.R." name="eprints.creators_name" />
  15. <meta content="McGoldrick, P.J." name="eprints.creators_name" />
  16. <meta content="Blake, M.D." name="eprints.creators_name" />
  17. <meta content="tireland@postoffice.utas.edu.au" name="eprints.creators_id" />
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  25. <meta content="Spatial distribution patterns of sulfur isotopes, nodular carbonate, and ore textures
  26. in the McArthur River (HYC) Zn-Pb-Ag deposit, Northern Territory, Australia" name="eprints.title" />
  27. <meta content="pub" name="eprints.ispublished" />
  28. <meta content="260100" name="eprints.subjects" />
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  30. <meta content="SEDEX, Seafloor massive sulfide, sediment-hosted,zinc, lead, Mt Isa, McArthur Basin" name="eprints.keywords" />
  31. <meta content="The HYC Zn-Pb-Ag deposit at McArthur River is the largest known and least deformed Australian sedimenthosted
  32. stratiform base metal deposit. A study of mineralogical, geochemical, and isotopic zonation through the
  33. deposit reveals concentric distribution patterns in (1) the occurrence of nodular carbonate, (2) the δ34S composition
  34. of sphalerite, and (3) microscopic ore textures. The correlation of previously documented lateral metal
  35. zonation with these other zonation patterns precludes exclusive postsedimentation mineralization and provides
  36. some insight into the mechanisms and controls on synsedimentary to early diagenetic mineralization. This mineralization
  37. timing is also supported by new carbon and oxygen isotope analyses, recognition of two stages of texturally
  38. and isotopically distinct sphalerite, and reinterpretation of complex sulfide textures.
  39. Dolomitic carbonate nodules occur in the south, southwest, northwest, and northern fringes of the deposit
  40. and are interpreted to have surrounded the high-grade ore lenses prior to structural and erosive truncation.
  41. The carbon and oxygen isotope composition of these carbonate nodules is similar to the sedimentary dolomite
  42. within the ore lenses. There is no evidence for incorporation of light carbon derived from oxidation of organic
  43. material under closed-system conditions and the nodular carbonate probably formed under open-system conditions
  44. in communication with seawater. These nodules displace siltstone laminae and, therefore, likely formed
  45. in the very shallow subsea-floor environment.
  46. In ore lens 3, the δ34S of laminated early sphalerite (sp1) changes from a mean value of 5 per mil in the deposit
  47. center to a mean of 1.7 per mil in the extreme fringes. We interpret this to be the result of sulfide precipitation
  48. in a restricted marine basin. Later sphalerite (sp2) associated with nodular carbonate has a mean δ34S
  49. value of 9.8 per mil, whereas laminated early sphalerite (sp1) has a mean δ34S value of 3.8 per mil. This isotopic
  50. separation of the two paragenetic stages of sphalerite is found in immediately adjacent aggregates. Concentration
  51. of 34S in late sphalerite (sp2) is likely the result of closed-system conditions in the sediment pore fluid.
  52. Textures of laminated sphalerite change from strongly anastomosing in the central part of the deposit to
  53. plane laminar and patchy in the deposit fringes. Mass-balance calculations preclude substantial carbonate dissolution
  54. and a stylolitic origin for these textures. Instead we propose that rapidly precipitated sphalerite coagulated
  55. and trapped pelagic silt and early pyrite (py1) as it was deposited on the sea floor. In contrast, paragenetically
  56. late sphalerite (sp2) and pyrite (py2) must be diagenetic as they overprint and are pseudomorphous
  57. after the carbonate nodules. We propose a repeating paragenetic sequence of galena/sphalerite (sp1) → pyrite
  58. (py1) → nodular carbonate → sphalerite (sp2) → pyrite (py2), which accounts for all the textural complexity and
  59. isotopic disequilibrium between sulfide phases.
