K Transfer during Burial Diagenesis in the Mahakam Delta Basin (Kalimantan, Indonesia)

Furlan, S.; Clauer, Norbert; Chaudhuri, S.; Sommer, Frédéric

doi:10.1346/ccmn.1996.0440201

Cited by 33 publications

(6 citation statements)

References 31 publications

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“…This suggests that K may be considered highly mobile in fine-grained illitization systems at the basinal scale (e.g., Furlan et al, 1996) --more so than Al, which is redistributed through isomorphic substitution and limited to exchange between primary and secondary mineral phases. Given these relationships, if source composition is known or can be inferred, a predicted "pre-metamorphic" weathering trend can be calculated.…”

Section: Paleo-weathering Indices and K-metasomatismmentioning

confidence: 99%

Clay mineralogy, organic carbon burial, and redox evolution in Proterozoic oceans

Tosca

Johnston

Mushegian

et al. 2010

Geochimica et Cosmochimica Acta

100

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Section: Paleo-weathering Indices and K-metasomatismmentioning

confidence: 99%

Clay mineralogy, organic carbon burial, and redox evolution in Proterozoic oceans

Tosca

Johnston

Mushegian

et al. 2010

Geochimica et Cosmochimica Acta

100

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“…1976), an increasing number of studies suggest that the illitization of smectite in mudrocks may occur in an open system in which an external source of K + , such as interbedded sandstones, is required (e.g. Furlan et al . 1996; Land et al .…”

Section: Spatial and Temporal Distribution Of Mesogenetic Alterationsmentioning

confidence: 99%

Spatial and temporal distribution of diagenetic alterations in siliciclastic rocks: implications for mass transfer in sedimentary basins

2000

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Summary The spatial and temporal distribution of diagenetic alterations in siliciclastic sequences is controlled by a complex array of interrelated parameters that prevail during eodiagenesis, mesodiagenesis and telodiagenesis. The spatial distribution of near‐surface eogenetic alteration is controlled by depositional facies, climate, detrital composition and relative changes in sea‐level. The most important eogenetic alterations in continental sediments include silicate dissolution and the formation of kaolinite, smectite, calcrete and dolocrete. In marine and transitional sediments, eogenetic alterations include the precipitation of carbonate, opal, microquartz, Fe‐silicates (glaucony, berthierine and nontronite), sulphides and zeolite. The eogenetic evolution of marine and transitional sediments can probably be developed within a predictable sequence stratigraphic context. Mesodiagenesis is strongly influenced by the induced eogenetic alterations, as well as by temperature, pressure and the composition of basinal brines. The residence time of sedimentary sequences under certain burial conditions is of key importance in determining the timing, extent and patterns of diagenetic modifications induced. The most important mesogenetic alterations include feldspar albitization, illitization and chloritization of smectite and kaolinite, dickitization of kaolinite, chemical compaction as well as quartz and carbonate cementation. Various aspects of deep‐burial mesodiagenesis are still poorly understood, such as: (i) whether reactions are accomplished by active fluid flow or by diffusion; (ii) the pattern and extent of mass transfer between mudrocks and sandstones; (iii) the role of hydrocarbon emplacement on sandstone diagenesis; and (iv) the importance and origin of fluids involved in the formation of secondary inter‐ and intragranular porosity during mesodiagenesis. Uplift and incursion of meteoric waters induce telogenetic alterations that include kaolinitization and carbonate‐cement dissolution down to depths of tens to a few hundred metres below the surface.

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“…In this case, the K + /H + activity ratio continues to increase and a chemical gradient exists from fault to more distant zones, where illitic minerals precipitate from kaolin precursors. Similarly, Furlan et al (1996) describe a more intense kaolin illitization further away from underlying shale formation in the Mahakam Delta Basin (Indonesia). Feldspar dissolution, and subsequent kaolin precipitation, prevails in the deeper part, closer to the source rock.…”

Section: Possible Reaction Pathways For Kaolin Illitizationmentioning

confidence: 99%

Authigenic kaolin and illitic minerals during burial diagenesis of sandstones: a review

et al. 2002

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AB ST R ACT : The diagenetic evolution of kaolin and illitic minerals in sandstones is described here. The structural characterization of these minerals, the possible reaction pathways leading to their crystallization, and the origin of the fluids involved are discussed specifically.While early precipitation of kaolinite is in general related to flushing by meteoric waters, subsequent diagenetic kaolinite-to-dickite transformation probably results from invasion by acidic fluids of organic origin. Dickite is the stable polytype in most sandstone formations and the kaoliniteto-dickite conversion is kinetically controlled.The conventional model of kaolin illitization, assuming a thermodynamic control in a closed system, is discussed and compared to an alternative model in which illitization of kaolin is not coupled to dissolution of K-feldspar (Berger et al., 1997). In the latter model, illite crystallization at the expense of kaolin implies that an energy barrier is overcome either by an increased K + /H + activity ratio in solution or by a considerable temperature increase.

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K Transfer during Burial Diagenesis in the Mahakam Delta Basin (Kalimantan, Indonesia)

Cited by 33 publications

References 31 publications

Clay mineralogy, organic carbon burial, and redox evolution in Proterozoic oceans

Clay mineralogy, organic carbon burial, and redox evolution in Proterozoic oceans

Spatial and temporal distribution of diagenetic alterations in siliciclastic rocks: implications for mass transfer in sedimentary basins

Authigenic kaolin and illitic minerals during burial diagenesis of sandstones: a review

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