Hostname: page-component-78c5997874-lj6df Total loading time: 0 Render date: 2024-11-14T00:05:05.210Z Has data issue: false hasContentIssue false
  • English
  • Français

Relation Between Interlayer Composition of Authigenic Smectite, Mineral Assemblages, I/S Reaction Rate and Fluid Composition in Silicic Ash of the Nankai Trough

Published online by Cambridge University Press:  28 February 2024

Harue Masuda ,
James R. O'Neil ,
Wei-Teh Jiang  and
Donald R. Peacor
Harue Masuda
Affiliation:
Department of Geosciences, Osaka City University, Sumiyoshi, Osaka 558, Japan
James R. O'Neil
Affiliation:
Department of Geological Sciences, University of Michigan, Ann Arbor, Michigan 48109
Wei-Teh Jiang*
Affiliation:
Department of Geological Sciences, University of Michigan, Ann Arbor, Michigan 48109
Donald R. Peacor
Affiliation:
Department of Geological Sciences, University of Michigan, Ann Arbor, Michigan 48109
*
†Present address: Department of Earth Sciences, National Cheng Kung University, Tainan, Taiwan 70101, R.O.C.
Rights & Permissions [Opens in a new window]

Abstract

Core share and HTML view are not available for this content. However, as you have access to this content, a full PDF is available via the ‘Save PDF’ action button.

The compositions, fabrics and structures of authigenic minerals that formed recently from silicic volcanic ash layers from a 1300-meter sediment column obtained at ODP Site 808 of the Nankai Trough were studied using XRD, STEM, AEM and SEM. Smectite and zeolites were first detected as alteration products of volcanic glass with increasing depth, as follows: smectite at 200 m below seafloor (mbsf) (20 °C), clinoptilolite at 640 mbsf (60 °C) and analcime at 810 mbsf (75 °C).

A primitive clay precursor to smectite was observed as a direct alteration product of glass at 366 mbsf (approximately 30 °C). High defect smectite with lattice fringe spacings of 12 to 17 Å and having a cellular texture filling pore space between altering glass shards occurs at 630 mbsf. Packets of smectite become larger and less disordered with increasing depth and temperature. The smectite that forms as a direct alteration product of volcanic glass has K as the dominant interlayer cation.

With increasing depth, smectite becomes depleted in K as the proportion of clinoptilolite increases, and then becomes depleted in Na as the proportion of analcime increases. The composition of the exchangeable interlayer of smectite appears to be controlled by the formation first of K-rich clinoptilolite and then Na-rich analcime, via the pore fluid, giving rise at depth to Ca-rich smectite. Smectite reacted to form illite in the interbedded shales but not in the bentonites. Paucity of K in smectite and pore fluids, due to formation of clinoptilolite under closed system conditions, is believed to have inhibited the reaction relative to shales.

Keywords

Chemical ControlsGlass AlterationIllite/SmectiteInterlayer CationsPorewater CompositionPrecursor Clay MineralsSilicic AshSmectite
Type
Research Article
Information
Clays and Clay Minerals , Volume 44 , Issue 4 , August 1996 , pp. 443 - 459
Copyright
Copyright © 1996, The Clay Minerals Society