  60. The data presented in this paper suggest that base metal sulfides formed both in the water column and in
  61. the uppermost sediment pile. Biological and thermochemical sulfate reduction probably occurred simultaneously
  62. in different parts of a complex physicochemical system in which stratification of the marine environment
  63. is seen as the primary control on the lateral distribution of the mineralized facies. We propose a stratified water
  64. body in which sharp internal chemical gradients separate a surficial oxic layer, an anoxic layer, and a basal hypersaline
  65. brine pool. Asymmetric metal zonation across the deposit reflects individual pulses of metalliferous
  66. fluid that were introduced into the basin as a bottom-hugging dense current." name="eprints.abstract" />
  67. <meta content="2004-12" name="eprints.date" />
  68. <meta content="published" name="eprints.date_type" />
  69. <meta content="Economic Geology" name="eprints.publication" />
  70. <meta content="99" name="eprints.volume" />
  71. <meta content="8" name="eprints.number" />
  72. <meta content="1687-1709" name="eprints.pagerange" />
  73. <meta content="10.2113/99.8.1687" name="eprints.id_number" />
  74. <meta content="TRUE" name="eprints.refereed" />
  75. <meta content="0361-0128" name="eprints.issn" />
  76. <meta content="http://dx.doi.org/10.2113/99.8.1687" name="eprints.official_url" />
  77. <meta content="Arp, G., Reimer, A., and Reitner, J., 2003, Microbialite formation in seawater
  78. of increased alkalinity, Satonda Crater Lake, Indonesia: Journal of Sedimentary
  79. Research, v. 73, p. 105–127.
  80. Atkins, P.W., 1999, Physical chemistry, 6th ed.: New York, Oxford University
  81. Press, 874 p.
  82. Badham, J.P.N., 1981, Shale hosted Pb-Zn deposits: Products of exhalation of
  83. formation waters?: Institution of Mining and Metallurgy Transactions, v.
  84. 90, p. 370–376.
  85. Barrett, T., and MacLean, W.H., 1994, Chemostratigraphy and hydrothermal
  86. alteration in exploration for VHMS deposits in greenstones and younger
  87. volcanic rocks, in Lentz, D.R., ed., Alteration and alteration processes associated
  88. with ore forming systems: Geological Society of Canada Short
  89. Course Notes, v. 11, p. 433–467.
  90. Benning, L.G., Wilkin, R.T., and Barnes, H.L., 2000, Reaction pathways in
  91. the Fe-S system below 100 degrees: Chemical Geology, v. 167, p. 25–51.
  92. Bosbach, D., Hall, C., and Putnis, A., 1998, Mineral precipitation and dissolution
  93. in aqueous solution: In situ microscopic observations on barite (001)
  94. with atomic force microscopy: Chemical Geology, v. 151, p. 143–160.
  95. Broadbent, G.C., Myers, R.E., and Wright, J.V., 1998, Geology and origin of
  96. shale-hosted Zn-Pb-Ag mineralization at the Century deposit, Northwest
  97. Queensland, Australia: ECONOMIC GEOLOGY, v. 93, p. 1264–1294.
  98. Bull, S.W., 1998. Sedimentology of the Palaeoproterozoic Barney Creek Formation
  99. in DDH BMR McArthur 2, southern McArthur basin, Northern
  100. Territory: Australian Journal of Earth Sciences, v. 45, p. 21–31.
  101. Canfield, D.E., and Thamdrup, B., 1994, The production of 34S-depleted sulphide
  102. during bacterial disproprtionation of elemental sulphur: Science, v.
  103. 266, p. 1973–1975.
  104. Chafetz, H.S., and Buczynski, C., 1992, Bacterially induced lithification of
  105. microbial mats: Palaios, v. 7, no. 3, p. 277–293.
  106. Chen, J., Walter, M.R., Logan, G.A., Hinman, M.C., and Summons, R.E.,
  107. 2003, The Paleoproterozoic McArthur River (HYC) Pb/Zn/Ag deposit of
  108. northern Australia: Organic geochemistry and ore genesis: Earth and Planetary
  109. Science Letters, v. 210, p. 467–479.
  110. Cooke, D.R., Bodon, S.B., and Bull, S.W., 1998, Element associations and
  111. depositional processes for McArthur-type and Selwyn-type sediment
  112. hosted Pb-Zn deposits: Australian Mineral Industry Research Association
  113. International Ltd. Unpublished Report P384A, v. 2, p. 145–182.
  114. Cooke, D.R., Bull, S.W., Large, R.R., and McGoldrick, P.J., 2000, The importance
  115. of oxidized brines for the formation of Australian Proterozoic
  116. stratiform sediment-hosted Pb-Zn (SEDEX) deposits: ECONOMIC GEOLOGY,
  117. v. 95, p. 1–17.
