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Bacterial mineralization patterns in basaltic aquifers: Implications for possible life in martian meteorite ALH84001: Comment
Alternative origins for nannobacteria-like objects in calcite
The possible role of nannobacteria (dwarf bacteria) in clay-mineral diagenesis and the importance of careful sample preparation in high-magnification SEM study
Formation of aragonite cement by nannobacteria in the Great Salt Lake, Utah
Abstract Early precipitation of siderite cement in Sonora Canyon sandstones (Wolfcampian) in the Val Verde Basin, southwest Texas strongly influenced later diagenesis and reservoir quality in these low-permeability gas reservoirs. Sandstones of the Sonora Canyon interval were deposited in water depths of 100 to 500 m in coalesced submarine fans basinward (southwest) of the northwest-trending shelf margin. Sonora Canyon sandstones are composed of hundreds of feet of fanlobe turbidites and local channel-fill facies deposited on the continental slope and basin floor. Sonora Canyon sandstones are fine-grained sublitharenites and litharenites (average composition Q 77 F 9 R 19 ). Grain-rimming siderite rhombs 1 to 2 μm long were the earliest major cement to precipitate, in volumes ranging from 0 to 38%. Siderite is concentrateti in bedding-parallel layers 8 to 10 cm thick or in irregular patches 3 to 8 cm in diameter. Isotopic composition of the siderite falls in a narrow range, 5 I3 C averaging 2.4‰ (PDB) and 5 15 O averaging 31.1 ‰ (SMOW). The isotopic data indicate that siderite cement formed in a methanogenic geochemical environment at a burial depth of about 300 to 600 m (27°C) from sea-water-derived pore fluids (δ 18 O = 0‰). Bacterial reduction of iron accompanying anaerobic bacterial methanogenesis increased the Fe +2 in the pore fluids and, in the absence of sulfide, siderite precipitated. Subspherical nan-nobacterial bodies (0.05 to 0.15 μm) are revealed by etching siderite in warm HCl. These bodies are locally abundant, ranging to 100 per μm 2 of siderite crystal surface; other parts of the crystals contain virmally no bodies. The bacteria presumably helped trigger siderite precipitation. Abundant early siderite inhibited later porosity loss by compaclion and quartz cementation; siderite-rich sandstones (containing a 10% siderite) average 33% minuscement porosity and 6% quartz cement. Siderite-poor sandstones (<10%), are extensively cemented by quartz (average = 11%) and are much more compacted (16% minus-cement porosity). Siderite-rich sandstones retain higher porosity (7.9%) and permeability (0.042 md) than do siderite-poor sandstones (average porosity = 6.4%, geometric mean permeability = 0.006 md). Best matrix reservoir quality in Sonora Canyon sandstones occurs in siderite-cemented zones.
SEM imaging of bacteria and nannobacteria in carbonate sediments and rocks
Meteoric Modification Of Early Dolomite And Late Dolomitization By Basinal Fluids, Upper Arbuckle Group, Slick Hills, Southwestern Oklahoma
Abstract The lower Datil Group (40–37 Ma) records the early phase of intermediate-composition volcanism in the northern Mogollon-Datil field of New Mexico. Eruptive products consist almost entirely of high-K andesite and dacite that range in SiO 2 content from about 58 to 67 weight percent. Lower Datil conglomerate clasts and correlative(?) lavas are characterized by phenocrystic plagioclase (An 20–60 ), amphibole, and titanomagnetite (±biotite, pyroxene) within a groundmass containing alkali feldspar, silica minerals, and plagioclase. Volcaniclastic rocks of the lower Datil Group were deposited by a spectrum of fluvial, debris-flow and lacustrine processes in two semi-arid intermontane basins and differ mineralogically from their volcanic progenitors in the following ways: 1) nonwelded ash is not represented in conglomerate; 2) phenocryst phases are preferentially concentrated in sandstone; 3) groundmass constituents and devitrification products are over-represented in mudstone and detrital matrix in sandstone; 4) opaque reaction rims on free amphibole and biotite grains are poorly developed or not present; 5) amphibole abundance is slightly diminished relative to plagioclase and biotite in sandstone; and 6) potassic riras on plagioclase grains may have been removed by abrasion. Mineralogic fractionation of lower Datil Group volcaniclastic sediments occurred primarily by impact shattering and abrasion during transportation. As a result, provenance determinations for volcaniclastic rocks may be influenced by grain-size effects.
Comment and Reply on “Sedimentary fabrics in Alpine ophicalcites, South Pennine Arosa zone, Switzerland”: COMMENT
Diagenesis and Dolomitization in Triassic (Rhaetian) “Portoro” Limestone, Portovenere, Liguria, Italy: ABSTRACT
Bizarre Forms of Depositional and Diagenetic Calcite in Hot-Spring Travertines, Central Italy
Abstract Travertines of central Italy have been deposited from warm, fresh-water springs very rich in H,S. Probably as a result of this, the carbonate sediments are largely constructed by bacteria instead of algae. Even the chemically-precipitated forms of calcite show a variety of bizarre characteristics, some of them probably due to the interaction of S with the calcite crystal lattice. Among these are thick crusts of radial fibrous calcite crystals up to a meter long, that show probable daily lamination due to the diurnal activity of photosynthetic bacteria and have depositional rates of as much as one meter per year. Fine ray-crystal fans only one mm or so thick are made of helically-twisting radial ribbons of calcite and also show daily growth bands. Bacterial clumps are enclosed within an elliptical ball of calcite, and the bacteria plate out upon crystal planes; the ball is then surrounded by a tattered hollow carapace of very thin-walled calcite forming a single crystal outline. Fibrous nests of square-ended calcite rods with inclined extinction (“lublinite”) occur among the bacterial calcite clumps. Pore-filling calcite cement in the rocks is also weird, sometimes showing forms like superimposed, curving gothic arches, or multiple spikes. Some calcite crystals also show features resembling screw-dislocations. Palisade calcite cement shows a nearly basal parting.
Travertines; depositional morphology and the bacterially constructed constituents
Complex polyhedral crystals of limpid dolomite associated with halite, Permian upper Clear Fork and Glorieta formations, Texas
New scents on the chattermark trail; weathering enhances obscure microfractures
The Natural History of Crystalline Calcium Carbonate: Effect of Magnesium Content and Salinity 1
Abstract Morphology of calcium carbonate crystals is controlled mainly by rate of crystallization, and Mg and Na content of the precipitating waters. Together, these factors integrate to provide important indicators of environment. Magnesium selectively poisons sideward growth of calcite; thus CaCO 3 prefers to crystallize as aragonite, or as minute fibers or steep rhombs of magnesian-calcite, whose sidewise growth is generally stopped at widths of a few microns. Thus in Mg-rich environments, such as beaches or marine bottoms, micritic or fibrous aragonite and magnesian calcite cements form. As seawater is buried, Na usually remains high but Mg is selectively lost so that the Mg/Ca ratio drops from 3:1 to about 1:3. Thus, in the absence of Mg-poisoning, coarse sparry calcite cement can form in the subsurface, and crystallizes as irregular polyhedra. In meteoric waters, both Mg and Na are very low. If precipitation is very rapid, calcite micrite may form (caliche). Fresh-water calcite can also occur as euhedral rhombs in very dilute solutions. In the phreatic-meteoric zone, sparry calcite develops. Carbonate ooze initially contains much Mg. Upon lithification, it is proposed that much of the Mg is retained as a sort of “cage” around each polyhedron of calcite, preventing growth beyond a few microns. Fresh-water flushing removes this Mg-cage, and allows recrystallization to coarser microspar.