Dolomitization and silicification in low-energy lacustrine carbonates (Paleogene, Madrid Basin, Spain)

Bustillo, Ma Ángeles; Arribas, M.E.

doi:10.1016/s0037-0738(01)00234-2

Cited by 68 publications

(45 citation statements)

References 45 publications

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“…Silicification, dolomitisation, dissolution, cementation, shrinkage cracks Armenteros et al (1995), Calvo et al (1995Calvo et al ( , 1999, Bustillo et al (2002), Alonso-Zarza (2003), Bustillo and Alonso-Zarza (2007), Bustillo (2010) Cementation, neomorphism (? ), dissolution Lopez et al (2017), Westaway (1993), Pentecost et al (1997), Kele et al (2011), De Filippis et al (2012, Özkul et al (2013), Van Noten et al (2013), Lebatard et al (2014), Claes et al (2015Claes et al ( , 2017aClaes et al ( , 2017b Sorey and Colvard (1997), Fouke et al (2000Fouke et al ( , 2003, Kharaka et al (2000), Chafetz and Guidry (2003), Kandianis et al (2008), Veysey et al (2008) Cipriani et al (1977), Barazzuoli et al (1988), Guo and Riding (1992, Pentecost (1995), Minissale et al (2002), Brogi et al (2007), Brogi and Capezzuoli (2008), Pedley (2009), Gandin and Capezzuoli (2014) Arp et al (2001Arp et al ( , 2010, Shiraishi et al (2008aShiraishi et al ( , 2008b, Brinkmann et al (2015) (continued on next page) et al, 2012; …”

Section: Tablementioning

confidence: 99%

“…Such conditions are found where, for example, pCO 2 varies, like in cave atmospheres (Woo et al, 2008), or where waters of different composition and saturation state mix (saline/alkaline, meteoric waters), or where ascending, Si-bearing thermal waters cool down (Bustillo, 2010). The dissolved silica can be sourced from associated or extra-formational clays, volcanic or metamorphic rocks, or even siliceous microorganisms like diatoms within the deposits (Bustillo et al, 2002;Burne et al, 2014). Silica often first forms as metastable opal A, transforming to opal CT and then quartz, or may form directly as stable quartz (Armenteros et al, 1995;Bustillo et al, 2002).…”

Section: Replacementmentioning

confidence: 99%

“…The dissolved silica can be sourced from associated or extra-formational clays, volcanic or metamorphic rocks, or even siliceous microorganisms like diatoms within the deposits (Bustillo et al, 2002;Burne et al, 2014). Silica often first forms as metastable opal A, transforming to opal CT and then quartz, or may form directly as stable quartz (Armenteros et al, 1995;Bustillo et al, 2002). Early, pseudomorphic silicification may protect primary features from later, burial-or subaerial exposure-related alteration and dissolution.…”

Section: Replacementmentioning

confidence: 99%

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What do we really know about early diagenesis of non-marine carbonates?

Boever

Brasier

Foubert

et al. 2017

Sedimentary Geology

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Non-marine carbonate rocks including cave, spring, stream, calcrete and lacustrine-palustrine sediments, are susceptible to early diagenetic processes. These can profoundly alter the carbonate fabric and affect paleoclimatic proxies. This review integrates recent insights into diagenesis of non-marine carbonates and in particular the variety of early diagenetic processes, and presents a conceptual framework to address them. With ability to study at smaller and smaller scales, down to nanometers, one can now observe diagenesis taking place the moment initial precipitates have formed, and continuing thereafter. Diagenesis may affect whole rocks, but it typically starts in nano-and micro-environments. The potential for diagenetic alteration depends on the reactivity of the initial precipitate, commonly being metastable phases like vaterite, Ca-oxalates, hydrous Mg-carbonates and aragonite with regard to the ambient fluid. Furthermore, organic compounds commonly play a crucial role in hosting these early transformations. Processes like neomorphism (inversion and recrystallization), cementation and replacement generally result in an overall coarsening of the fabric and homogenization of the wide range of complex, primary microtextures. If early diagenetic modifications are completed in a short time span compared to the (annual to millennial) time scale of interest, then recorded paleoenvironmental signals and trends could still acceptably reflect original, depositional conditions. However, even compact, non-marine carbonate deposits may behave locally and temporarily as open systems to crystal-fluid exchange and overprinting of one or more geochemical proxies is not unexpected. Looking to the future, relatively few studies have examined the behaviour of promising geochemical records, such as clumped isotope thermometry and (non-conventional) stable isotopes, in well-constrained diagenetic settings. Ongoing and future in-vitro and in-situ experimental approaches will help to investigate and detangle sequences of intermediate, diagenetic products, processes and controls, and to quantify rates of early diagenesis, bridging a gap between nanoscale, molecular lab studies and the fossil field rock record of non-marine carbonates.

