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  5.     <title>UTas ePrints - Nature and origin of the fluids responsible for forming the Hellyer Zn–Pb–Cu, volcanic-hosted massive sulphide deposit, Tasmania, using fluid inclusions, and stable and radiogenic isotopes</title>
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  13.     <meta content="Solomon, M." name="eprints.creators_name" />
  14. <meta content="Gemmell, J.B." name="eprints.creators_name" />
  15. <meta content="Zaw, K." name="eprints.creators_name" />
  16. <meta content="Mike.Solomon@utas.edu.au" name="eprints.creators_id" />
  17. <meta content="Bruce.Gemmell@utas.edu.au" name="eprints.creators_id" />
  18. <meta content="Khin.Zaw@utas.edu.au" name="eprints.creators_id" />
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  23. <meta content="Nature and origin of the fluids responsible for forming the Hellyer
  24. Zn–Pb–Cu, volcanic-hosted massive sulphide deposit, Tasmania, using fluid inclusions, and stable and radiogenic isotopes " name="eprints.title" />
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  28. <meta content="Hellyer; Tasmania; Australia; Massive sulphide deposit; Stable isotopes" name="eprints.keywords" />
  29. <meta content="Definitive version is available online at http://www.sciencedirect.com/" name="eprints.note" />
  30. <meta content="The Hellyer massive sulphide deposit lies within the Mount Read Volcanics province of western Tasmania. Before mining, it consisted largely of pyrite, sphalerite, galena, arsenopyrite and chalcopyrite, and was overlain by discontinuous barite–sulphide and/or silica–sulphide assemblages. It overlay a downward-tapering cone of hydrothermally altered rocks that shows concentric
  31. mineral zonation and contains steeply inclined veins containing sulphide and/or barite. New laser ablation and existing conventional sulphur isotopic compositions of sulphides from the massive sulphide ore range from -5.0 per mil to 12.2 per mil. There is no significant spatial variation in sulphur isotopic composition in the sulphide ore, or evidence of significant change in the
  32. textural paragenesis, but there is considerable variation at millimetre scale within and between minerals. Apart from the few negative values, which may be of biogenic origin, the sulphur data can be explained by mixtures of sulphur reduced from seawater sulphate and that derived directly or indirectly from magma. The sulphur of the barite cap and the barite veins in the footwall (mostly 33.5–46.0 per mil) is probably also derived from seawater sulphate, and radiogenic 87Sr/86Sr values in the barite (0.70989–0.71144) suggest fluid circulation deep into the basement. delta 34 S values of disseminated sulphides in the footwall
  33. alteration cone are like those of overlying ore, the aqueous sulphur being totally reduced due to low fluid velocities and protracted rock interaction. However, unusually high delta 34 S sulphide values (up to 41.4 per mil) are found in some of the footwall vein sulphides, probably because in these veins the fluid velocities are enhanced and rock interaction limited, so that pyrite
  34. supersaturation may occur before reduction of entrained seawater sulphate is complete. High delta 34 S sulphide values (up to 45.6 per mil) also occur in ‘‘unaltered’’ volcanic rock outside the alteration cone and may be the product of local convection of seawater prior
  35. to, during, or (most probably) after massive sulphide mineralization. Fluid delta 18 O values calculated from isotopic analyses of quartz in footwall veins (8.5–11.8 per mil) and Th data range between 4.4 per mil and 3.1 per mil. Dolomite occurs with chlorite in the core of the footwall alteration cone immediately below the massive
  36. sulphide. Its isotopic composition (delta 13 C=1.5 to 2.8, delta 18 O=8.2–18.3 per mil) may reflect precipitation from an acid, seawaterderived, fluid having delta 13 C=1 per mil(the ambient seawater value), and delta 18 O ranging from 0 per mil to 6 per mil, or, alternatively, its
  37. composition is the result of mixing between modified seawater at 150 degrees C (delta 18 O=6 per mil) with 1% of fluid at 350 degrees C having delta 13 C= -6 and delta 18 O=0 per mil. Dolomites in the footwall veins (delta 13 C= -1.8 to 1.7, delta 18 O= 9.3–14.2 per mil) could be derived from an acid, seawater-derived fluid with negative delta 18 O values, or a fluid that has interacted with 600–700 Ma old, 13 C-enriched carbonates in the deep footwall during convective circulation. Both the chlorite-associated and the vein carbonates contain highly radiogenic Sr, possibly derived from Devonian metamorphic fluids.