  118. Cotton, R.E., 1965, HYC lead-zinc-silver deposit, McArthur River: Geology
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  125. from the Middle Proterozoic McArthur basin, Australia: Australian
  126. Journal of Earth Sciences, v. 39, p. 501–519.
  127. Croxford, N.J.W., 1968, A mineralogical examination of the McArthur leadzinc-
  128. silver deposit: Australasian Institute of Mining and Metallurgy Proceedings,
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  131. Northern Territory, Australia: Australasian Institute of Mining and
  132. Metallurgy Proceedings, v. 243, p. 1–26.
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  137. J.F., 2002, Biogenic precipitation of monomineralic nanocrystalline
  138. sulfides: Implications of observed and modeled processes to ore deposition:
  139. ECONOMIC GEOLOGY, v. 97, p. 1319–1329.
  140. Eldridge, C.S., Williams, N., and Walshe, J.L., 1993, Sulfur isotope variability
  141. in sediment-hosted massive sulfide deposits as determined using the ion
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  152. ore formation at McArthur River, Northern Territory: “A Hydrothermal
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  160. ablation sulphur isotope microprobe: Australian Journal of Earth Sciences,
  161. v. 42, p. 549–555.
  162. Ireland, T., 2001, Lateral variability of sedimentology, mineralogy and geochemistry
  163. in the HYC Zn-Pb-Ag deposit, Northern Territory, Australia: Implications
  164. for deposit genesis: Unpublished honours thesis, Hobart, University
  165. of Tasmania, 138 p.
  166. Ireland, T., Bull, S.R., and Large, R.R., 2004, Mass flow sedimentology
  167. within the HYC Zn-Pb-Ag deposit, Northern Territory, Australia: Evidence
  168. for syn-sedimentary ore genesis: Mineralium Deposita, v. 39, p. 143–158.
  169. Jorgensen, B.B., 1990, A thiosulphate shunt in the sulphur cycle of marine
  170. sediments: Science, v. 249, p. 152–154.
  171. Kribek, B., 1975, The origin of framboidal pyrite as a surface effect of sulphur
  172. grains: Mineralium Deposita, v. 10, p. 389–396.
  173. Lambert, I.B., 1976, The McArthur lead-zinc-silver deposit: Features in metallogenesis
  174. and comparisons with some other stratiform ores, in Wolfe,
  175. K.H., ed., Handbook of stratabound and stratiform ore deposits: Amsterdam,
  176. Elsevier, v. 6, p. 535–585.
  177. Lambert, I.B., and Scott, K.M., 1973, Implications of geochemical investigations
  178. of sedimentary rocks within and around the zinc-lead-silver deposit,
  179. Northern Territory, Australia: Journal of Geochemical Exploration, v. 2, p.
  180. 307–330.
  181. Large, D.E., 1983, Sediment-hosted massive sulphide lead-zinc deposits:
  182. Mineralogical Association of Canada Short Course Handbook, v. 9, p. 1–29.
  183. Large, R.R., Bull, S.W., Cooke, D.R., and McGoldrick, P.J, 1998, A genetic
  184. model for the HYC deposit, Australia, based on regional sedimentology,
  185. geochemistry, and sulfide-sediment relationships: ECONOMIC GEOLOGY, v.
  186. 93, p. 1345–1368.
  187. Large, R.R., Bull, S.W., and McGoldrick, P.J., 2000, Lithogeochemical halos
  188. and geochemical vectors to stratiform sediment hosted Zn-Pb-Ag deposits.
