Mudrock

Coleman ML, Eggenkamp HGM, Aranyossy JF (2001) Chlorine stable isotope characterization of solute transport in mudrocks, ANDRA. Actes des Jounces Scientifiques EDP Sciences, France, p 155-175 Curie I (1921) Sur le poids atomique du chloe dans quelques mineraux. CR Acad Sci (Paris) 172 1025-1028 Deruelle B, Dreibus G, Jambon A (1992) Iodine abundances in oceanic basalts implications for Earth dynamics. Earth Planet Sci Lett 108 217-227... 

Raiswell R, Fisher QJ (2000) Mudrock-hosted carbonate concretions a review of growth mechanisms and their influence on chemical and isotopic composition. J Geol Soc 157 239-251 Roden EE, Lovley DR (1993) Dissimilatory Fe (111) reduction by the marine microorganism Desulfuromonas acetoxidans. App Environ Microbio 59 734-742... 

Variation of Cs adsorption with depth, as a function of changes in clay content, is reported by Melkior et al. (2005) the study aimed to test the efficiency of a host rock for radionuclide confmement. Mudrock samples were collected from Callovo-Oxfordian layers in Bure (France), at depths between 22m and 78m. The total clay content increases with depth by a factor of two to three between the measured depths. Figure 8.37 depicts the of Cs as a function of its concentration in solution at equilibrium. 

Fig. 8.37 Cesium sorption on Bure mudrock samples as a function of concentration in solution at equilibrium, at four different depths (Melkior et al. 2005)...

Sedimentary rocks within the lower (mainly felsic) part of the volcanic pile are highly variable and not voluminous. Greenish grey to dark grey mudrocks and volcaniclastic rocks occur locally in the FLB, MB, NF, SL and SR formations (Fig. 

Sedimentary rocks in the upper (mainly mafic) part of the pile are predominantly mudrocks, but they have an exhalative component. Maroon shale and chert are present in the BB, LR, and SK formations (Fig. 1). Notably, maroon shale and chert are abundant in the CLL Formation and also occur locally near the top of the FLB and SR formations. Caradocian black shale and pelagic chert of the BB, LR, and SK formations mark the end of volcanic activity in the BMC. In places, these rocks grade upward into flysch of the M or T formations (Fig. 1). 

Potter, P. E. 2003. Mudrocks. In Middleton, G. V. (ed) Encyclopedia of Sediments and Sedimentary Rocks. Kluwer Academic Publishers, Dordrecht, 451-459. 

Harrington, J.F. and Horseman, S.T. (1999) Gas transport properties of clays and mudrocks. In Geological Society, Special Publications, London, pp. 107-124... 

C, weathered shale, mudrock, sorption isotherm-headspace method, Grathwohl 1990)... 

Entwisle, D. C., and Reeder, S. (1993). New apparatus for pore fluid extraction from mudrocks for geochemical analysis. In Geochemistry of Clay-Pore Fluid Interaction (D. A. C. Manning, P. L. Hall, and C. R. Hughes, eds.), pp. 365—388. Chapman Hall, London. 

Dorsch, J. et al., Effective Porosity and Pore-Throat Size of Conasauga Group Mudrock Application, Test and Evaluation of Petrophysical Techniques, Oak Ridge National Laboratory, Oak Ridge, TN, ORNL/GWPO-021, 1996. 

Precise Re-Os ages of organic-rich mudrocks and the Os isotope composition of Jurassic seawater. Earth Planet. Sci. Lett. 167, 159-173. 

Pickard A. L. (2002) SHRIMP U-Pb zircon ages of tuffaceous mudrocks in the Brockman Iron Formation on the Hamersley Range, Western Australia. Austral. J. Earth Sci. 49, 491-507. 

Wignall P. B. and Myers K. J. (1988) Interpreting benthic oxygen levels in mudrocks a new approach. Geology 16, 452-455. 

Wignall P. B. and Newton R. (1998) Pyrite framboid diameter as a measure of oxygen deficiency in ancient mudrocks. Am. J. Sci. 298, 537-552. 

