• Journal of fish pathology
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• v.23 no.2
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• pp.245-254
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• 2010

Effects of heavy metal ions on the gene expression of cytochrome P4501A (CYP1A) were examined in cultured eel hepatocytes. When the expression of CYP1A mRNA was measured by RT-PCR after incubation of eel hepatocytes with benzo[$\alpha$]pyrene (B[$\alpha$]P) at concentrations of 10-8~10-5 M, the CYP1A expression increased with B[$\alpha$]P treatment in a dose dependent manner, showing significant increase at concentrations more than 10-7 M. When the eel hepatocyte was treated with cadmium (10-6 and 10-5 M), the expression of CYP1A was inhibited and especially at higher concentration (10-5 M). The inhibition of CYP1A expression by cadmium was also observed in cells treated with B[$\alpha$]P. In another study, effects of heavy metal ions on the expression of CYP1A were examined in cultured hepatocytes isolated from eel which was treated previously with B[$\alpha$]P in vivo. Hepatocytes isolated from the liver of eel taken at 48 hours after injection of B[$\alpha$]P (10 mg/kg) were cultured for 2 days with cadmium, copper, lead or zinc (10-6 and 10-5 M). The expression of CYP1A was found to be suppressed by the metal ions compared with the control in which CYP1A was induced with previous treatment of B[$\alpha$]P in vivo. The present results may provide an important basic information for studying the effects of heavy metal ions on CYP1A expression in other species of fish and studying toxicological mechanisms of heavy metal ions in aquatic livings.

• Economic and Environmental Geology
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• v.25 no.4
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• pp.417-433
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• 1992

Lead-zinc-copper deposits of the Jeonheung and the Oksan mines around Euiseong area occur as hydrothermal quartz and calcite veins that crosscut Cretaceous sedimentary rocks of the Gyeongsang Basin. The mineralization occurred in three distinct stages (I, II, and III): (I) quartz-sulfides-sulfosalts-hematite mineralization stage; (II) barren quartz-fluorite stage; and (III) barren calcite stage. Stage I ore minerals comprise pyrite, chalcopyrite, sphalerite, galena and Pb-Ag-Bi-Sb sulfosalts. Mineralogies of the two mines are different, and arsenopyrite, pyrrhotite, tetrahedrite and iron-rich (up to 21 mole % FeS) sphalerite are restricted to the Oksan mine. A K-Ar radiometric dating for sericite indicates that the Pb-Zn-Cu deposits of the Euiseong area were formed during late Cretaceous age ($62.3{\pm}2.8Ma$), likely associated with a subvolcanic activity related to the volcanic complex in the nearby Geumseongsan Caldera and the ubiquitous felsite dykes. Stage I mineralization occurred at temperatures between > $380^{\circ}C$ and $240^{\circ}C$ from fluids with salinities between 6.3 and 0.7 equiv. wt. % NaCl. The chalcopyrite deposition occurred mostly at higher temperatures of > $300^{\circ}C$. Fluid inclusion data indicate that the Pb-Zn-Cu ore mineralization resulted from a complex history of boiling, cooling and dilution of ore fluids. The mineralization at Jeonheung resulted mainly from cooling and dilution by an influx of cooler meteoric waters, whereas the mineralization at Oksan was largely due to fluid boiling. Evidence of fluid boiling suggests that pressures decreased from about 210 bars to 80 bars. This corresponds to a depth of about 900 m in a hydrothermal system that changed from lithostatic (closed) toward hydrostatic (open) conditions. Sulfur isotope compositions of sulfide minerals (${\delta}^{34}S=2.9{\sim}9.6$ per mil) indicate that the ${\delta}^{34}S_{{\Sigma}S}$ value of ore fluids was ${\approx}8.6$ per mil. This ${\delta}^{34}S_{{\Sigma}S}$ value is likely consistent with an igneous sulfur mixed with sulfates (?) in surrounding sedimentary rocks. Measured and calculated hydrogen and oxygen isotope values of ore-forming fluids suggest meteoric water dominance, approaching unexchanged meteoric water values. Equilibrium thermodynamic interpretation indicates that the temperature versus $fs_2$ variation of stage I ore fluids differed between the two mines as follows: the $fs_2$ of ore fluids at Jeonheung changed with decreasing temperature constantly near the pyrite-hematite-magnetite sulfidation curve, whereas those at Oksan changed from the pyrite-pyrrhotite sulfidation state towards the pyrite-hematite-magnetite state. The shift in minerals precipitated during stage I also reflects a concomitant $fo_2$ increase, probably due to mixing of ore fluids with cooler, more oxidizing meteoric waters. Thermodynamic consideration of copper solubility suggests that the ore-forming fluids cooled through boiling at Oksan and mixing with less-evolved meteoric waters at Jeonheung, and that this cooling was the main cause of copper deposition through destabilization of copper chloride complexes.