Copper Mineralization in the Haman-Gunbuk Area, Gyeongsangnamdo-Province: Fluid Inclusion and Stable Isotope Study
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(7) . . . . . . Copper Mineralization in the Haman-Gunbuk Area, GyeongsangnamdoProvince: Fluid Inclusion and Stable Isotope Study Chul-Ho Heo1*, Seong-Taek Yun2, Sang-Hoon Choi3, Seon-Gyu Choi2 and Chil-Sup So2 1. Ecological Research Institute, National Parks Authority, Seoul 121-717, Korea Department of Earth and Environmental Sciences, Korea University, Seoul 136-701, Korea 3 Department of Earth and Environmental Sciences, Chungbuk National University, Cheongju 361-763, Korea 2. The Haman-Gunbuk mineralized area is located within the Cretaceous Gyeongsang Basin along the southeastern part of the Korean peninsula. Major ore minerals, magnetite, scheelite, molybdenite and chalcopyrite, together with base-metal sulfides and minor sulfosalts, occur in fissure-filling tourmaline, quartz and carbonates veins contained within Cretaceous sedimentary and volcanic rocks and/or granodiorite (118±3.0 Ma). The ore and gangue mineral paragenesis can be divided into three distinct stages: Stage I, tourmaline+quartz+Fe-Cu ore mineralization; Stage II, quartz+sulfides+sulfosalts+carbonates; Stage III, barren calcite. Earliest fluids are recorded in stage I and early portions of stage II veins as hypersaline (35~70 equiv. wt.% NaCl+KCl) and vapor-rich inclusions which homogenize from ~300oC to ≥500oC . The high-salinity fluids are complex chloride brines with significant concentrations of sodium, potassium, iron, copper, and sulfur, though sulfide minerals are not associated with the early mineral assemblage produced by this fluid. Later solutions circulated through newly formed fractures and reopened veins, and are recorded as lower-salinity(less than ~20 equiv. wt.% NaCl) fluid inclusions which homogenize primarily from ~200 to 400oC. The oxygen and hydrogen isotopic compositions of fluid in the Haman-Gunbuk hydrothermal system represents a progressive shift from magmatic-hydrothermal dominance during early mineralization stage toward meteoric-hydrothermal dominance during late mineralization stage. The earliest hydrothermal fluids to circulate within the granodiorite stock localizing the ore body at Haman-Gunbuk could have exsolved from the crystallizing magma and unmixed into hypersaline liquid and H2O-NaCl vapor. As these magmatic fluids moved through fractures, tourmaline and early Fe, W, Mo, Cu ore mineralization occurred without concomitant deposition of other sulfides and sulfosalts. Later solutions of dominantly meteoric origin progressively formed hypogene copper and base-metal sulfides, and sulfosalt mineralization.. The Haman-Gunbuk area, copper mineralization, fluid inclusion, stable isotope.
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(29) ! " # $%& '(. . Table 1. Rb-Sr data of specimen from the Haman-Gunbuk Cu area (see Fig. 1 for locality) Rb-Sr data two-point isochrons 86. Granodiorite whole-rock biotite. GB-1. 87. Sr(ppm). Sample no. Description. 87. Rb(ppm). Sr/86Sr. 2.300. 0.7137. 0.0381. 3.193. 79.0. 0.7547. 24.43. . . . . . . . . . .
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(61) . . Phase disappearance temperatures of type IIIa, IIIb and IIIc inclusions in vein minerals from the Haman-Gunbuk area.. ,: aS $"7U +(> ';A 666+ wMK $ *o '« )#KFò: hFÌW M> F { wMK$ hFÌE '"F , *o/a: a $"7U +(28 ÒK3 '« "#Kf w 2 6> wMK '" Â$ zL7 U .> wMK$ wMK ¬A @;7U j©28 ó '7U ´> . ';A 666+. * 31. ;A 666+. .
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(77) ! " # $%& '( . . . Frequency diagram of salinities of fluid inclusions in vein minerals of the Haman-Gunbuk area. Symbols are the same as in Fig. 4.. Ðaq ó wMK$ @ Q yz@#j ?#j . . . . #. . . . . #. . . . . . 0#. . . #( ' qr ó wMK oñA >Y ý > #( ' Ðaq oñ A F> . -. ;A. 6. . #. 41. . 0 41 . . ;A. 666. 0. . 0 41 . .
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(85) . . H2O-NaCl-KCl phase diagram (in wt.%) showing fields occupied by types IIIa, IIIb, and IIIc inclusion fluids (figure modified from Cloke and Kesler, 1979). Thin solid lines are isotherms and dashed lines are isobars. Dotdash lines projecting to H2O are lines of constant K/Na (atomic ratio). Field A shows compositional range of type IIIa and IIIb (sylvite-free) inclusions. Field C shows compositional range of type IIIc inclusions.. ~ ¢ . : ?@ 2 oñW b> F { *o7U w( wMK{$ ºü Aq MNW M2A wMK ºB3 ®4' > - wMK$ oñ wMK ºB3 ®4A %&> oñ wMK *o +(¢ ~º $ ²$ º y? ²9 ï w(Of r> §I6> ×z F ²F FÞ $ +(¢A wC¢W º ²z I 678 y MN¢A R¢ B'"$" +(¢: ºä I 6> O b´D:A Aq I/P wMK{F wMK{X> ì 2E F{ wMK{ Gb +(¢ ~W X<"> ¢ '"F ì wMKF L7U ®4> F { wMK{$ pgL7U wMK =28 Aq MN TDL` ¦ ± '"f x/2 . #. . 41. . . . * . . ;A. . . #. 6. . ;A 66. . !7
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(107) Filling temperature (TfC) versus salinity diagram for primary and secondary inclusions from the HamanGunbuk area. Dashed lines are isobars.. = . . . . 5 @; . # .