  38. A re-interpretation of the fluid inclusion data of Khin Zaw et al. [Ore Geol. Rev. 10 (1996) 251] shows that there are three groups of fluids in the quartz of veins in the altered footwall, viz. (a) saline (6.6–14.8 wt.%) with Th = 170–246 degrees C, high K/Na, K/Ca and K/Fe values (fluid 1); (b) of similar salinity and temperature but with low K/Na, K/Ca and K/Fe values (fluid 2); and
  39. (c) an additional fluid of low salinity (2.9–7.0 wt.%) with Th = 289–322 degrees C, element ratios unknown (fluid 3). Fluid 1 has cation ratios like those of magmatic fluids in the K-silicate and phyllosilicate zones of the Panguna and Endeavour 26N porphyry copper deposits. Combined with the lack of alternative source of salts in the pre-ore rock sequences at Hellyer, fluid 1 is thought to be at least partly magmatic. Fluid 2 has cation ratios like those of modern black smoker and Kuroko ore-forming
  40. fluids, and was probably derived from both magmatic fluid and seawater; fluid 3 may be evolved seawater like that forming the deposits of the Hokuroku Basin.
  41. It is suggested that a pluton or plutonic complex of mixed crustal and lithospheric mantle parentage, like that of the volcanic rocks hosting the Hellyer orebody, was emplaced at several km depth below the deposit during faulting related to crustal extension. The heated zone over and around the pluton displaying plastic behaviour was sealed off from the overlying brittle zone in which groundwater (modified seawater) underwent convection due to heat transfer across the brittle-plastic boundary.
  42. The seal was broken intermittently due to tectonic extension or increased fluid pressure in the pluton, and magmatic fluid joined with convecting groundwater in the rising plume, leading to fluid mixing. Upward flow was focused on the Eastern Fault, the fracture system responsible for forming the basin in which the ore sulphides were sedimented." name="eprints.abstract" />
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  328. (e.g., Hokuroku, Hellyer, and Mt. Lyell): the likely role of fractures,
  329. deep footwall permeability, and rock buffering capacity.
  330. Geological Society of Australia Abstracts 59, 466.
  331. Solomon, M., Quesada, C., 2003. Zn –Pb –Cu massive sulphide
  332. deposits: brine pool types occur in collisional orogens, black
  333. smoker types in backarc and/or arc basins. Geology 31,
  334. 1029–1032.
  335. Solomon, M., Eastoe, C.J., Walshe, J.L., Green, G.R., 1988. Mineral
  336. deposits and sulfur isotope abundances in the Mount Read
  337. Volcanics between Que River and Mount Darwin, Tasmania.
  338. Economic Geology 83, 1307– 1328.
  339. Solomon, M., Tornos, F., Gaspar, O.C., 2002. Explanation for many
  340. of the unusual features of the massive sulfide deposits of the
  341. Iberian pyrite belt. Geology 30, 87–90.
  342. Stanton, R.L., Rafter, T.A., 1966. The isotopic constitution of sulphur
  343. in some stratiform lead–zinc ores. Mineralium Deposita 1,
  344. 16– 29.
  345. Turner, N.J., 1989. Precambrian. Geological Society of Australia
  346. Special Publication 15, 5 –46.
  347. Vanko, D.A., Bonnin-Mosbah, M., Philippot, P., Roedder, E.,
  348. Sutton, S.R., 2001. Fluid inclusions in quartz from oceanic
  349. hydrothermal specimens and the Bingham, Utah, porphyry-Cu
  350. deposit: a case study with PIXE and SXRF. Chemical Geology
  351. 171, 227– 238.
