Table of Contents

• Dataset Description
  • Methods & Sampling
  • Data Processing Description
• Data Files
• Parameters
• Instruments
• Deployments
• Project Information
• Funding

Porosity of vertical profiles from multi- and gravity cores from two research cruises, SP1215 and NH1319, in the Santa Monica and Santa Barbara Basins.

Related datasets:
Methane Isotopes
DOC and Isotopes
POC and Isotopes
Other Solutes
DIC and Isotopes

Sediment cores were recovered using the following coring equipment:
Ocean Instruments multicorer MC-800 (SP1215) and MC-400 (NH1319)
OSU Gravity Core (6 meters long, 4 inch diameter)
OSU “Big Bertha” Core (12 meters long, 4 inch diameter)

Multi cores were immediately transferred into a refrigerated van. They were then extruded in an N2 atmosphere within 2-12 hours of recovery.

Gravity cores were sectioned on deck immediately upon recovery. All but one of the gravity cores were secured horizontally on the ship’s deck and sampled from the bottom of the core upwards by sequentially removing 10 cm sediment intervals by cutting the core liner using a pipe cutter. One core was secured vertically and sampled similarly, but from the top down. Freshly exposed sediment was immediately subsampled using 3- to 60-mL push corers made of plastic syringes with the tips removed. All subcores, except those for methane (see next paragraph), were immediately transferred to a N2 filled glove bag in the refrigerated van for further processing.

All sediment aliquots were centrifuged in polycarbonate tubes at 4 degrees C. The supernatant was collected into all-polypropylene syringes with stainless steel needles, and filtered through disposable 0.2 um nylon filters with 0.7 um GF/F pre-filter (Whatman 6870-2502). The first 3 mL were discarded. To minimize the DOC blank, 100 mL of UV-irradiated deionized water were pushed through each disposable filter prior to use. DIC samples for 13C and 14C abundances were immediately flame-sealed under a stream of ultra-high-purity (UHP) N2 into 10-15 mL borosilicate tubes spiked with HgCl2 following (McCorkle et al., 1985). DOC samples for concentration determination only were acidified and ampoulated under a stream of UHP N2 gas and refrigerated. DOC samples for isotopic analyses were frozen without acidification in 20 mL scintillation vials with Teflon-lined caps. Samples for methane concentration and delta 13C values were immediately placed into 20-mL serum glass vials (Wheaton) containing a 5-mm glass bead, basified, sealed with a blue butyl rubber septum (Chemglass), homogenized, crimp sealed, and stored upside down at room temperature until analysis. For analysis of delta 14C values of methane, 150- and 250-mL sediment aliquots were immediately placed into 250- and 500-mL glass media bottles (VWR) containing 80 and 100 mL of 1 M KOH solution, respectively. The bottles were immediately capped with #7 rubber stoppers, sealed thoroughly with electric tape, screw capped, and stored upside down at room temperature until analysis. Centrifuge tubes containing sediment were frozen.

All tools and parts were first cleaned with household dish soap, then acid rinsed (exclusive of metal parts). Plasticware was air dried; glassware and metal tools were baked at 550 degrees C for 4 hours. Bottom-water DIC and DOC samples were collected with a Go Flo bottle following DOE (1994) and Beaupré et al. (2007), respectively.

For further details including quality assurance measures for DOC, see Komada et al. (2013) and Komada et al. (2016). Also refer to the table of information on the methods, relative uncertainity, and references for each analyte (PDF).

References:
Beaupré S. R., Druffel E. R. M. and Griffin S. (2007) A low-blank photochemical extraction system for concentration and isotopic analyses of marine dissolved organic carbon. Limnol. Oceanogr. Methods 5, 174–184.

Burdige D. J. and Gardner K. G. (1998) Molecular weight distribution of dissolved organic carbon in marine sediment pore waters. Mar. Chem. 62, 45–64.

Burdige D. J. and Zheng S. L. (1998) The biogeochemical cycling of dissolved organic nitrogen in estuarine sediments. Limnol. Oceanogr. 43, 1796–1813.

Cline J. D. (1969) Spectrophotometric determination of hydrogen sulfide in natural waters. Limnol. Oceanogr. 14, 454–458.

DOE (1994) Handbook of Methods for the Analysis of the Various Parameters of the Carbon Dioxide System in Sea Water; version 2. eds. A. G. Dickson and C. Goyet, ORNL/CDIAC-74.

Druffel E. R. M., Williams P. M., Bauer J. E. and Ertel J. R. (1992) Cycling of dissolved and particulate organic matter in the open ocean. J. Geophys. Res. Ocean. 97, 15639–15659.

Gieskes J. M., Gamo T. and Brumsack H. (1991) Chemical methods for interstitial water analysis aboard JOIDES RESOLUTION: Ocean Drilling Program, Technical Note 15.

Hall P. O. J. and Aller R. C. (1992) Rapid, small-volume, flow injection analysis for SCO2, and NH4+ in marine and freshwaters. Limnol. Oceanogr. 37, 1113–1119.

Hu X. and Burdige D. J. (2008) Shallow marine carbonate dissolution and early diagenesis - Implications from an incubation study. J. Mar. Res. 66, 489–527.

