Porewater δ13CDOC indicates variable extent of degradation in different talik layers of coastal Alaskan thermokarst lakes

• Published in: Biogeosciences
• Main Authors: Meisel, Ove H., Dean, Joshua F., Vonk, Jorien E., Wacker, Lukas, Reichart, Gert-Jan, Dolman, Han
• Format: Text
• Language: English
• Published: 2021
• Subjects: Arctic; Talik; permafrost; Thermokarst; Alaska
• Online Access: https://doi.org/10.5194/bg-18-2241-2021; https://bg.copernicus.org/articles/18/2241/2021/

Thermokarst lakes play an important role in permafrost environments by warming and insulating the underlying permafrost. As a result, thaw bulbs of unfrozen ground (taliks) are formed. Since these taliks remain perennially thawed, they are zones of increased degradation where microbial activity and geochemical processes can lead to increased greenhouse gas emissions from thermokarst lakes. It is not well understood though to what extent the organic carbon (OC) in different talik layers below thermokarst lakes is affected by degradation. Here, we present two transects of short sediment cores from two thermokarst lakes on the Arctic Coastal Plain of Alaska. Based on their physiochemical properties, two main talik layers were identified. A “lake sediment” is identified at the top with low density, sand, and silicon content but high porosity. Underneath, a “taberite” (former permafrost soil) of high sediment density and rich in sand but with lower porosity is identified. Loss on ignition (LOI) measurements show that the organic matter (OM) content in the lake sediment of 28±3 wt % ( 1 σ , n =23 ) is considerably higher than in the underlying taberite soil with 8±6 wt % ( 1 σ , n =35 ), but dissolved organic carbon (DOC) leaches from both layers in high concentrations: 40±14 mg L −1 ( 1 σ , n =22 ) and 60±14 mg L −1 ( 1 σ , n =20 ). Stable carbon isotope analysis of the porewater DOC ( δ 13 C DOC ) showed a relatively wide range of values from −30.74 ‰ to −27.11 ‰ with a mean of <math xmlns="http://www.w3.org/1998/Math/MathML" id="M23" display="inline" overflow="scroll" dspmath="mathml"><mrow><mo>-</mo><mn mathvariant="normal">28.57</mn><mo>±</mo><mn mathvariant="normal">0.92</mn></mrow></math> <svg:svg xmlns:svg="http://www.w3.org/2000/svg" width="70pt" height="10pt" class="svg-formula" dspmath="mathimg" md5hash="cc170526505501bc8c89012fee9729bb"><svg:image xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="bg-18-2241-2021-ie00001.svg" width="70pt" height="10pt" src="bg-18-2241-2021-ie00001.png"/></svg:svg> ‰ ( 1 σ , n =21 ) in the lake sediment, compared to a relatively narrow range of −27.58 ‰ to −26.76 ‰ with a mean of <math xmlns="http://www.w3.org/1998/Math/MathML" id="M28" display="inline" overflow="scroll" dspmath="mathml"><mrow><mo>-</mo><mn mathvariant="normal">27.59</mn><mo>±</mo><mn mathvariant="normal">0.83</mn></mrow></math> <svg:svg xmlns:svg="http://www.w3.org/2000/svg" width="70pt" height="10pt" class="svg-formula" dspmath="mathimg" md5hash="2725490854322eebaa3bb08f0a7a4852"><svg:image xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="bg-18-2241-2021-ie00002.svg" width="70pt" height="10pt" src="bg-18-2241-2021-ie00002.png"/></svg:svg> ‰ ( 1 σ , n =21 ) in the taberite soil (one outlier at −30.74 ‰). The opposite was observed in the soil organic carbon (SOC), with a narrow δ 13 C SOC range from −29.15 ‰ to −27.72 ‰ in the lake sediment ( <math xmlns="http://www.w3.org/1998/Math/MathML" id="M36" display="inline" overflow="scroll" dspmath="mathml"><mrow><mo>-</mo><mn mathvariant="normal">28.56</mn><mo>±</mo><mn mathvariant="normal">0.36</mn></mrow></math> <svg:svg xmlns:svg="http://www.w3.org/2000/svg" width="70pt" height="10pt" class="svg-formula" dspmath="mathimg" md5hash="527ef9eb01d30114e7d3c9d9f23fd36c"><svg:image xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="bg-18-2241-2021-ie00003.svg" width="70pt" height="10pt" src="bg-18-2241-2021-ie00003.png"/></svg:svg> ‰, 1 σ , n =23 ) in comparison to a wider δ 13 C SOC range from −27.72 ‰ to −25.55 ‰ in the underlying taberite soil ( <math xmlns="http://www.w3.org/1998/Math/MathML" id="M43" display="inline" overflow="scroll" dspmath="mathml"><mrow><mo>-</mo><mn mathvariant="normal">26.84</mn><mo>±</mo><mn mathvariant="normal">0.81</mn></mrow></math> <svg:svg xmlns:svg="http://www.w3.org/2000/svg" width="70pt" height="10pt" class="svg-formula" dspmath="mathimg" md5hash="c52a3b77fdd7a4d588069a90fa906142"><svg:image xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="bg-18-2241-2021-ie00004.svg" width="70pt" height="10pt" src="bg-18-2241-2021-ie00004.png"/></svg:svg> ‰, 1 σ , n =21 ). The wider range of porewater δ 13 C DOC values in the lake sediment compared to the taberite soil, but narrower range of comparative δ 13 C SOC , along with the δ 13 C-shift from δ 13 C SOC to δ 13 C DOC indicates increased stable carbon isotope fractionation due to ongoing processes in the lake sediment. Increased degradation of the OC in the lake sediment relative to the underlying taberite is the most likely explanation for these differences in δ 13 C DOC values. As thermokarst lakes can be important greenhouse gas sources in the Arctic, it is important to better understand the degree of degradation in the individual talik layers as an indicator for their potential in greenhouse gas release, especially, as predicted warming of the Arctic in the coming decades will likely increase the number and extent (horizontal and vertical) of thermokarst lake taliks.