JURASSIC LAKE EVOLUTION MODEL INFERRED FROM THE COE LIMESTONE, LOWER SHUTTLE MEADOW FORMATION, HARTFORD BASIN, CONNECTICUT
Siliceous organisms within bedded dolomite rhombs and void-lining chalcedony comprise some of the early textures supporting a biogenic source for silica. Silica precipitation ceases as pH and water temperature rise as vents discharges. Briny hydrothermal waters rich in Mg+2 and Fe+2 ions favor dolomite deposition. Degassing at elevated temperatures would cause higher concentrations of interstitial salt ions and raise the Eh, further oxygenating the stagnant lake bottom waters (Renaut & Owen, 1988).
Sweeping baroque dolomite and iron oxide staining suggest that the precipitation occurred proximal to the vent at elevated temperatures ~60˚C to ~120˚C. Deposition either transitioned away from the vent or waned with cooling and with mixing of meteoric water causing a return to neutral conditions. The drop in pH is evident by precipitation of silica in fractures and in moldic porosity, by the formation of dedolomites and by the spar filling of voids. Further shallowing and tectonic uplift are inferred from spar-filled voids, dedolomites, authogenic evaporites, brecciation, hydrocarbon flushing, and late stage dissolution.