Abstract:
The stable isotope and minor element geochemistry of Neocomian (Lower Cretaceous) pelagic carbonates of the North Atlantic Basin (Deep Sea Drilling Project Sites 105, 367, 387, 391, and 603) was examined to develop a diagenetic model for pelagic limestones. In particular, we hoped to test the fidelity of whole-rock geochemical records as paleoceanographic indicators for pelagic deposits of pre-Aptian age, in which individual microfossils are not available for analysis. Data indicate that in addition to depth of burial, rhythmic variations in primary carbonate content have strongly controlled diagenetic patterns and associated geochemical signatures in these Neocomian sequences. Samples become increasingly depleted in Sr and delta (super 18) O with increasing CaCO (sub 3) content. Within individual sedimentary sections, substantial decreases in Sr/Ca ratios and delta (super 18) O values are evident over a range of 4 to 98% CaCO (sub 3) . However, even over a relatively narrow range of 50 to 98% CaCO (sub 3) a 2.5 per mil variation in delta (super 18) O values and a change of a factor of 1.7 in Sr/Ca ratios are observed. Carbon isotope compositions do not vary as extensively with CaCO (sub 3) content, but carbonate-rich intervals tend to be relatively depleted in (super 13) C. Petrographic analysis reveals that these geochemical patterns are related to the transfer of CaCO (sub 3) from carbonate-poor intervals (calcareous shales and marlstones) to adjacent carbonate-rich intervals (limestones) during burial compaction and pressure solution. This process results in the addition of diagenetic cement to carbonate-rich intervals to produce a bulk composition that is relatively depleted in Sr and (super 18) O and, at the same time, enables the retention of more-or-less primary carbonate that is relatively enriched in Sr and (super 18) O in adjacent carbonate-poor intervals. Thus, although cyclic variations in CaCO (sub 3) content are primary in the Neocomian sequences examined, measured variations in Sr/Ca ratios and delta (super 18) O values are not and, as such, do not provide reliable proxies for past variations in climate, oceanographic conditions, or global ice volume.