Hwang J. and Druffel E. R. M. (2005) Blank Correction for ∆14 C measurements in organic compound classes of oceanic particulate matter. Radiocarbon 47, 75–87.

Johnson L. and Komada T. (2011) Determination of radiocarbon in marine sediment porewater dissolved organic carbon by thermal sulfate reduction. Limnol. Oceanogr. Methods 9, 485–498.

Kanamori S. and Ikegami H. (1980) Computer-processed potentiometric titration for the determination of calcium and magnesium in sea water. J. Oceanogr. Soc. Japan 36, 177–184.

Kessler J. D. and Reeburgh W. S. (2005) Preparation of natural methane samples for stable isotope and radiocarbon analysis. Limnol. Oceanogr. Methods 3, 408–418.

Komada T., Anderson M. R. and Dorfmeier C. L. (2008) Carbonate removal from coastal sediments for the determination of organic carbon and its isotopic signatures, d13C and D14C: comparison of fumigation and direct acidification by hydrochloric acid. Limnol. Oceanogr. Methods 6, 254–262.

Komada T., Burdige D. J., Crispo S. M., Druffel E. R. M., Griffin S., Johnson L. and Le D. (2013) Dissolved organic carbon dynamics in anaerobic sediments of the Santa Monica Basin. Geochim. Cosmochim. Acta 110, 253–273.

Komada T., Burdige D. J., Li H. L., Magen C., Chanton J. P. and Cada A. K. (2016) Organic matter cycling across the sulfate-methane transition zone of the Santa Barbara Basin, California Borderland. Geochim. Cosmochim. Acta 176, 259–278.

Lang S. Q., Butterfield D. A., Schulte M., Kelley D. S. and Lilley M. D. (2010) Elevated concentrations of formate, acetate and dissolved organic carbon found at the Lost City hydrothermal field. Geochim. Cosmochim. Acta 74, 941–952.

Lustwerk R. L. and Burdige D. J. (1995) Elimination of dissolved sulfide interference in the flow injection determination of SCO2, by addition of molybdate. Limnol. Oceanogr. 40, 1011–1012.

Magen C., Lapham L. L., Pohlman J. W., Marshall K., Bosman S., Casso M. and Chanton J. P. (2014) A simple headspace equilibration method for measuring dissolved methane. Limnol. Oceanogr. Methods 12, 637–650.

McCorkle D. C., Emerson S. R. and Quay P. D. (1985) Stable carbon isotopes in marine porewaters. Earth Planet. Sci. Lett. 74, 13–26.

McNichol A. P., Jones G. A., Hutton D. L., Gagnon A. R. and Key R. M. (1994) The rapid preparation of seawater Sigma CO (sub 2) for radiocarbon analysis at the National Ocean Sciences AMS facility. Radiocarbon 36, 237–246.

delta 14C and delta 13C values were blank-corrected following Hwang and Druffel (2005) and Kessler and Reeburgh (2005).

BCO-DMO Processing:
- replaced blank cells with nd (no data);
- modified parameter names to conform with BCO-DMO naming conventions;
- replaced the phi symbol with "phi" in the sample_id column.

Description from NSF award abstract:
Organic carbon (Corg) remineralization rates are typically highest near the sediment-water interface, and decrease with depth as labile substrates and strong oxidants are consumed. However, in many ocean margin sediments, at the depth interval where sulfate (SO4=) is exhausted and CH4 concentrations begin to increase (the sulfate-methane transition; SMT), SO4= reduction rates typically show strong sub-surface maxima, indicating locally-enhanced microbial activity and carbon turnover. These hot spots for SO4= reduction are generally attributed to anaerobic oxidation of CH4 by SO4=, but a number of studies have found an excess of SO4= reduction over CH4 oxidation, indicating the presence of a major additional SO4= sink in the SMT.

In this project a research team from San Francisco State University, Florida State University, and Old Dominion University will investigate the nature of this SO4= sink by combining cutting-edge porewater compositional analyses -- del-14C and del-13C of CH4, dissolved organic and inorganic carbon (DOC and DIC), and 1H-NMR on DOC -- with numerical reactive transport modeling. They will test the hypothesis that the SMT is an oxidation front for not just CH4, but also for DOC that is produced deeper in the sediment column, and transported upward into the SMT. They will also test the idea that not all of this DOC is oxidized in the SMT, and that some reaches the surface sediments, and represents a source of 14C-depleted (pre-aged) DOC to the oceans. The premise is that DOC production from Corg is enhanced in methanogenic sediments due to an uncoupling in the anaerobic food chain between terminal metabolism and fermentation reactions involved in the overall Corg remineralization process. The work will focus on two ocean margin sites, Santa Monica Basin and Santa Barbara Basin, which despite their geographic proximity, appear to have different CH4 dynamics in the deep sediments.

This study should result in a greater understanding of the role of sub-surface sediments in the overall benthic Corg remineralization process, and in the exchange of major elements between the sea floor and the water column. It will also allow testing of the hypothesis that marine sediments are sources of 14C-depleted, recalcitrant DOC to the overlying water column, thereby addressing a problem that has perplexed chemical oceanography for several decades: what factors control the 14C signature of DOC in the deep oceans?