Between Ca 50 °C and 300 °C, sandstones and mudrocks ( shales ) undergo massive chemical and textural reorganization. In this temperature interval detrital grains, and the rock textures defined by grains, are lost by reactions with pore fluids. Chemical and physical processes in late diagenesis transform sUiciclastic sediments into rocks. Predictive models of porosity evolution with depth depend upon an understanding of these processes. Because the magnitude of... 

The concept of IGV in muddy sediments is less well established because it is difficult to petro-graphically discriminate between grains, cements, and porosity. As a result, compaction within mudrocks is described primarily on the basis of porosity decline curves (Giles et al, 1998). The porosity of muddy sediments is very high at deposition (near 80%) it declines exponentially with depth (summarized in Giles et al., 1998) in response to temperature, burial rate, and the degree of overpressuring (Bjprlykke, 1999). 

Two difficulties beset the notion of a mudrock source for calcite cement in sandstones. First, the lack of a strong depth trend for calcite cement in sandstones is difficult to reconcile with the prominent depth-related trend for carbonate loss in mudrocks. Second, there is a tremendous volume imbalance between the large amounts of CaCOa that appear to be missing from shales compared to the observed amount of calcite cement in sandstone (Land and Macpherson, 1992b). Unfortunately, quantitative data for depth trends of calcite in associated shales and sandstones outside the Gulf of Mexico are few. 

Awwiller D. N. (1993) Illite/smectite formation and potassium transfer during burial diagenesis of mudrocks a study from the Texas Gulf Coast Paleocene-Eocene. J. Sedim. Petrol. 63, 501-512. 

Awwiller D. N. (1994) Geochronology and mass transfer in Gulf Coast mudrocks (south-central Texas, USA) Rb-Sr, Sm-Nd, and REE systematics. Chem. Geol. 116, 61-84. 

Blatt H. and Schultz D. J. (1976) Size distribution of quartz in mudrocks. Sedimentology 23, 857—866. 

Blatt H. and Totten M. W. (1981) Detrital quartz as an indicator of distance from shore in marine mudrocks. J. Sedim. Petrol. 51, 1259-1266. 

Land L. S. and Milliken K. L. (2000) Regional loss of Si02 and CaCOs and gain of K2O during burial diagenesis of Gulf Coast mudrocks, USA. In Quartz Cementation in Sandstones (eds. R. H. Worden and S. Morad). International Association of Sedimentologists, Oxford, vol. 29, pp. 183-198. 

Lee J. I. and Lee Y. I. (1998) Feldspar albitization in Cretaceous non-marine mudrocks, Gyeongsang Basin, Korea. Sedimentology 45, 745-754. 

Milliken K. L. (1992) Chemical behavior of detrital feldspars in mudrocks versus sandstones, Frio Formation (Oligocene), South Texas. J. Sedim. Petrol. 62, 790-801. 

Milliken K. L. (1995) Petrographic evidence of open-system chemical reactions in mudrocks in the Gulf of Mexico sedimentary basin. Geological Society of American Annual Meeting 27(6), p. 461. 

Milliken K. L. and Land L. S. (1993) The origin and fate of siltsized carbonate in subsurface Miocene-Oligocene mudrocks. South Texas Gulf Coast. Sedimentology 40, 107-124. 

Milodowski A. E. and Zalasiewicz J. A. (1991) Redistribution of REE during diagenesis of turbidite/hemipelagite mudrock sequences of Llandovery age from central Wales. Geol. Soc. London Spec. Publ. 57, 101-124. 

Fine clastic sediments, mostly mudrocks, in contrast to their coarser counterparts, are either derived by first cycle weathering of silicate minerals or glass, or from recycling of older mudrocks. Physical comminution plays only a secondary role. The average shale is composed of 40-60% clay minerals, 20-30% quartz, 5-10% feldspar and minor iron oxide, carbonate, organic matter, and other components (Yaalon, 1962 Shaw and Weaver, 1965). Granitic source rocks produce shales richer in kaolinite and illite, the... 

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