  189. Part 2: HYC deposit, McArthur River, Northern Territory: Journal of Geochemical
  190. Exploration, v. 68, p. 105–126.
  191. Large, R.R., Bull, S.W., and Winefield, P.R., 2001, Carbon and oxygen isotope
  192. halo in carbonate related to the McArthur River (HYC) Zn-Pb-Ag deposit:
  193. Implications for sedimentation, ore genesis, and mineral exploration:
  194. ECONOMIC GEOLOGY, v. 96, p. 1567–1593.
  195. Logan, G.A., Hinman, M., Walter, M.R., and Summons, R.E., 2001, Biogeochemistry
  196. of the 1640 Ma McArthur River (HYC) lead-zinc ore and host
  197. sediments, Northern Territory, Australia: Geochimica et Cosmochimica
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  199. Logan, R.G., 1979, The geology and mineralogical zoning of the HYC Ag-Pb-
  200. Zn deposit, McArthur River, Northern Territory, Australia: Unpublished
  201. M.Sc. thesis, Canberra, Australian National University, 277 p.
  202. Longstaffe, F.J., 1989, Stable isotopes as tracers in clastic diagenesis: Mineralogical
  203. Asociation of Canada Short Course Handbook, v. 15, p. 201–277.
  204. Lydon, J.W., 1983, Chemical parameters controlling the origin and deposition
  205. of sediment-hosted stratiform lead-zinc deposits: Mineralogical Association
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  207. Machel, H.G., Krouse, H.R., and Sassen, R., 1995, Products and distinguishing
  208. criteria of bacterial and thermochemical sulphate reduction: Applied
  209. Geochemistry, v. 10, p. 373–389.
  210. McDougall, T.J., 1984, Convection processes caused by a dense hot saline
  211. source flowing into a submarine depression from above: Deep Sea Research,
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  213. Muir, M.D., Donnelly, T.H., Wilkins, R.W.T., and Armstrong, K.J., 1985, Stable
  214. isotope, petrological and fluid inclusion studies of minor mineral deposits
  215. from the McArthur basin: Implications for the genesis of some sediment-
  216. hosted base metal mineralization from the Northern Territory:
  217. Australian Journal of Earth Sciences, v. 32, p. 239–260.
  218. Murray, W.J., 1975, McArthur River HYC lead-zinc-silver and related deposits,
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  222. Oehler, J.H., and Logan, R.G, 1977, Microfossils, cherts and associated mineralization
  223. in the Proterozoic McArthur (HYC) lead-zinc-silver deposit:
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  225. Ohmoto, H., and Goldhaber, M.B., 1997, Sulfur and carbon isotopes, in
  226. Barnes, H.L., ed., Geochemistry of the hydrothermal ore deposits, 3rd ed.:
  227. New York, Wiley and Sons, p. 517–612.
  228. Page, R.W., and Sweet, I.P., 1998, Geochronology of basin phases in the
  229. western Mt. Isa inlier, and correlation with the McArthur basin: Australian
  230. Journal of Earth Sciences, v. 45, p. 219–232.
  231. Peck, H.D.J., 1982, Physiological diversity of the sulfate-reducing bacteria, in
  232. Strohl, W.R., and Tuovinen, O.H., eds., Microbial chemautotrophy: Columbus,
  233. OH, Ohio State University Press, 351 p.
  234. Perkins, W.G., and Bell, T.H., 1998, Stratiform replacement lead-zinc deposits:
  235. A comparison between Mount Isa, Hilton, and McArthur River:
  236. ECONOMIC GEOLOGY, v. 93, p. 1190–1212.
  237. Plumb, K.A., and Brown, M.C., 1973, Revised correlations and stratigraphic
  238. nomenclature in the Proterozoic carbonate complex of the McArthur
  239. Group, Northern Territory: Australian Bureau of Mineral Resources, Geology
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  241. Plumb, K.A., and Wellman, P., 1987, McArthur basin, Northern Territory:
  242. Mapping of deep troughs using gravity and magnetic anomalies: Bureau of
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  245. Plumb, K.A., Ahmad, M., and Wygralak, A.S., 1990, Mid-Proterozoic basins
  246. of the North Australian craton—regional geology and mineralization, in
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  253. B., 1996, Distribution of bacterial populations in a stratified fjord
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  261. at McArthur River, Northern Territory, Australia: III. The stable isotope
  262. geochemistry of the HYC, Ridge and Cooley deposits: ECONOMIC GEOLOGY,
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  264. Sangster, D.F., 2001, The role of dense brines in the formation of vent-distal
  265. sedimentary-exhalative (sedex) lead-zinc deposits: Field and laboratory evidence:
  266. Mineralium Deposita, v. 37, p. 149–157.
  267. Schidlowski, M., 2000, Carbon isotopes and microbial sediments, in Riding,
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  282. advances concerning the HYC and associated deposits, McArthur River,
  283. Northern Territory: Journal of the Geological Society of Australia, v. 24, p.
  284. 365–380.
  285. Williams, N., 1978, Studies of the base metal sulfide deposits at McArthur
  286. River, Northern Territory, Australia: I. The Cooley and Ridge deposits:
  287. ECONOMIC GEOLOGY, v. 73, p. 1005–1035.
  288. Winefield, P., 1999. Late Palaeoproterozoic carbonates, southern McArthur
  289. Basin, Northern Territory. Unpublished Ph.D. thesis, Hobart, University of
  290. Tasmania, 252 p." name="eprints.referencetext" />
  291. <meta content="Ireland, T. and Large, R.R. and McGoldrick, P.J. and Blake, M.D. (2004) Spatial distribution patterns of sulfur isotopes, nodular carbonate, and ore textures in the McArthur River (HYC) Zn-Pb-Ag deposit, Northern Territory, Australia. Economic Geology, 99 (8). pp. 1687-1709. ISSN 0361-0128" name="eprints.citation" />
  292. <meta content="http://eprints.utas.edu.au/2048/1/Ireland.Large.McGoldrick.Blake.ECON.2004.pdf" name="eprints.document_url" />
  293. <link rel="schema.DC" href="http://purl.org/DC/elements/1.0/" />
  294. <meta content="Spatial distribution patterns of sulfur isotopes, nodular carbonate, and ore textures
  295. in the McArthur River (HYC) Zn-Pb-Ag deposit, Northern Territory, Australia" name="DC.title" />
  296. <meta content="Ireland, T." name="DC.creator" />
  297. <meta content="Large, R.R." name="DC.creator" />
  298. <meta content="McGoldrick, P.J." name="DC.creator" />
  299. <meta content="Blake, M.D." name="DC.creator" />
  300. <meta content="260100 Geology" name="DC.subject" />
  301. <meta content="The HYC Zn-Pb-Ag deposit at McArthur River is the largest known and least deformed Australian sedimenthosted
  302. stratiform base metal deposit. A study of mineralogical, geochemical, and isotopic zonation through the
  303. deposit reveals concentric distribution patterns in (1) the occurrence of nodular carbonate, (2) the δ34S composition
  304. of sphalerite, and (3) microscopic ore textures. The correlation of previously documented lateral metal
  305. zonation with these other zonation patterns precludes exclusive postsedimentation mineralization and provides
  306. some insight into the mechanisms and controls on synsedimentary to early diagenetic mineralization. This mineralization
  307. timing is also supported by new carbon and oxygen isotope analyses, recognition of two stages of texturally
  308. and isotopically distinct sphalerite, and reinterpretation of complex sulfide textures.
  309. Dolomitic carbonate nodules occur in the south, southwest, northwest, and northern fringes of the deposit
  310. and are interpreted to have surrounded the high-grade ore lenses prior to structural and erosive truncation.
  311. The carbon and oxygen isotope composition of these carbonate nodules is similar to the sedimentary dolomite
  312. within the ore lenses. There is no evidence for incorporation of light carbon derived from oxidation of organic
  313. material under closed-system conditions and the nodular carbonate probably formed under open-system conditions
  314. in communication with seawater. These nodules displace siltstone laminae and, therefore, likely formed
  315. in the very shallow subsea-floor environment.
