NOAA/WDS Paleoclimatology - Harding Lake, Alaska 31,000 Year Geochemical Data

Physical and geochemical proxy analyses of sediment cores from Harding Lake in central Alaska Alaska are used to reconstruct paleoenvironmental change and millennial scale fluctuations in lake level for the last ~ 31,000 years. We analyzed a composite 422 cm core from the lake depocenter (42.1 m water depth) and identified 4 distinct lithologic units based on variability in dry bulk density, organic matter, biogenic silica, carbon to nitrogen (C/N) mass ratios, organic matter carbon (d13C) isotopes, pollen, and elemental abundances via scanning X-ray fluorescence, with age control provided by 16 Accelerator Mass Spectrometry radiocarbon dates and 210Pb dating. In addition, we analyzed a transect of cores from 7.1m, 10.75m, 15.91m, and 38.05m water depths to identify lake level fluctuations and to characterize shallow water sediments. Organic matter content and magnetic susceptibility values in surface sediments from all transect cores show a strong correlation with water depth. Interpretation of four dated lithologic units produced a record of water-depth variations that is consistent with independent climate records from eastern Beringia. Basal coarse grained sediments (quartz pebble diamicton) were deposited prior to 30,700 calendar years before present (yr BP), possibly due to fluvial reworking or deflation during a period of severe aridity. Unit 1 sediments were deposited between 30,700 and 15,700 yr BP and are characterized by a low organic matter content, a high magnetic susceptibility, and low biogenic silica concentrations resulting from very low lake levels, low terrestrial and in-lake productivity and a significant flux of clastic sediment. An abrupt increase in organic matter and biogenic silica marks the transition into Unit 2 sediments, which were deposited between 15,700 and 9,400 yr BP when lake levels were higher and variable (relative to Unit 1). Unit 3 sediments began forming at 9,400 yr BP, indicating the final transition to full interglacial conditions. Here an abrupt increase in the sedimentation rate, organic matter content, and biogenic silica occurs (along with a corresponding decrease to low magnetic susceptibility). These high values persist until 8,700 yr BP, signifying a rapid rise to higher lake levels (in comparison to Units 1 and 2). Unit 4 sediments were deposited between 8,700 yr BP to 2010 AD and contain generally high concentrations of organic matter and biogenic silica with low magnetic susceptibility, suggesting that lake levels were relatively high and stable during the middle to late Holocene.