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NARROW
GeoRef Subject
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all geography including DSDP/ODP Sites and Legs
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North America
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Michigan Basin (2)
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United States
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Michigan
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Michigan Lower Peninsula
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Montcalm County Michigan (1)
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Saint Clair County Michigan (1)
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commodities
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oil and gas fields (2)
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petroleum
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natural gas (1)
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geologic age
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Paleozoic
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Devonian
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Middle Devonian
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Dundee Limestone (1)
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Silurian
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Middle Silurian (1)
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Niagaran (1)
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Primary terms
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geophysical methods (1)
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North America
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Michigan Basin (2)
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oil and gas fields (2)
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Paleozoic
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Devonian
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Middle Devonian
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Dundee Limestone (1)
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Silurian
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Middle Silurian (1)
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Niagaran (1)
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petroleum
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natural gas (1)
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reefs (1)
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sedimentary rocks
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carbonate rocks
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boundstone (1)
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wackestone (1)
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clastic rocks
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conglomerate (1)
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sedimentary structures
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biogenic structures
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stromatolites (1)
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United States
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Michigan
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Michigan Lower Peninsula
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Montcalm County Michigan (1)
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Saint Clair County Michigan (1)
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sedimentary rocks
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sedimentary rocks
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carbonate rocks
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boundstone (1)
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wackestone (1)
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clastic rocks
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conglomerate (1)
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sedimentary structures
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sedimentary structures
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biogenic structures
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stromatolites (1)
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Well-log tomography and 3-D imaging of core and log-curve amplitudes in a Niagaran reef, Belle River Mills field, St. Clair County, Michigan, United States
Devonian Dundee Formation, Crystal Field, Michigan Basin: Recovery of Bypassed Oil Through Horizontal Drilling
Abstract The usefulness of geochemical modeling in diagenesis lies in the ability to analyze processes that cannot be measured directly in the laboratory, either due to the time element (slow kinetics) or, more typically, metastable equilibria. Important diagenetic process include: albitization (Morad and others, 1990), the illite/smectite transition (Perry and Hower, 1970; Bjørlykke and Aagaard, 1992), zeolitization, development of quartz overgrowths, carbonate cementation (Boles, 1979; Bjørlykke, 1983; Bjørlykke and others, 1989), the role of calcium-plagioclase and other unstable minerals in driving diagenetic reactions (Boles, 1991; Ram-seyer and others, 1992), and the effects of fluid composition on the final diagenetic state. Computer modeling of these processes has reached the stage that it can perform fairly realistic "what if” experiments in which the investigator has control of all pertinent variables and can examine the results from a number of perspectives. All of the reactions mentioned above can be occurring separately or simultaneously, and the models have now reached a state of sophistication that they will accurately keep a mass balance and insure that chemical equilibrium is maintained at all points along the reaction path. At present, there is no other way to dissect these complex and effect relationships other than by invoking the so-called “PATH” models or their variants. They are powerful tools, difficult to master and prone to abuse, but overall constitute a tool for the study of diagenesis that rivals X-rays diffraction analysis and petrographic analysis.
Abstract Diagenetic reactions are characterized by mineral dissolution and precipitation. Both can occur separately or simultaneously and can involve one or more minerals. The process, either dissolution or precipitation, can vary over many orders of magnitude, from sub-millimeter to kilometer scale. The dominant scale for diagenetic purposes, however, would seem to be from millimeters (mm) to meters (m), with the mm scale more common in fine grained rocks such as shales and siltstones, and the meter scale more common in sandstones. Megascale phenomena (kilometers) appear to be related to fluid movement along faults and fractures and are associated with tectonic events and thermal anomalies. There is also a slow, persistent, large-scale fluid movement associated with the dewatering of mudstones that begins on initial deposition and persists until effective porosity is lost (Bonham, 1980; Bjørlykke, 1983). The mechanics of this dewatering are reasonably well understood, at least relative to the chemical consequences, but it is still an area of active investigation, particularly as it may involve overpressure development in young, subsiding basins such as the Gulf Coast or the San Joaquin Basin of California. The importance of this dewatering flow is that it is pervasive, it involves huge volumes of rock, and if it becomes focused even slightly, it can concentrate large fluxes of fluid through limited volumes of rock.
Abstract Chapter 18, Data Analysis and Empirical Modeling, presented aspects of development of linear models using multivariate linear regression analysis. This methodology is highly practical and easily utilized by most geologists, but is clearly not the only one available for development of predictive models, nor does it necessarily always provide the most accurate models. Numerous alternate methodologies and emerging methodologies, both process- and effect-oriented, theoretical and empirical, have been and are being developed. This chapter will briefly touch on emerging and alternate methodologies for process- and effect-oriented modeling.
Advective diagenesis predicts that large-scale mineral migration will occur when saturated pore fluids move across isotherms (or isobars). A general picture of the change in a given porosity field can be calculated if the fluid flow and temperature (or pressure) fields are known. For more detailed analysis it is necessary to know the details of the chemical equilibria involved, their temperature and pressure dependence, the host rock mineralogy and, in particular, the thermal mass transfer coefficients for the phases involved. In this paper thermal mass transfer coefficients for quartz and calcite have been calculated in detail over the temperature range 0- 200°C. Simple approximations (involving only equilibrium constants) have been obtained for the concentrations of the aqueous species as well as for the solid mass precipitated or dissolved. Quartz solubility is prograde over the entire temperature range of interest, and the mass transfer coefficients for quartz range from 0.1 ppm/C° at 0°C to about 4 ppm/C° at 200°C. In a closed system calculation shows that calcite solubility is prograde up to 125°C, and then becomes retrograde, while in open systems calcite solubility is retrograde over this temperature range. The mass transfer coefficients for calcite range from +0.1 ppm/ °C in a closed system at 0°C to greater than −60 ppm/°C at 0°C under 62 atm of CO 2 pressure. At higher temperatures these coefficients seem to trend toward a common asymptotic value of 0(?) ppm/°C at temperatures greater than 200°C. These calculations suggest that low temperatures and high CO 2 pressures are most effective in mobilizing calcite but that high temperatures are more effective in mobilizing quartz. The calculations support recent suggestions that decarboxylation of organic matter is involved in the development of secondary porosity.
Abstract Diagenesis of volcanogenic sandstones is characterized by the alteration of glass and feldspar (plagioclase) to carbonates, clays and zeolites. These alteration products are commonly distributed throughout the body in well defined zones, but the chemical and physical controls on the spatial location of these zones is poorly understood. A quantitative model describing these processes has been constructed by combining the equations describing chemical reaction with those governing mass transfer. This approach leads to a set of differential equations with associated boundary conditions constrained by a set of mass action equations. In this framework the identity and spatial distribution of the reaction products can be shown to originate as a consequence of counter-current mass flows in which different aqueous species diffuse in opposite directions due to imposed boundary conditions. In the case of opposing diffusion currents containing components which are capable of reacting to form a solid precipitate, a well-defined precipitation zone will form. The positions of these zones are a function of the boundary conditions and the strength of the sources and sinks. The calculation emphasizes the importance of knowing whether or not the system was open or closed with respect to fluid flow and/or gas exchange and shows that the Peclet number is a key parameter as it not only affects the spatial distribution of the alteration products but also effects the magnitude of the precipitation flow.