  352. Veizer, J., Ala, D., Azmy, K., Bruckschen, P., Buhl, D., Bruhn, F.,
  353. Carden, G.A.F., Diener, A., Ebneth, S., Godderis, Y., Jasper, T.,
  354. Korte, K., Pawellek, F., Podlaha, O.G., Strauss, H., 1999.
  355. 87Sr/86Sr, d13C and d18O evolution of Phanerozoic seawater.
  356. Chemical Geology 161, 59– 88.
  357. Von Damm, K.L., 1995. Controls on the chemistry and temporal
  358. variability of seafloor hydrothermal fluids. Geophysical Monograph
  359. 91, 222–247.
  360. Waters, J.C., Wallace, D.B., 1992. Volcanology and sedimentology
  361. of the host succession to the Hellyer and Que River volcanichosted
  362. massive sulphide deposits, northwestern Tasmania. Economic
  363. Geology 87, 650–666.
  364. Whitford, D.J., Sun, S.-S., Togashi, Y., 1982. Petrological and geochemical
  365. studies at Que River, Part 3. CSIRO Restricted Investigation
  366. Report 1332R (34 pp.).
  367. Whitford, D.J., Korsch, M.J., Solomon, M., 1992. Strontium
  368. isotope studies of barites: implications for the origin of base
  369. metal mineralization in Tasmania. Economic Geology 87,
  370. 953– 959.
  371. Whitford, D.J., Sharpe, R., Gemmell, J.B., 1993. Origin of barite
  372. from the Hellyer VHMS deposit, Tasmania: a Sr isotopic study.
  373. Geological Society of Australia Abstracts Series 24, 75.
  374. Wyman, W.F., 2001. Cambrian granite-related hydrothermal alteration
  375. and Cu–Au mineralisation in the southern Mt Read Volcanics,
  376. western Tasmania. Unpublished Ph.D. thesis, University
  377. of Tasmania, Hobart. 343 pp.
  378. Yang, J., Large, R.R., 2001. Computational modelling of hydrothermal
  379. ore-forming fluid migration in complex earth structures.
  380. In: Xie, H., Wang, Y., Jiang, Y., (Eds.), Computer
  381. Applications in the Mineral Industries. Swets and Zeitlinger,
  382. Lisse, pp. 115– 120.
  383. Zheng, Y.-F., Hoefs, J., 1993. Carbon and oxygen isotopic covariation
  384. in hydrothermal calcites. Theoretical modeling on mixing
  385. processes and application to Pb–Zn deposits in the Harz Mountains,
  386. Germany. Mineralium Deposita 28, 79–89." name="eprints.referencetext" />
  387. <meta content="Solomon, M. and Gemmell, J.B. and Zaw, K. (2004) Nature and origin of the fluids responsible for forming the Hellyer Zn–Pb–Cu, volcanic-hosted massive sulphide deposit, Tasmania, using fluid inclusions, and stable and radiogenic isotopes. Ore Geology Reviews, 25 (1-2). pp. 89-124. ISSN 0169-1368" name="eprints.citation" />
  388. <meta content="http://eprints.utas.edu.au/2051/1/Solomon.Gemmell.Zaw.OGR.2004.pdf" name="eprints.document_url" />
  389. <link rel="schema.DC" href="http://purl.org/DC/elements/1.0/" />
  390. <meta content="Nature and origin of the fluids responsible for forming the Hellyer
  391. Zn–Pb–Cu, volcanic-hosted massive sulphide deposit, Tasmania, using fluid inclusions, and stable and radiogenic isotopes " name="DC.title" />
  392. <meta content="Solomon, M." name="DC.creator" />
  393. <meta content="Gemmell, J.B." name="DC.creator" />
  394. <meta content="Zaw, K." name="DC.creator" />
  395. <meta content="260100 Geology" name="DC.subject" />
  396. <meta content="The Hellyer massive sulphide deposit lies within the Mount Read Volcanics province of western Tasmania. Before mining, it consisted largely of pyrite, sphalerite, galena, arsenopyrite and chalcopyrite, and was overlain by discontinuous barite–sulphide and/or silica–sulphide assemblages. It overlay a downward-tapering cone of hydrothermally altered rocks that shows concentric
  397. mineral zonation and contains steeply inclined veins containing sulphide and/or barite. New laser ablation and existing conventional sulphur isotopic compositions of sulphides from the massive sulphide ore range from -5.0 per mil to 12.2 per mil. There is no significant spatial variation in sulphur isotopic composition in the sulphide ore, or evidence of significant change in the