  316. In ore lens 3, the δ34S of laminated early sphalerite (sp1) changes from a mean value of 5 per mil in the deposit
  317. center to a mean of 1.7 per mil in the extreme fringes. We interpret this to be the result of sulfide precipitation
  318. in a restricted marine basin. Later sphalerite (sp2) associated with nodular carbonate has a mean δ34S
  319. value of 9.8 per mil, whereas laminated early sphalerite (sp1) has a mean δ34S value of 3.8 per mil. This isotopic
  320. separation of the two paragenetic stages of sphalerite is found in immediately adjacent aggregates. Concentration
  321. of 34S in late sphalerite (sp2) is likely the result of closed-system conditions in the sediment pore fluid.
  322. Textures of laminated sphalerite change from strongly anastomosing in the central part of the deposit to
  323. plane laminar and patchy in the deposit fringes. Mass-balance calculations preclude substantial carbonate dissolution
  324. and a stylolitic origin for these textures. Instead we propose that rapidly precipitated sphalerite coagulated
  325. and trapped pelagic silt and early pyrite (py1) as it was deposited on the sea floor. In contrast, paragenetically
  326. late sphalerite (sp2) and pyrite (py2) must be diagenetic as they overprint and are pseudomorphous
  327. after the carbonate nodules. We propose a repeating paragenetic sequence of galena/sphalerite (sp1) → pyrite
  328. (py1) → nodular carbonate → sphalerite (sp2) → pyrite (py2), which accounts for all the textural complexity and
  329. isotopic disequilibrium between sulfide phases.
  330. The data presented in this paper suggest that base metal sulfides formed both in the water column and in
  331. the uppermost sediment pile. Biological and thermochemical sulfate reduction probably occurred simultaneously
  332. in different parts of a complex physicochemical system in which stratification of the marine environment
  333. is seen as the primary control on the lateral distribution of the mineralized facies. We propose a stratified water
  334. body in which sharp internal chemical gradients separate a surficial oxic layer, an anoxic layer, and a basal hypersaline
  335. brine pool. Asymmetric metal zonation across the deposit reflects individual pulses of metalliferous
  336. fluid that were introduced into the basin as a bottom-hugging dense current." name="DC.description" />
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  450.     <h1 class="ep_tm_pagetitle">Spatial distribution patterns of sulfur isotopes, nodular carbonate, and ore textures in the McArthur River (HYC) Zn-Pb-Ag deposit, Northern Territory, Australia</h1>
  451.     <p style="margin-bottom: 1em" class="not_ep_block"><span class="person_name">Ireland, T.</span> and <span class="person_name">Large, R.R.</span> and <span class="person_name">McGoldrick, P.J.</span> and <span class="person_name">Blake, M.D.</span> (2004) <xhtml:em>Spatial distribution patterns of sulfur isotopes, nodular carbonate, and ore textures in the McArthur River (HYC) Zn-Pb-Ag deposit, Northern Territory, Australia.</xhtml:em> Economic Geology, 99 (8). pp. 1687-1709. ISSN 0361-0128</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/2048/1/Ireland.Large.McGoldrick.Blake.ECON.2004.pdf"><img alt="[img]" src="http://eprints.utas.edu.au/style/images/fileicons/application_pdf.png" class="ep_doc_icon" border="0" /></a></td><td valign="top"><a href="http://eprints.utas.edu.au/2048/1/Ireland.Large.McGoldrick.Blake.ECON.2004.pdf"><span class="ep_document_citation">PDF</span></a> - Full text restricted - Requires a PDF viewer<br />1417Kb</td><td><form method="get" accept-charset="utf-8" action="http://eprints.utas.edu.au/cgi/request_doc"><input accept-charset="utf-8" value="2584" name="docid" 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/10.2113/99.8.1687">http://dx.doi.org/10.2113/99.8.1687</a></p><div class="not_ep_block"><h2>Abstract</h2><p style="padding-bottom: 16px; text-align: left; margin: 1em auto 0em auto">The HYC Zn-Pb-Ag deposit at McArthur River is the largest known and least deformed Australian sedimenthosted&#13;
  452. stratiform base metal deposit. A study of mineralogical, geochemical, and isotopic zonation through the&#13;
  453. deposit reveals concentric distribution patterns in (1) the occurrence of nodular carbonate, (2) the δ34S composition&#13;
  454. of sphalerite, and (3) microscopic ore textures. The correlation of previously documented lateral metal&#13;
