Geochemically controlled calcite precipitation by CO2 outgassing: Field measurements of precipitation rates in comparison to theoretical predictions

Dreybrodt, Wolfgang; Bühmann, Dieter; Michaelis, Jochen; Usdowski, E.

doi:10.1016/0009-2541(92)90082-g

Cited by 93 publications

(57 citation statements)

References 15 publications

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“…Since the thickness of the boundary layer decreases with flow rate, this provides a mechanism for a causal link between flow rate and precipitation rate (Buhmann & Dreybrodt 1985). This idea has been confirmed experimentally (Liu & Dreybrodt 1997;Dreybrodt et al 1997) and by comparison with field measurements (Dreybrodt et al 1992;Liu et al 1995). Wooding (1991) presents a particularly interesting analysis of the growth of individual travertine and ice terraces, using a similar conceptual model.…”

Section: Mechanisms For Precipitation Localizationmentioning

confidence: 78%

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Travertine terracing: patterns and mechanisms

Hammer

Dysthe

Jamtveit

2010

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Travertine terracing is one of the most eye-catching phenomena in limestone caves and around hydrothermal springs, but remains fairly poorly understood. The interactions between water chemistry, precipitation kinetics, topography, hydrodynamics, carbon dioxide degassing, biology, erosion and sedimentation constitute a complex, dynamic pattern formation process. The processes can be described and modeled at a range of abstraction levels. At the detailed level concerning the physical and chemical mechanisms responsible for precipitation localization at rims, a single explanation is probably insufficient. Instead, a multitude of effects are likely to contribute, of varying importance depending on scale, flux and other parameters.

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Section: Mechanisms For Precipitation Localizationmentioning

confidence: 78%

“…not hyperalkaline) conditions calcite precipitation depends on loss of CO 2 from aqueous solution to the atmosphere (e.g. Dreybrodt et al 1992). An extremely simplified, cartoon-like equation, summarizing many partial reactions that are variously important at different pH, can be written as…”

Section: Mechanisms For Precipitation Localizationmentioning

confidence: 99%

Travertine terracing: patterns and mechanisms

Hammer

Dysthe

Jamtveit

2010

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“…Early calculations (Dreybrodt, 1980(Dreybrodt, , 1981Buhmann & Dreybrodt, 1985) used the Nancollas-Reddy equation to model the data. Comparison of calculated rates using the Plummer-Wigley-Parkhurst equation with actual growth rates in a travertine-depositing stream produced good agreement (Dreybrodt et al, 1992). After many investigations, the rate equation for the growth of calcite speleothems, particularly Speleothem ontogeny stalagmites, is presented in the form (Dreybrodt, 1999):…”

Section: Calcite Growth Rates From Bulk Solution Measurementsmentioning

confidence: 94%

Speleothem microstructure/speleothem ontogeny: a review of Western contributions

White¹

2012

IJS

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Mineral ontogeny is the study of the growth and development of mineral deposits in general and, in the present context, speleothems in particular. Previous researchers, mainly in Russia, have developed a nomenclatural hierarchy based on the forms and habits of individual crystals and the assembly of individual crystals into both monomineralic and polymineralic aggegates (i.e. speleothems). Although investigations of the growth processes of speleothems are sparse, there is a large literature on growth processes of speleothem minerals and related crystals in the geochemical and materials science literature. The purpose of the present paper is to sort through the various concepts of crystal growth and attempt to relate these to observations on speleothems and to the Russian conceptual framework of mineral ontogeny. For calcite, the most common mineral in speleothems, the activation energy for two dimensional nucleation (required for the growth of large single crystals) is almost the same as the activation energy for threedimensional nucleation (which would result in the growth of many small crystals). Calcite growth is highly sensitive to minor impurities that may poison growth in certain crystallographic directions or may poison growth altogether. Extensive recent research using the atomic force microscope (AFM) provides many details of calcite growth including the transition from growth on screw dislocations to growth by two-dimensional nucleation. The deposition of aragonite speleothems requires metastable supersaturation curve and is usually ascribed to the impurities Mg 2+ and Sr 2+ . AFM studies reveal that Mg 2+ poisons calcite growth by blocking deposition sites on dislocations, thus allowing supersaturation to build up past the aragonite solubility curve. Sr 2+ precipitates as a Sr-rich nucleus with the aragonite structure which acts as a template for aragonite growth. The different morphology of gypsum speleothems can be explained by the different growth habit of gypsum. Examples of twinned growth, dendrite growth, and spherulitic growth are common in the crystal growth literature and can be used to interpret the corresponding cave forms. Interpretation of monomineralic aggregate growth follows from individual crystal mechanisms. Interpretation of polymineralic aggregate growth requires knowing the evolving chemistry which in turn requires new methods for the sampling and analysis of microliter or nanoliter quantities of fluid.

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“…The meteogene travertine is usually referred to as "tufa", especially that which contains remains of micro and macrophytes, invertebrates and bacteria [11,12]. It is usually derived from lower water temperature, and lower contents of dissolved inorganic carbon (Dissolved inorganic carbon (DIC) < 10 mmol·L −1 ), CO 2 partial pressure (pCO 2 < 0.1 atm) and higher pH values (7)(8) [10]. Meteogene usually displays low deposition rates (<10 mmol·cm −2 year −1 ) and shows a negative carbon isotopic composition (δ 13 C vs. PDB between −12 and 0‰).…”

Section: Introductionmentioning

confidence: 99%

“…The terms travertine and tufa are sometimes used synonymously [5]. Calcite precipitation occurs due to CO 2 -loss, and associated pH-reduction during fluid equilibration with the atmosphere [6,7]. Travertine precipitation seems to be controlled by a combination of several factors, such as: (i) a fast decrease of the hydrostatic pressure and the pCO 2 , resulting in a rapid degassing process; and (ii) microbes and algae activity [6].…”

Section: Introductionmentioning

confidence: 99%

Geochemistry and Stable Isotopes of Travertine from Jordan Valley and Dead Sea Areas

et al. 2017

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Travertine deposits in Deir Alla, Suwayma, and Az Zara areas were investigated. Mineralogy, geochemistry, stable isotopes and age dating indicate the presence of low-Mg calcite, with minor quartz components. The variable isotope (δ 13 C and δ 18 O) signatures indicate dependence on water temperature and water/rock isotopic exchange. In contrast, the high δ 13 C values in some travertine samples reflect 12 CO 2 degassing processes, increased input of 13 C-enriched groundwater, and the presence of surface and groundwater hydrological systems. The high δ 18 O values may be attributed to evaporation effects and low water temperature during the formation of localized travertine. The age of travertine is the Late Pleistocene.

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Geochemically controlled calcite precipitation by CO2 outgassing: Field measurements of precipitation rates in comparison to theoretical predictions

Cited by 93 publications

References 15 publications

Travertine terracing: patterns and mechanisms

Travertine terracing: patterns and mechanisms

Speleothem microstructure/speleothem ontogeny: a review of Western contributions

Geochemistry and Stable Isotopes of Travertine from Jordan Valley and Dead Sea Areas

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