  398. textural paragenesis, but there is considerable variation at millimetre scale within and between minerals. Apart from the few negative values, which may be of biogenic origin, the sulphur data can be explained by mixtures of sulphur reduced from seawater sulphate and that derived directly or indirectly from magma. The sulphur of the barite cap and the barite veins in the footwall (mostly 33.5–46.0 per mil) is probably also derived from seawater sulphate, and radiogenic 87Sr/86Sr values in the barite (0.70989–0.71144) suggest fluid circulation deep into the basement. delta 34 S values of disseminated sulphides in the footwall
  399. alteration cone are like those of overlying ore, the aqueous sulphur being totally reduced due to low fluid velocities and protracted rock interaction. However, unusually high delta 34 S sulphide values (up to 41.4 per mil) are found in some of the footwall vein sulphides, probably because in these veins the fluid velocities are enhanced and rock interaction limited, so that pyrite
  400. supersaturation may occur before reduction of entrained seawater sulphate is complete. High delta 34 S sulphide values (up to 45.6 per mil) also occur in ‘‘unaltered’’ volcanic rock outside the alteration cone and may be the product of local convection of seawater prior
  401. to, during, or (most probably) after massive sulphide mineralization. Fluid delta 18 O values calculated from isotopic analyses of quartz in footwall veins (8.5–11.8 per mil) and Th data range between 4.4 per mil and 3.1 per mil. Dolomite occurs with chlorite in the core of the footwall alteration cone immediately below the massive
  402. sulphide. Its isotopic composition (delta 13 C=1.5 to 2.8, delta 18 O=8.2–18.3 per mil) may reflect precipitation from an acid, seawaterderived, fluid having delta 13 C=1 per mil(the ambient seawater value), and delta 18 O ranging from 0 per mil to 6 per mil, or, alternatively, its
  403. composition is the result of mixing between modified seawater at 150 degrees C (delta 18 O=6 per mil) with 1% of fluid at 350 degrees C having delta 13 C= -6 and delta 18 O=0 per mil. Dolomites in the footwall veins (delta 13 C= -1.8 to 1.7, delta 18 O= 9.3–14.2 per mil) could be derived from an acid, seawater-derived fluid with negative delta 18 O values, or a fluid that has interacted with 600–700 Ma old, 13 C-enriched carbonates in the deep footwall during convective circulation. Both the chlorite-associated and the vein carbonates contain highly radiogenic Sr, possibly derived from Devonian metamorphic fluids.
  404. A re-interpretation of the fluid inclusion data of Khin Zaw et al. [Ore Geol. Rev. 10 (1996) 251] shows that there are three groups of fluids in the quartz of veins in the altered footwall, viz. (a) saline (6.6–14.8 wt.%) with Th = 170–246 degrees C, high K/Na, K/Ca and K/Fe values (fluid 1); (b) of similar salinity and temperature but with low K/Na, K/Ca and K/Fe values (fluid 2); and
  405. (c) an additional fluid of low salinity (2.9–7.0 wt.%) with Th = 289–322 degrees C, element ratios unknown (fluid 3). Fluid 1 has cation ratios like those of magmatic fluids in the K-silicate and phyllosilicate zones of the Panguna and Endeavour 26N porphyry copper deposits. Combined with the lack of alternative source of salts in the pre-ore rock sequences at Hellyer, fluid 1 is thought to be at least partly magmatic. Fluid 2 has cation ratios like those of modern black smoker and Kuroko ore-forming
  406. fluids, and was probably derived from both magmatic fluid and seawater; fluid 3 may be evolved seawater like that forming the deposits of the Hokuroku Basin.
