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Formation of flint horizons in North Sea chalk through marine sedimentation of nano-quartz

Published online by Cambridge University Press:  09 July 2018

H. Lindgreen ,
V. A. Drits ,
A. L. Salyn ,
F. Jakobsen  and
N. Springer
H. Lindgreen*
Affiliation:
Geological Survey of Denmark and Greenland, Øster Voldgade 10, DK1350 Copenhagen K, Denmark
V. A. Drits
Affiliation:
Geological Institute, Russian Academy of Science, Pyzhevsky per D7, 119017 Moscow, Russia
A. L. Salyn
Affiliation:
Geological Institute, Russian Academy of Science, Pyzhevsky per D7, 119017 Moscow, Russia
F. Jakobsen
Affiliation:
Geological Survey of Denmark and Greenland, Øster Voldgade 10, DK1350 Copenhagen K, Denmark
N. Springer
Affiliation:
Geological Survey of Denmark and Greenland, Øster Voldgade 10, DK1350 Copenhagen K, Denmark
*
*E-mail: hl@geus.dk
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Abstract

In the Upper Cretaceous-Danian North Sea chalk, silica composed of nano-size quartz spheres is dispersed in the chalk matrix, and quartz is present in bands and nodules of flint. In the present investigation of the North Sea Danian chalk the nano-quartz in the chalk matrix is compared with the silica in the flint. Samples of chalk and flint layers from four North Sea wells have been investigated. Atomic Force Microscopy (AFM) has been applied to image the quartz in the chalk and in the flint. X-ray diffraction (XRD), including analysis of the positions and profiles of hkl reflections in powder diffraction patterns, has been applied to characterize the lattice of the quartz in both the chalk matrix and in the flint. The quartz in the chalk matrix and in the flint is composed of nano-quartz spheres having identical cell parameters. Based on the results we propose a new model for formation of flint in North Sea chalk: (1) The nano-quartz in the flint, like the nano-quartz in the chalk matrix, has crystallized in the marine Chalk Sea environment. The colloidal quartz particles flocculated and were deposited on the sea floor mixed with calcitic bioclastic material. (2) Regional variations in the concentration of nano-quartz particles in the sediment reflect different degrees of acidification of the Chalk Sea. (3) This resulted in areas where practically all the calcite bioclasts were dissolved leaving a high concentration of nano-quartz particles to form flint layers; where there was less dissolution, indurated chalk with abundant nano-quartz particles is now preserved. (4) The acidification could have been caused by the effects of enhanced atmospheric CO2 linked to massive short-lived volcanic eruptions in the British Tertiary Igneous Province.

Keywords

flint formationchalkmarine sedimentationNorth Seanano-quartzX-ray diffractionatomic force microscopy
Type
Research Article
Information
Clay Minerals , Volume 46 , Issue 4 , December 2011 , pp. 525 - 537
Copyright
Copyright © The Mineralogical Society of Great Britain and Ireland 2011