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Section: Tablementioning

confidence: 99%

Section: Replacementmentioning

confidence: 99%

Section: Replacementmentioning

confidence: 99%

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What do we really know about early diagenesis of non-marine carbonates?

Boever

Brasier

Foubert

et al. 2017

Sedimentary Geology

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“…They consist of euhedral to anhedral crystals from a submicron size to 7 mm and are normally nonstoichiometric and poorly ordered (Last et al 2012). Although the formation of fine dolomites in both modern and ancient lake records has been widely studied (Wright 1999;Bustillo et al 2002;Casado et al 2014;Lu et al 2015), in many studies of lacustrine dolomites, there is insufficient evidence to determine whether the fine dolomite is of a primary or secondary (replacement) origin.…”

Section: Introductionmentioning

confidence: 99%

Formation of fine crystalline dolomites in lacustrine carbonates of the Eocene Sikou Depression, Bohai Bay Basin, East China

et al. 2016

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The genesis of the fine crystalline dolomites that exhibit good to excellent reservoir properties in the upper fourth member of the Eocene Shahejie Formation (Es 4 s ) around the Sikou Sag, Bohai Bay Basin, is uncertain. This paper investigates the formation mechanisms of this fine crystalline dolomite using XRD, SEM, thin section analysis and geochemical data. The stratigraphy of the Sikou lacustrine carbonate is dominated by the repetition of metre-scale, high-frequency deposition cycles, and the amount of dolomite within a cycle increases upward from the cycle bottom. These dolomite crystals are 2-30 lm in length, subhedral to anhedral in shape and typically replace both grains and matrix. They also occur as rim cement and have thin lamellae within ooid cortices. Textural relations indicate that the dolomite predates equant sparry calcite cement and coarse calcite cement. The Sr concentrations of dolomites range from 900 to 1200 ppm. Dolomite

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“…The silica may be sourced from rivers, mid-ocean ridge volcanic products that reacted with sea water, and silica particles on the sea oor [2]. The enrichment of silica is also related to diagenetic e ects and replacement of older minerals [2,3,[7][8][9][10][11]. Chert formation-cherti cation during diagenesis a ects the porosity, strength and density of the rocks, and these in turn control reservoir characteristics [3,8,12].…”

Section: Introductionmentioning

confidence: 99%

Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SWTurkey)

Gül

2015

Open Geosciences

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Abstract:The Lycian Nappes, containing ophiolite and sedimentary rocks sequences, crop out in the southwest Turkey. The Tavas Nappe is a part of the Lycian Nappes. It includes the Lower Jurassic-Upper Cretaceous calciturbidites. Chert occurrences were observed in the lower part of this calciturbidite. These cherts can be classi ed on the basis of length, internal structure and host rock. Chert bands are 3.20-35.0 m in length and 7.0-35.0 cm thick. Chert lenses are 5.0-175.0 cm in length and 1.0-33.0 cm thick. According to its internal structure, granular chert (bladedlarge equitant quartz minerals replaced the big calcite mineral of fossil shell) and porcelanious chert (microcrystalline silica replaced micrite) have been separated. Cherts are generally associated with calcarenite-calcirudite, the others with calcilutite. Micritic calcite patches of cherts point out an uncompleted silici cation. The source of silica was dominantly quartz-rich, older, basal rocks and to a lesser extent radiolarians. The coarse-grained calciturbidites act as a way for silica transportation. Some calcite veins (formed during transportation and emplacement of nappes) cut both calciturbidites and cherts. Thus, chert occurrences evolved before emplacement of nappes (the latest Cretaceous-Late Miocene period) during the epigenetic phase.

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Dolomitization and silicification in low-energy lacustrine carbonates (Paleogene, Madrid Basin, Spain)

Cited by 68 publications

References 45 publications

What do we really know about early diagenesis of non-marine carbonates?

What do we really know about early diagenesis of non-marine carbonates?

Formation of fine crystalline dolomites in lacustrine carbonates of the Eocene Sikou Depression, Bohai Bay Basin, East China

Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SWTurkey)

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