The transfer of bomb radiocarbon and anthropogenic lead to the deep North Atlantic Ocean observed from a deep sea coral

- A ∼560 yr history of C14, Pb, and Pb isotopes in the deep North Atlantic Ocean was reconstructed.
- Deep-ocean Pb increased by ∼5 fold due to the intrusion of anthropogenic Pb.
- Deep-ocean ΔC14 increased by ∼40‰ due to the intrusion of bomb-radiocarbon.
- Approx. 25 yr of transit time is estimated for 14C and Pb by comparing the data to the surface ocean record.
- Model suggests that mixing is as important as advection in the transport of these tracers.

Deep-ocean, ΔC14, Pb concentrations, and Pb isotopes were reconstructed from a deep-sea coral Enallopsammia rostrata from 1410 m depth off of Bermuda. Our high-resolution time series is created from closely spaced radial cross sections, with samples taken from the center of concentric coral growth bands that we show to be the oldest portion of the section. Prebomb radiocarbon ages from the coral demonstrate that the vertical growth rate of the coral is linear, and the age of the coral is estimated to be 560-630 yr old based on the growth rate. Using this age model to reconstruct ΔC14 in deep seawater, we first detect bomb radiocarbon at the coral growth site around 1980, and show that ΔC14 increased from −80±1‰ (average 1930-1979) to a plateau at −39±3‰ (1999-2001). Pb/Ca of the coral ranges between 1.1-4.5 nmol/mol during the 16th and 17th centuries, and Pb isotope ratios (206Pb/207Pb = 1.21, 208Pb/207Pb = 2.495) in this period agree with pre-anthropogenic values found in the pelagic sediments of the North Atlantic Ocean basin. Coral Pb/Ca is slightly elevated to 6.2±0.9 nmol/mol between the 1740s and the 1850s and then increases to 25.1±0.2 nmol/mol in the 1990s. The increase in coral Pb/Ca is accompanied by a decrease in coral 206Pb/207Pb and 208Pb/207Pb, indicating that the increase was caused by the infiltration of anthropogenic Pb to the coral growth site. Comparing our data to the surface coral ΔC14 and Pb records from Bermuda reveals a time scale of tracer transport from the surface ocean to the coral growth site. Some characteristic features, e.g., the bomb-derived ΔC14 increase, appear in the deep ocean approximately 25 yr later than the surface, but the overall increase of ΔC14 and Pb in the deep ocean is smaller and slower than the surface, showing the importance of mixing during the transport of these tracers.