References

Ahn, J.H., Peacor, D.R. and Coombs, D.S.. 1988. Formation mechanisms of illite, chlorite and mixed-layer illite-chlorite in Triassic volcanogenic sediments from the Southland Syncline, New Zealand. Contrib Mineral Petrol 99: 82–89.CrossRefGoogle Scholar
Altener, S.P. and Grim, R.E.. 1990. Mineralogy, chemistry, and diagenesis of tuffs in the Sucker Creek Formation (Miocene), eastern Oregon. Clays & Clay Miner 38: 561–572.CrossRefGoogle Scholar
Anjos, S.M.C.. 1991. Absence of clay diagenesis in Cretaceous-Tertiary marine shales, Campos Basin, Brazil. Clays & Clay Miner 34: 424–434.CrossRefGoogle Scholar
Aoki, Y., Yamano, T. and Kato, S.. 1982. Detailed structure of the Nankai Trough from migrated seismic sections. In: Watkins, J., Drake, C.L., editors. Studies in continental margin geology. AAPG Mem 34: 309–322.Google Scholar
Aoki, Y., Kinoshita, H. and Kagami, H.. 1986. Evidence of a low-velocity layer beneath the accretionary prism of the Nankai Trough: Inferences from a synthetic sonic log. In: Kagami, H., Karig, D.E., Coulbourn, W., et al. Init. Repts. DSDP, 87A, Washington: U.S. Govt. Printing Office, p 727–743.Google Scholar
Banfield, J.F., Jones, B.F. and Veblen, D.R.. 1991. An AEM-TEM study of weathering and diagenesis, Abert Lake, Oregon: I. Weathering reactions in the volcanics. Geochim Cosmochim Acta 55: 2781–2798.CrossRefGoogle Scholar
Boles, J.R. and Franks, S.G.. 1979. Clay diagenesis in Wilcox sandstones of southwest Texas: Implications of smectite diagenesis on sandstone cementation. J Sed Petrol 49: 55–70.Google Scholar
Buatier, M.D., Peacor, D.R. and O'Neil, J.R.. 1992. Smectite illite transition in Barbados accretionary wedge sediments: TEM and AEM evidence for dissolution/crystallization at low temperature. Clays & Clay Miner 40: 65–80.CrossRefGoogle Scholar
Dickens. Personal Communication. Department of Geological Sciences. University of Michigan. 1006 C.C. Little Building. Ann Arbor, MI 48109.Google Scholar
Eberl, D.D. and Hower, J.. 1976. Kinetics of illite formation. Geol Soc Am Bull 87: 1326–1330.2.0.CO;2>CrossRefGoogle Scholar
Eggleton, R.A.. 1987. Non-crystalline Fe-Si-Al-oxyhydroxides. Clays & Clay Miner 35: 29–37.CrossRefGoogle Scholar
Eslinger, E.V. and Savin, S.. 1973. Oxygen isotope geothermometry of the burial metamorphic rocks of the Precambrian Belt Supergroup, Glacier National Park, Montana. Geol Soc Am Bull 85: 2549–2560.2.0.CO;2>CrossRefGoogle Scholar
Freed, R.L. and Peacor, D.R.. 1992. Diagenesis and the formation of authigenic illite-rich I/S crystals in Gulf Coast shales: TEM study of clay separates. J Sed Petrol 62: 220–234.Google Scholar
Hover. Personal Communication. Department of Geological Sciences. University of Michigan. 1006 C.C. Little Building. Ann Arbor, MI 48109.Google Scholar
Howard, J.J. and Roy, D.M.. 1985. Development of layer charge kinetics of experimental smectite alteration. Clays & Clay Miner 33: 81–88.CrossRefGoogle Scholar
Hower, J., Eslinger, E.V., Hower, M.E. and Perry, E.A.. 1976. Mechanism of burial metamorphism of argillaceous sediments: 1. Mineralogical and chemical evidence. Geol Soc Am Bull 87: 725–737.2.0.CO;2>CrossRefGoogle Scholar
Huang, W.-L., Longo, J.M. and Pevear, D.R.. 1993. An experimentally derived kinetic model for smectite-to-illite conversion and its use as a geothermometer. Clays & Clay Miner 41: 162–177.CrossRefGoogle Scholar
Inoue, A.. 1983. Potassium fixation by clay minerals during hydrothermal treatment. Clays & Clay Miner 31: 81–91.CrossRefGoogle Scholar
Inoue, A. and Utada, M.. 1983. Further investigation of a conversion series of dioctahedral mica/smectites in the Shinzan hydrothermal alteration area, northeast Japan. Clays & Clay Miner 31: 401–412.CrossRefGoogle Scholar
Jezak, P.A. and Noble, D.C.. 1978. Natural hydration and ion exchange of obsidian: An electron microprobe study. Am Mineral 63: 266–273.Google Scholar
Jiang, W.-T., Peacor, D.R., Merriman, R.J. and Roberts, B.. 1990. Transmission and analytical electron microscopic study of mixed-layer illite/smectite formed as an apparent replacement product of diagenetic illite. Clays & Clay Miner 38: 449–468.CrossRefGoogle Scholar