(108)
(109) . . Table 2. Sulfur isotope data of sulfide minerals from the Haman-Gunbuk mineralized area δ34SH2S (‰)3 5.3 5.3 5.8 4.4 4.4 5.4 5.4 6.0 4.0 5.2 5.2 3.6 5.5 5.5 4.6 4.6 4.6 4.5 14.6 11.6 11.5 12.3 10.7 7.7 11.7 10.9. δ34S ∆34S Sample T (ºC)1 Mineral Stage T (ºC)2 (‰) (‰) no. Haman HM-1-1 Pyrite I 6.5 1.3 315±45 315 HM-1-2 Chalcopyrite I 5.2 315 HM-3 Pyrite I 6.9 340 HM-21-1 Pyrite IIa 5.7 1.5 274±45 274 HM-21-2 Chalcopyrite IIa 4.2 274 HM-5-1 Pyrite IIa 6.5 0.8 342±55 342 HM-5-2 Pyrrhotite IIa 5.7 342 HM-33 Pyrrhotite IIa 6.3 350 HM-23 Pyrrhotite IIa 4.3 300 HM-31-1 Pyrite IIb 6.6 1.6 257±45 257 HM-31-2 Chalcopyrite IIb 5.0 257 HM-34 Pyrite IIb 5.1 250 Gunbuk GB-2 Pyrite I 6.6 340 GB-6 Pyrite IIa 6.6 340 GB-7 Sphalerite IIa 5.0 260 GB-10 Sphalerite IIb 5.0 2.6 254±30 254 GB-11 Galena IIb 2.4 254 GB-5 Sphalerite IIb 4.9 240 Jeilgunbuk JG-11-1 Pyrite I 15.7 340 JG-11-2 Chalcopyrite I 11.5 320 JG-6-1 Chalcopyrite IIa 11.3 300 JG-6-2 Chalcopyrite IIa 12.1 300 JG-1 Pyrrhotite IIa 11.0 330 JG-21 Pyrrhotite IIa 8.0 300 JG-14-3 Chalcopyrite IIb 11.5 250 JG-14 Chalcopyrite IIb 10.8 250 1 Calculated sulfur isotope temperatures using compiled data of Ohmoto and Rye (1979) 2 Based on fluid inclusion temperatures and paragenetic constraints and/or sulfur isotope temperatures 3 Calculated from the sulfur isotope fractionation equations in Ohmoto and Rye (1979) Mine. gOôf XFA #( ' niq n q n iq éiq #( ' niq n q í q ‰ Ð qX{ δ W$ µµ ° F8 ± ° ± ± ° ± g ~ ¢W E«[> MNwMK´° ¯W hø7U HIMN p¢W ºJ2Þ ¯j δ W$ 0 ‰ F8 yz@#j Wf yò2Þ ‰ ~: a> n ~ OP ~A ? @G HIMN: '< nF Ô 7U M½eYf b >- 0 ‰ δ Wf \ ²7U ´4A `1 %&' ()* ? @#j ≥ ‰ δ Wf \ ²7U ´4A L* yz@#j . . . . (. . . . . . . #. . . . . 0. 0. . #. . . . . . 0. . .
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(118) ! " # $%& '(. . . Table 3. Carbon, oxygen and hydrogen isotope data for various minerals and inclusion fluids, Haman-Gunbuk mineralized area Sample no. HM-8 HM-7 HM-21 HN HM-6 Hi HM-31 GB-31 GB-8 JG-14. Mine Haman. Gunbuk Jeilgunbuk. Mineral. Stage. Quartz Quartz Quartz Calcite Calcite Calcite Calcite Quartz Calcite Calcite. I I II II II III III I III II. δ13C(‰). -5.8 -6.0 -8.0 -6.4 -7.4 -2.6. δ18O(‰). T(ºC)1). 12.4 10.9 11.0 9.6 8.8 11.8 8.1 11.2 8.8 11.6. 430∼360 370∼320 330∼260 240∼190 180∼150 180∼150 170∼150 480∼390 200∼170 220∼190. δ18Owater(‰)2 δDwater(‰) 8.9∼ 7.4 6.1∼ 4.7 5.1∼ 2.6 1.9∼ -0.5 -1.9∼ -3.8 1.1∼ -0.8 -3.2∼ -4.5 8.7∼ 6.9 -0.7∼ -2.5 3.1∼ 1.5. -68 -72 -72 -74 -78 -90 -68 -78. 1. Based on fluid inclusion temperatures and paragenetic constraints 2 Calculated from the quartz-water oxygen isotope fractionation equations of Matsuhisa et al. (1979). ´W "7U 8_4> wMK K: W$ >Y ý> #( ' ‰ #( ' ‰ #( ' ‰ . -. #
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