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In this contribution we explore constraints on the fractions of deep water present in the Indian and Pacific oceans which originated in the northern Atlantic and in the Southern Ocean. Based on PO4* we show that if ventilated Antarctic shelf waters characterize the Southern contribution, then the proportions could be close to 50-50. If instead a Southern Ocean bottom water value is used, the Southern contribution is increased to 75%. While this larger estimate may best characterize the volume of water entering the Indo-Pacific from the Southern Ocean, it contains a significant portion of entrained northern water. We also note that ventilation may be highly tracer dependent: for instance Southern Ocean waters may contribute only 35% of the deep radiocarbon budget, even if their volumetric contribution is 75%. In our estimation, the most promising approaches involve using CFC-11 to constrain the amount of deep water formed in the Southern Ocean. Finally, we highlight the broad utility of PO4* as a tracer of deep water masses, including descending plumes of Antarctic Bottom Water and large-scale patterns of deep ocean mixing, and as a tracer of the efficiency of the biological pump. [ABSTRACT FROM AUTHOR]

In this contribution we explore constraints on the fractions of deep water present in Indian and Pacific Oceans which originated in the northern Atlantic and in the Southern Ocean. Based on PO4* we show that if ventilated Antarctic shelf waters characterize the Southern contribution, then the proportions are close to 50-50. If instead a Southern Ocean bottom water value is used, the Southern contribution is increased to 75 %. While this larger estimate may characterize the volume of water entering the Indo-Pacific from the Southern Ocean, it contains a significant portion of entrained northern water. We also note that ventilation may be highly tracer dependent: for instance Southern Ocean waters may contribute only 35 % of the deep radiocarbon budget, even if their volumetric contribution is 75 %. In our estimation, the most promising approaches involve using CFC-11 to constrain the amount of deep water formed in the Southern Ocean. [ABSTRACT FROM AUTHOR]

Measurements on fluid inclusions (Timofeeff and others, 2006) indicate that over the last 110 million years, the Mg to Ca ratio in seawater has risen by at least a factor of four. Those by Zachos and others (2003) on planktic foraminifera suggest that about half of this rise occurred during the last 55 million years. Although Coggon and others' (2010) measurements on ridge-flank basalts are consistent with a rise of this magnitude, they indicate that it occurred after 46 million years ago and perhaps even as recently as the last 15 million years. Based on the Mg to K trend in 36 million-year-old halite-hosted fluid inclusions, Brennan and others (2013) confirm Zimmerman's (2000) conclusion that the Mg content of sea salt was about 35 percent lower than now at that time. Hence, if the Coggon and others' (2010) results are to be believed, then the rise in Mg must have been accompanied by a drop in calcium. When account is taken that the C02 content of the atmosphere 35 million years ago was about five times larger than it is today, then perhaps at that time, the dissolution rate of limestone was greater than today's. If so, then the large increase in Mg to Ca ratio could be explained by a combination of a decrease in sea level which slowed the rate of dolomite formation and a drop in atmospheric CO2 content which slowed the delivery by rivers to the sea of Ca derived from limestone weathering. Unfortunately, as the deposition of gypsum prior to halite formation removed virtually all the calcium from the brine pools in which the halite subsequently formed, there is no record of Ca in Cenozoic-age fluid inclusions. Hence, in order to resolve the difference between the large Mg/Ca rise over the last 40 million years suggested by ridge-plank calcites and, the smaller one suggested by planktic foraminifera, an additional proxy for Ca is needed. As I suggested many years ago (Broecker, 1970), one such candidate is the uranium content of corals. [ABSTRACT FROM AUTHOR]

Deep-ocean carbonate ion concentrations ([CO32-]) and carbon isotopic ratios (δ13C) place important constraints on past redistributions of carbon in the ocean-land-atmosphere system and hence provide clues to the causes of atmospheric CO2 concentration changes. However, existing deep-sea [CO32-] reconstructions conflict with one another, complicating paleoceanographic interpretations. Here, we present deep-sea [CO32-] for five cores from the three major oceans quantified using benthic foraminiferal boron/calcium ratios since the last glacial period. Combined benthic δ 13C and [CO32-] results indicate that deep-sea-released CO2 during the early deglacial period (17.5 to 14.5 thousand years ago) was preferentially stored in the atmosphere, whereas during the late deglacial period (14 to 10 thousand years ago), besides contributing to the contemporary atmospheric CO2 rise, a substantial portion of CO2 released from oceans was absorbed by the terrestrial biosphere. [ABSTRACT FROM AUTHOR]

The article presents an abstract of comments written on the article "Deep-Sea Temperature and Ice Volume Changes Across the Pliocene-Pleistocene Climate Transitions," by S. Sosdian and Y. Rosenthal in the July 17, 2009 issue.