Kagami, H., Karig, D.E. and Coulbourn, W.S. et al. 1986. Init. Repts. DSDP 87. Washington: U.S. Govt. Printing Office. 986 p.Google Scholar
Kaiko Research Group. 1986. Topography and structure of trenches around Japan—Data atlas of Franco-Japanese Kaiko Project, Phase I, Taira A, Tokuyama H, editors. Tokyo: University Tokyo Press. 305 p.Google Scholar
RWO'B, K.n.o.x. and Fletcher, B.N.. 1978. Bentonites in the lower D beds (Ryazanian) of the Speeton Clay of Yorkshire. Proc Yorkshire Geol Soc 42: 21–27.Google Scholar
Lanson, B. and Champion, D.. 1991. The I/S-to-illite reaction in the late stage diagenesis. Am J Sci 291: 473–506.CrossRefGoogle Scholar
Masuda, H., Tanaka, H., Gamo, T., Soh, W. and Taira, A.. 1993. Major element chemistry and alteration mineralogy of volcanic ash, Site 808 in the Nankai Trough. In: Hill, I., Taira, A., Firth, J.V., editors. Proc. Ocean Drill. Prog., Sci. Results 131B. Ocean Drilling Program, College Station, TX. p. 175–183.Google Scholar
McMurtry, G.M., Wang, C.-H. and Yeh, H.-W.. 1983. Chemical and isotopic investigation into the origin of clay minerals from the Galapagos hydrothermal mound field. Geochim Cosmochim Acta 47: 475–489.CrossRefGoogle Scholar
Moore, G.F., Shipley, T.H., Stoffa, P.L., Karig, D.E., Taira, A., Kuramoto, S., Tokuyama, H. and Suyehiro, K.. 1990. Structure of the Nankai Trough accretionary zone from multichannel seismic reflection data. J Geophys Res 95: 8753–8765.CrossRefGoogle Scholar
Peacor, D.R.. 1992. Diagenetic and low-metamorphism of shales and slates. In: Buseck, P.R., editor. Minerals and reactions at the atomic scale: Transmission Electron Microscopy, Rev Mineral 27: 335–380.CrossRefGoogle Scholar
Perry, E. and Hower, J.. 1970. Burial diagenesis in Gulf Coast pelitic sediments. Clays & Clay Miner 18: 165–177.CrossRefGoogle Scholar
Petit, J.-C., Dellamea, G., Dran, J.-C., Magontheir, M.-C. and Paccagnella, A.. 1990. Hydrated-layer formation during dissolution of complex silicate glasses and minerals. Geochim Cosmochim Acta 54: 1941–1955.CrossRefGoogle Scholar
Roberson, H.E. and Lahann, R.W.. 1981. Smectite to illite conversion rates: Effects of solution chemistry. Clays & Clay Miner 29: 129–135.CrossRefGoogle Scholar
Small, J.S.. 1993. Experimental determination of the rates of precipitation of authigenic illite and kaolinite in the presence of aqueous oxalate and comparison to the K/Ar ages of authigenic illite in reservoir sandstones. Clays & Clay Miner 41: 191–208.CrossRefGoogle Scholar
Steiner, A.. 1968. Clay minerals in hydrothermally altered rocks at Wairakei, New Zealand. Clays & Clay Miner 16: 193–213.CrossRefGoogle Scholar
Taira, A., Hill, I. and Firth, J. et al. 1991. Site 808 Summary. Proc Ocean Drill Prog Sci Results 131 A, Ocean Drilling Program, College Station, TX. p 434.Google Scholar
Tazaki, K. and Fyfe, W.S.. 1987. Primitive clay precursors formed on feldspar. Ca J Earth Sci 24: 506–527.CrossRefGoogle Scholar
Tazaki, K., Fyfe, W.S. and Van der Gaast, S.J.. 1989. Growth of clay minerals in natural and synthetic glasses. Clays & Clay Miner 37: 348–354.CrossRefGoogle Scholar
Underwood, M., Pickering, K., Gieskes, J.M., Kastner, M. and Orr, R.. 1993. Sedimentary facies evolution of the Nanlkai forearc and its implications for the growth of the Shimanto accretionary prism. In: Hill, I., Taira, A., Firth, J.V., editors. Proc Ocean Drill Prog, Sci Results 131B. Ocean Drilling Program, College Station, TX. p 343–363.Google Scholar
Weaver, C.E.. 1958. The effects and geologic significance of potassium “fixation” by expandable clay minerals derived from muscovite, biotite, chlorite and volcanic materials. Am Mineral 43: 839–861.Google Scholar
Whitney, G.. 1990. Role of water in the smectite-to-illite reaction. Clays & Clay Miner 38: 343–350.CrossRefGoogle Scholar
Whitney, G. and Northrop, H.R.. 1988. Experimental investigation of the smectite to illite reactions: Dual reaction mechanisms and oxygen-isotope systematics. Am Mineral 73: 77–90.Google Scholar
Yau, Y.-C., Peacor, D.R. and Essene, E.J.. 1987. Smectite-illite reactions in Salton Sea shales. J Sed Petrol 57: 335–342.Google Scholar