  455. zonation with these other zonation patterns precludes exclusive postsedimentation mineralization and provides&#13;
  456. some insight into the mechanisms and controls on synsedimentary to early diagenetic mineralization. This mineralization&#13;
  457. timing is also supported by new carbon and oxygen isotope analyses, recognition of two stages of texturally&#13;
  458. and isotopically distinct sphalerite, and reinterpretation of complex sulfide textures.&#13;
  459. Dolomitic carbonate nodules occur in the south, southwest, northwest, and northern fringes of the deposit&#13;
  460. and are interpreted to have surrounded the high-grade ore lenses prior to structural and erosive truncation.&#13;
  461. The carbon and oxygen isotope composition of these carbonate nodules is similar to the sedimentary dolomite&#13;
  462. within the ore lenses. There is no evidence for incorporation of light carbon derived from oxidation of organic&#13;
  463. material under closed-system conditions and the nodular carbonate probably formed under open-system conditions&#13;
  464. in communication with seawater. These nodules displace siltstone laminae and, therefore, likely formed&#13;
  465. in the very shallow subsea-floor environment.&#13;
  466. In ore lens 3, the δ34S of laminated early sphalerite (sp1) changes from a mean value of 5 per mil in the deposit&#13;
  467. center to a mean of 1.7 per mil in the extreme fringes. We interpret this to be the result of sulfide precipitation&#13;
  468. in a restricted marine basin. Later sphalerite (sp2) associated with nodular carbonate has a mean δ34S&#13;
  469. value of 9.8 per mil, whereas laminated early sphalerite (sp1) has a mean δ34S value of 3.8 per mil. This isotopic&#13;
  470. separation of the two paragenetic stages of sphalerite is found in immediately adjacent aggregates. Concentration&#13;
  471. of 34S in late sphalerite (sp2) is likely the result of closed-system conditions in the sediment pore fluid.&#13;
  472. Textures of laminated sphalerite change from strongly anastomosing in the central part of the deposit to&#13;
  473. plane laminar and patchy in the deposit fringes. Mass-balance calculations preclude substantial carbonate dissolution&#13;
  474. and a stylolitic origin for these textures. Instead we propose that rapidly precipitated sphalerite coagulated&#13;
  475. and trapped pelagic silt and early pyrite (py1) as it was deposited on the sea floor. In contrast, paragenetically&#13;
  476. late sphalerite (sp2) and pyrite (py2) must be diagenetic as they overprint and are pseudomorphous&#13;
  477. after the carbonate nodules. We propose a repeating paragenetic sequence of galena/sphalerite (sp1) → pyrite&#13;
  478. (py1) → nodular carbonate → sphalerite (sp2) → pyrite (py2), which accounts for all the textural complexity and&#13;
  479. isotopic disequilibrium between sulfide phases.&#13;
  480. The data presented in this paper suggest that base metal sulfides formed both in the water column and in&#13;
  481. the uppermost sediment pile. Biological and thermochemical sulfate reduction probably occurred simultaneously&#13;
  482. in different parts of a complex physicochemical system in which stratification of the marine environment&#13;
  483. is seen as the primary control on the lateral distribution of the mineralized facies. We propose a stratified water&#13;
  484. body in which sharp internal chemical gradients separate a surficial oxic layer, an anoxic layer, and a basal hypersaline&#13;
  485. brine pool. Asymmetric metal zonation across the deposit reflects individual pulses of metalliferous&#13;
  486. fluid that were introduced into the basin as a bottom-hugging dense current.</p></div><table style="margin-bottom: 1em" cellpadding="3" class="not_ep_block" border="0"><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">SEDEX, Seafloor massive sulfide, sediment-hosted,zinc, lead, Mt Isa, McArthur Basin</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">ID Code:</th><td valign="top" class="ep_row">2048</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">11 Oct 2007 10:02</td></tr><tr><th valign="top" class="ep_row">Last Modified:</th><td valign="top" class="ep_row">09 Jan 2008 02:30</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=2048;">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=2048">item control page</a></p>
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