Effects of groundwater flow on mineral diagenesis, with emphasis on carbonate aquifers

Machel, Hans G.

doi:10.1007/s100400050182

Cited by 68 publications

(36 citation statements)

References 41 publications

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“…This succession can be related to the following sequence of processes that characterizes the three diagenetic stages (eodiagenesis, mesodiagenesis and telodiagenesis) according to the criteria proposed by Choquette and Pray (1970), Schmidt and McDonald (1979a, b) and Worden and Burley (2003). The fi rst two stages (eodiagenesis and mesodiagenesis) refer to burial stages and are equivalent to those proposed by Machel (1999), as shallow burial, intermediate burial and deep burial.…”

Section: Secondary Porositymentioning

confidence: 99%

Diagenetic paths in the margin of a Triassic Basin: NW zone of the Iberian Chain, Spain

Ochoa

Arribas

2005

Int J Earth Sci (Geol Rundsch)

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Buntsandstein deposits generated in a slowly subsiding basin on the western margin of the Iberian Chain are represented by a stratigraphic succession of fluvial deposits less than 100 m thick (conglomerates, sandstones, and shales). Diagenetic processes in sand stones can be grouped as eodiagenetic, mesodiagenetic, and telodiagenetic. Eodiagenesis can be associated with Muschelkalk, Keuper, and probably early Juras sic times. Mesodiagenesis is probably related to Jurassic times. Diagenetic chemical reactions suggest a maximum burial less than 1.5 km and low tempera tures « 120°C). Patterns of porosity reduction by compaction and cementation suggest four diagenetic stages: (1) Loss of primary porosity by early mechanical compaction; (2) early cementation (K feldspar and dolomite); (3) dissolution of cements; and (4) framework collapse by re-compaction. These stages are manifested by the presence of two types of sand stone. Type I sandstones present high intergranular volume (mean, 30%). Type II sandstones are charac terized by high compactional porosity loss and exhibit low values of intergranular volume (mean, 16.9%). Type 11 sandstones are associated with the dissolution of cement and later re-compaction of type I sand stones. An intermediate telodiagenetic phase is de duced and related to the sharp unconformity between Lower Cretaceous sediments and the underlying sedi ments. This suggests that a mechanically unstable framework collapsed during the Cretaceous, generating type II sandstones. The analyzed diagenetic paths have a wide applicability on similar marginal areas of rift basins.

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Section: Secondary Porositymentioning

confidence: 99%

Diagenetic paths in the margin of a Triassic Basin: NW zone of the Iberian Chain, Spain

Ochoa

Arribas

2005

Int J Earth Sci (Geol Rundsch)

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“…lst = restricted to limestones; r = restricted to uncommon occurrences. Diagenetic settings and their relative depths are based on Machel (1999).…”

Section: Near-surface and Shallow-burial Diagenesismentioning

confidence: 99%

Pervasive dolomitization with subsequent hydrothermal alteration in the Clarke Lake gas field, Middle Devonian Slave Point Formation, British Columbia, Canada

Lonnee

Machel

2006

Bulletin

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Hans G. Machel is a professor at the Department of Earth and Atmospheric Sciences, University of Alberta. His research involves carbonate and evaporite facies and the diagenesis, lowtemperature geochemistry, and petroleum geology of Alberta, particularly dolomitization, cathodoluminescence, and diagenetic redox processes relevant to sour gas, sulfur, and Mississippi Valley -type sulfide deposits, and magnetic exploration for hydrocarbons.The Clarke Lake gas field in British Columbia, Canada, is hosted in pervasively dolomitized Middle Devonian carbonates of the Slave Point Formation. The Clarke Lake field consists mostly of pervasive matrix dolomite and some saddle dolomite, the latter varying in volume from about zero in limestones to normally 20 -40% (locally up to 80%) in dolostones over any given 10-m (33-ft) core interval. Some of the saddle dolomite is replacive, some is cement, and both varieties are associated with dissolution porosity and recrystallized matrix dolomite.The major objective of this study is to identify the causes and timing of matrix and saddle dolomite formation, specifically, whether these dolomites are hydrothermal. A comprehensive petrographic and geochemical examination indicates that pervasive matrix dolomitization was accomplished by long-distance migration of halite-saturated brines during the Late Devonian to Mississippian. Fluid-inclusion homogenization temperatures suggest about 150 (uncorrected) to 190jC (corrected) at the time of matrix dolomitization. These temperatures differ markedly from most published work on the dolomitized Devonian reefs in the Alberta Basin south of the Peace River arch, where pervasive matrix dolomitization was accomplished by advection of slightly modified seawater at temperatures of about 60-80jC, and where no hydrothermal influence was ever present. The saddle dolomites at Clarke Lake are not cogenetic with matrix dolomite and are not the product of hydrothermal dolomitization (sensu stricto). Instead, they formed through the hydrothermal alteration of matrix dolomite by way of

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“…Stylolites are typically thought to develop at burial depths of 500-1500 m (Lind 1993;Machel 1999;Mountjoy et al 1999). Based on the estimated thickness of Wolfcampian and Leonardian strata on the NW shelf (Meyer 1966;Frenzel et al 1988), CiscoCanyon strata in the Indian Basin Field probably did not reach burial depths exceeding 500 m until the Guadalupian.…”

Section: Onset Of Late Diagenesismentioning

confidence: 97%

Repeated injection of hydrothermal fluids into downdip carbonates: a diagenetic and stratigraphic mechanism for localization of reservoir porosity, Indian Basin Field, New Mexico, USA

Hiemstra

Goldstein

2014

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A detailed study of the Pennsylvanian Indian Basin Field of New Mexico, USA is used to develop a conceptual model that predicts reservoir porosity in clean down-depositional-dip marine carbonate, where repeated fracturing allows for hydrothermal fluid flow. Strata updip probably experienced repeated events of subaerial exposure, resulting in mineralogical stabilization and extensive calcite cementation that prevented extensive hydrothermal alteration. Clean, carbonate sediment deposited downdip was more prone to alteration by hydrothermal fluids. In the reservoir, cement stratigraphy shows regionally persistent zones closely associated with fracturing. Fluid inclusion data show high temperatures and repeated rises and falls, indicating tectonic valving in a hydrothermal system. Salinity data support this and indicate a late event of meteoric influx. Srand O-isotope data indicate higher temperature and less rock-water interaction in fault damage zones, evidence for intensified fluid flow in such areas. Formation of vugs and molds was associated with the hydrothermal fluid flow, which was driven by convection, probably initiated during 40-30 Ma intrusive activity and continuing after the onset of Basin and Range uplift and unroofing.

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Effects of groundwater flow on mineral diagenesis, with emphasis on carbonate aquifers

Cited by 68 publications

References 41 publications

Diagenetic paths in the margin of a Triassic Basin: NW zone of the Iberian Chain, Spain

Diagenetic paths in the margin of a Triassic Basin: NW zone of the Iberian Chain, Spain

Pervasive dolomitization with subsequent hydrothermal alteration in the Clarke Lake gas field, Middle Devonian Slave Point Formation, British Columbia, Canada

Repeated injection of hydrothermal fluids into downdip carbonates: a diagenetic and stratigraphic mechanism for localization of reservoir porosity, Indian Basin Field, New Mexico, USA

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