Oxygen and carbon stable isotope tracers of Weddell Sea water masses: new data and some paleoceanographic implications

Mackensen, A (2001) Oxygen and carbon stable isotope tracers of Weddell Sea water masses: new data and some paleoceanographic implications. Deep Sea Research Part I: Oceanographic Research Papers, 48(6). 1401-1422. doi:10.1016/S0967-0637(00)00093-5

Abstract

Stable oxygen isotopic composition of sea water and stable carbon isotopes of Dissolved Inorganic Carbon (DIC) on the continental shelf in the southern Weddell Sea are presented. Using the stations sampled during the summer 1995 two sections can be constructed, one closely parallel to the ice shelf edge and the other one perpendicular to the upper continental slope. Generally, d18O values clearly separate between different shelf water masses depending on the content of meteoric meltwater added during melting of glacial ice. Extrapolation of the mixing line between the cores of High Salinity Shelf Water (HSSW) and supercooled Ice Shelf Water (ISW) reveals d18O values of the glacial ice of -27 �, whereas extrapolation of the mixing line between the d18O values of the most saline HSSW and lowest temperature ISW results in d18O values of -34 � for glacial ice. These values point to an origin of meltwater from below the ice shelf where ice is less depleted in 18O, since deeply beneath the ice shelf close to the grounding line, values may reach -40 �. If values between -34 and -27 � are used as d18O endmember values for glacial ice, the amount of meltwater from the ice shelf that adds to the formation of ISW off the Filchner-Ronne Ice Shelf ranges from 0.2 to 0.8 %, in agreement with previous studies based on d18O and 4He. Carbon isotopic fractionation due to gas exchange between the atmosphere and the ocean at cold temperatures, results in Dd13CDIC values of 0.20±0.17 � for Weddell Sea Deep Water (WSDW), the water mass that ventilates the global abyssal ocean, typically defined as Antarctic Bottom Water (AABW). This confirms the low end of the range estimated previously (0.2 � to 0.4 �), and thus corroborates the dominance of biology in shaping the deep and bottom water d13C signal. It has been hypothesized that different modes of glacial/interglacial Antarctic bottom water formation may be separated by different stable isotopic compositions of deep-sea foraminiferal calcite. Here I show that differences between Dd13C and d18O values of HSSW and ISW, both of which contribute to bottom water formation today, are too small to be resolved in deep and bottom water masses. Therefore, glacial/interglacial changes in relative proportions of these water masses in Antarctic deep and bottom water cannot be separated by stable isotopes of fossil benthic foraminiferal calcite.

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