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References

Berner, R.A. & Beerling, D.J. (2007) Volcanic degassing necessary to produce a CaCO3 undersaturated ocean at the Triassic-Jurassic boundary. Palaeogeography, Palaeoclimatolology, Palaeoecology, 244, 368–373.Google Scholar
Bromley, R.G. & Ekdale, A.A. (1986) Flint and fabric in the European chalk. Pp. 71–82 in: The Scientific Study of Flint and Chert (Sieveking, G.D.G. & Hart, M.B., editors) Cambridge University Press.Google Scholar
Calvert, S.E. (1974) Deposition and diagenesis of silica in marine sediments. Special Publications of the International Association of Sedimentlogists, 1, 273–279.Google Scholar
Clayton, C.J. (1986) The chemical environment of flint formation in Upper Cretaceous chalk. Pp. 43–54 in: The Scientific Study of Flint and Chert (Sieveking, G.D.G. & Hart, M.B., editors) Cambridge University Press.Google Scholar
Feely, R.A., Sabine, C.L., Lee, K., Berelson, W., Kleypas, J., Fabry, V.J. & Millero, F.J. (2004) Impact of anthropogenic CO2 on the CaCO3 system in the oceans. Science, 305, 362–366.Google Scholar
Frondini, F., Chiodini, G., Caliro, S., Cardellini, C., Granieri, D. & Ventura, G. (2004) Diffuse CO2 degassing at Vesuvio, Italy. Bulletin of'Volcanology, 66, 642–651.Google Scholar
Hautmann, M., Benton, M. J. & Tomasovych, A. (2008) Catastrophic ocean acidification at the Triassic-Jurassic boundary. Neues Jahrbuch für Geologie und Palaontologie; Abhandlungen. 249, 119–127.Google Scholar
Holmes, A. (1965) Principles of Physical Geology. (Thomas Nelson and Sons Ltd, London), 2nd edition.Google Scholar
Jakobsen, F., Lindgreen, H., & Springer, N. (2000) Precipitation and flocculation of spherical nano silica in North Sea chalk. Clay Minerals, 35, 175–184.Google Scholar
Lindgreen, H., Jakobsen, F. & Springer, N. (2010) Nanosize quartz accumulation in reservoir chalk, Ekofisk Formation, South Arne Field, North Sea. Clay Minerals, 45, 171–182.Google Scholar
Mackenzie, F.T. & Gees, R. (1971) Quartz: Synthesis at earth-surface conditions. Science, 173, 533–535.Google Scholar
Madsen, H.B. & Stemmerik, L. (2010) Diagenesis of flint and porcellanite in the Maastrichtian chalk at Stevns Klint, Denmark. Journal of Sedimentary Research, 80, 578–588.Google Scholar
Micheelsen, H. (1966) The structure of dark flint from Stevns, Denmark. Meddelelser fra Dansk Geologisk Forening, 16, 286–368.Google Scholar
Millot, G. (1970) Geology of Clays. Springer Verlag, London.CrossRefGoogle Scholar
Moore, D.M. & Reynolds, R.C. (1997) X-ray Diffraction and the Identification and Analysis of Clay Minerals. Oxford University Press, Oxford, p.378.Google Scholar
Moray, G.W., Fournier, R.O. & Rowe, J.J. (1962) The solubility of quartz in water in the temperature interval from 25°C to 300°C. Geochimica et Cosmochimica Acta, 26, 1029–1043.Google Scholar
Ridgwell, A. & Schmidt, D.N. (2010) Past constraints on the vulnerability of marine calcifiers to massive carbon dioxide release. Nature Geoscience, 3, 196–200.Google Scholar
Riebesell, U., Zondervan, I., Rost, B., Tortell, P.D., Zeebe, R.E. & Morel, F.M.M. (2000) Reduced calcification of marine plankton in response to increase atmospheric CO2 . Nature, 407, 364–367.Google Scholar
Saunders, A.D., Fitton, J.G., Kerr, A.C., Norry, M.J. & Kent, R.W. (1997) The North Atlantic Igneous Province. Pp. 45–97 in Large Igneous Provinces (Mahoney, J.J. & Coffin, M.F., editors) Geophysical Monograph Series, 100.Google Scholar
Schuiling, R. D. (2004) Thermal effects of massive CO2 emissions associated with subduction volcanism. Comptes Rendus Geoscience, 336, 1053–1059.CrossRefGoogle Scholar
Self, S., Widdowson, M., Thordarson, T. & Jay, A.E. (2006) Volatile fluxes during flood basalt eruptions and potential effects on the global environment: A Deccan perspective. Earth and Planetary Science Letters, 248, 518–532.CrossRefGoogle Scholar
Warnock, J., Scherer, R. & Laubere, P. (2007) A quantitative assessment of diatom dissolution and Late Quaternary primary productivity in the Eastern Equatorial Pacific. Deep Sea Research, II, 54, 772–783.Google Scholar
Williams, L.A. & Crerar, D.A. (1985) Silica diagenesis, II. General mechanisms. Journal of Sedimentary Petrology, 55, 312–321.Google Scholar
Williams, L.A., Parks, G.A. & Crerar, D.A. (1985) Silica diagenesis, I. Solubility controls. Journal of Sedimentary Petrology, 55, 301–311.Google Scholar
Zijlstra, H.J.P. (1987) Early diagenetic silica precipitation, in relation to redox boundaries and bacterial metabolism, in Late Cretaceous chalk of the Maastrichtian type locality. Geologie en Mijnbouw, 66, 343–355.Google Scholar
Zimmer, M. & Erzinger, J. (2003) Continuous H2O, CO2, 222Rn and temperature measurements on Merapi Volcano, Indonesia. Journal of Volcanology and Geothermermal Research, 125, 25–38.Google Scholar