  407. It is suggested that a pluton or plutonic complex of mixed crustal and lithospheric mantle parentage, like that of the volcanic rocks hosting the Hellyer orebody, was emplaced at several km depth below the deposit during faulting related to crustal extension. The heated zone over and around the pluton displaying plastic behaviour was sealed off from the overlying brittle zone in which groundwater (modified seawater) underwent convection due to heat transfer across the brittle-plastic boundary.
  408. The seal was broken intermittently due to tectonic extension or increased fluid pressure in the pluton, and magmatic fluid joined with convecting groundwater in the rising plume, leading to fluid mixing. Upward flow was focused on the Eastern Fault, the fracture system responsible for forming the basin in which the ore sulphides were sedimented." name="DC.description" />
  409. <meta content="2004-08" name="DC.date" />
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  522.     <h1 class="ep_tm_pagetitle">Nature and origin of the fluids responsible for forming the Hellyer Zn–Pb–Cu, volcanic-hosted massive sulphide deposit, Tasmania, using fluid inclusions, and stable and radiogenic isotopes</h1>
  523.     <p style="margin-bottom: 1em" class="not_ep_block"><span class="person_name">Solomon, M.</span> and <span class="person_name">Gemmell, J.B.</span> and <span class="person_name">Zaw, K.</span> (2004) <xhtml:em>Nature and origin of the fluids responsible for forming the Hellyer Zn–Pb–Cu, volcanic-hosted massive sulphide deposit, Tasmania, using fluid inclusions, and stable and radiogenic isotopes.</xhtml:em> Ore Geology Reviews, 25 (1-2). pp. 89-124. ISSN 0169-1368</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/2051/1/Solomon.Gemmell.Zaw.OGR.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/2051/1/Solomon.Gemmell.Zaw.OGR.2004.pdf"><span class="ep_document_citation">PDF</span></a> - Full text restricted - Requires a PDF viewer<br />2769Kb</td><td><form method="get" accept-charset="utf-8" action="http://eprints.utas.edu.au/cgi/request_doc"><input accept-charset="utf-8" value="2588" 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/10.1016/j.oregeorev.2003.11.001">http://dx.doi.org/10.1016/j.oregeorev.2003.11.001</a></p><div class="not_ep_block"><h2>Abstract</h2><p style="padding-bottom: 16px; text-align: left; margin: 1em auto 0em auto">The Hellyer massive sulphide deposit lies within the Mount Read Volcanics province of western Tasmania. Before mining, it consisted largely of pyrite, sphalerite, galena, arsenopyrite and chalcopyrite, and was overlain by discontinuous barite–sulphide and/or silica–sulphide assemblages. It overlay a downward-tapering cone of hydrothermally altered rocks that shows concentric&#13;
  524. mineral zonation and contains steeply inclined veins containing sulphide and/or barite. New laser ablation and existing conventional sulphur isotopic compositions of sulphides from the massive sulphide ore range from -5.0 per mil to 12.2 per mil. There is no significant spatial variation in sulphur isotopic composition in the sulphide ore, or evidence of significant change in the&#13;
  525. textural paragenesis, but there is considerable variation at millimetre scale within and between minerals. Apart from the few negative values, which may be of biogenic origin, the sulphur data can be explained by mixtures of sulphur reduced from seawater sulphate and that derived directly or indirectly from magma. The sulphur of the barite cap and the barite veins in the footwall (mostly 33.5–46.0 per mil) is probably also derived from seawater sulphate, and radiogenic 87Sr/86Sr values in the barite (0.70989–0.71144) suggest fluid circulation deep into the basement. delta 34 S values of disseminated sulphides in the footwall&#13;
  526. alteration cone are like those of overlying ore, the aqueous sulphur being totally reduced due to low fluid velocities and protracted rock interaction. However, unusually high delta 34 S sulphide values (up to 41.4 per mil) are found in some of the footwall vein sulphides, probably because in these veins the fluid velocities are enhanced and rock interaction limited, so that pyrite&#13;
  527. supersaturation may occur before reduction of entrained seawater sulphate is complete. High delta 34 S sulphide values (up to 45.6 per mil) also occur in ‘‘unaltered’’ volcanic rock outside the alteration cone and may be the product of local convection of seawater prior&#13;
  528. to, during, or (most probably) after massive sulphide mineralization. Fluid delta 18 O values calculated from isotopic analyses of quartz in footwall veins (8.5–11.8 per mil) and Th data range between 4.4 per mil and 3.1 per mil. Dolomite occurs with chlorite in the core of the footwall alteration cone immediately below the massive&#13;
  529. sulphide. Its isotopic composition (delta 13 C=1.5 to 2.8, delta 18 O=8.2–18.3 per mil) may reflect precipitation from an acid, seawaterderived, fluid having delta 13 C=1 per mil(the ambient seawater value), and delta 18 O ranging from 0 per mil to 6 per mil, or, alternatively, its&#13;
  530. composition is the result of mixing between modified seawater at 150 degrees C (delta 18 O=6 per mil) with 1% of fluid at 350 degrees C having delta 13 C= -6 and delta 18 O=0 per mil. Dolomites in the footwall veins (delta 13 C= -1.8 to 1.7, delta 18 O= 9.3–14.2 per mil) could be derived from an acid, seawater-derived fluid with negative delta 18 O values, or a fluid that has interacted with 600–700 Ma old, 13 C-enriched carbonates in the deep footwall during convective circulation. Both the chlorite-associated and the vein carbonates contain highly radiogenic Sr, possibly derived from Devonian metamorphic fluids.&#13;
  531. A re-interpretation of the fluid inclusion data of Khin Zaw et al. [Ore Geol. Rev. 10 (1996) 251] shows that there are three groups of fluids in the quartz of veins in the altered footwall, viz. (a) saline (6.6–14.8 wt.%) with Th = 170–246 degrees C, high K/Na, K/Ca and K/Fe values (fluid 1); (b) of similar salinity and temperature but with low K/Na, K/Ca and K/Fe values (fluid 2); and&#13;
  532. (c) an additional fluid of low salinity (2.9–7.0 wt.%) with Th = 289–322 degrees C, element ratios unknown (fluid 3). Fluid 1 has cation ratios like those of magmatic fluids in the K-silicate and phyllosilicate zones of the Panguna and Endeavour 26N porphyry copper deposits. Combined with the lack of alternative source of salts in the pre-ore rock sequences at Hellyer, fluid 1 is thought to be at least partly magmatic. Fluid 2 has cation ratios like those of modern black smoker and Kuroko ore-forming&#13;
  533. fluids, and was probably derived from both magmatic fluid and seawater; fluid 3 may be evolved seawater like that forming the deposits of the Hokuroku Basin.&#13;
  534. It is suggested that a pluton or plutonic complex of mixed crustal and lithospheric mantle parentage, like that of the volcanic rocks hosting the Hellyer orebody, was emplaced at several km depth below the deposit during faulting related to crustal extension. The heated zone over and around the pluton displaying plastic behaviour was sealed off from the overlying brittle zone in which groundwater (modified seawater) underwent convection due to heat transfer across the brittle-plastic boundary.&#13;
  535. The seal was broken intermittently due to tectonic extension or increased fluid pressure in the pluton, and magmatic fluid joined with convecting groundwater in the rising plume, leading to fluid mixing. Upward flow was focused on the Eastern Fault, the fracture system responsible for forming the basin in which the ore sulphides were sedimented.</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">Additional Information:</th><td valign="top" class="ep_row">Definitive version is available online at http://www.sciencedirect.com/</td></tr><tr><th valign="top" class="ep_row">Keywords:</th><td valign="top" class="ep_row">Hellyer; Tasmania; Australia; Massive sulphide deposit; Stable isotopes</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">2051</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">10 Oct 2007 03:44</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=2051;">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=2051">item control page</a></p>
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