Influence of the High Arctic Igneous Province on the Cenomanian/Turonian boundary interval, Sverdrup Basin, High Canadian Arctic

Abstract

Emplacement of Large Igneous Provinces (LIPs) had a major effect on global climate, ocean chemistries as traced in sedimentary records and biotic turnovers. The linkage between LIPs and oceanic anoxic events has been documented with the Cenomanian/Turonian boundary event and Oceanic Anoxic Event 2 (OAE2). The Caribbean LIP and High Arctic Large Igneous Province (HALIP) are regarded as possible triggers. The pericratonic Arctic Sverdrup Basin is the partial location of the HALIP, where little is known about sedimentary, geochemical and biotic responses to the HALIP phases. Sedimentary strata at Glacier Fiord, Axel Heiberg Island, exhibit a dynamic Cretaceous polar carbon burial history within the lower to middle Cenomanian Bastion Ridge Formation and upper Cenomanian to Turonian part of the Kanguk Formation. We present the first initial 187 Os/ 188 Os (Os i) composition profile for a polar Cenomanian/Turonian boundary interval (~100-93.9 Ma) linked to recently dated magmatic phases of the Strand Fiord Formation, part of the HALIP. The carbon isotope record coupled with the Os i profile show two events in the upper Cenomanian interval marked by positive carbon perturbations and shifts to more non-radiogenic Os i compositions. The earlier short-lived event is interpreted as result of weathering of the surrounding Strand Fiord volcanics causing a local non-radiogenic Os i signal. Coinciding transgressive shorelines let to an increase in marine and terrestrially derived organic matter. Subsequently, injection of mantle-derived basalts into organic rich sediments is credited with causing the release of methane documented in a distinct negative carbon isotope excursion. We speculate that the methane release of the HALIP was an important contribution for rapid global warming caused by increasing atmospheric CO 2 levels associated with the OAE2 event likewise recognized in the Sverdrup Basin. As climate cooled in the middle and late Turonian, carbon burial decreased under increasingly oxygenated benthic conditions. Epifaunal 3 foraminiferal species, adapted to low oxygen conditions, persisted during the OAE2. Our Cenomanian to Turonian multiproxy record of the Sverdrup Basin distinguishes between local and global signals within a restricted High Arctic basin. Our results demonstrate the interplay between basin tectonism and sea-level change, increased weathering during transgressive phases, seafloor processes such as hydrothermal activity and methane release and biotic response to a complex paleoceanography. With future reliable dated frameworks this unique polar record will facilitate correlations to other polar basins and records of lower paleolatitudes.

Cyanobacteria Proliferation in the Cenomanian‐Turonian Boundary Interval of the Apennine Carbonate Platform: Immediate Response to the Environmental Perturbations Associated With OAE‐2?

“…OAE-2 has been associated with LIP volcanism commencing~30-315 kyr before the onset of the event, as indicated by Os isotope data (Du Vivier et al, 2014; VP-1 in Figure 8). This timing suggests a close relationship between the first pulse of LIP Volcanism recorded by Os-isotopes (Du Vivier et al, 2014;Schroder-Adams et al, 2019) and bacterial proliferation observed on the ACP (Figure 8). This timing suggests a close relationship between the first pulse of LIP Volcanism recorded by Os-isotopes (Du Vivier et al, 2014;Schroder-Adams et al, 2019) and bacterial proliferation observed on the ACP (Figure 8).…”

“…Combining the chemostratigraphic framework established for OAE-2 on the ACP, approximating an event duration of~445 to 820 kyr (Eldrett et al, 2014(Eldrett et al, , 2015Li et al, 2017;Ma et al, 2014;Sageman et al, 2006;Voigt et al, 2008), and presuming no large hiatus in the sedimentary succession during the OAE-2 interval Parente et al, 2007), the beginning of the first dark laminite unit can be placed~40 to 70 kyr before the first positive δ 13 C carb shift that denotes the onset of OAE-2. This timing suggests a close relationship between the first pulse of LIP Volcanism recorded by Os-isotopes (Du Vivier et al, 2014;Schroder-Adams et al, 2019) and bacterial proliferation observed on the ACP (Figure 8).…”

“…Large emissions of CO 2 were released during this time due to intense volcanic activity associated with the emplacement of Large Igneous Provinces (LIPs; Caribbean and High Arctic LIPs). These periods of enhanced eruptive activity have been invoked as the possible trigger of OAE-2 (Du Vivier et al, 2014Flögel et al, 2011;Jenkyns et al, 2017;Jones & Jenkyns, 2001;Kuroda et al, 2007;Meyers, 2014;Schaife et al, 2017;Schroder-Adams et al, 2019;Snow et al, 2005;Tegner et al, 2011;Turgeon & Creaser, 2008). Following, the CO 2 emitted to the atmosphere would have increased temperature and precipitation extremes (Heimhofer et al, 2018;Van Helmond et al, 2014;Wagner et al, 2013).…”

A Re‐evaluation of the Plenus Cold Event, and the Links Between CO2, Temperature, and Seawater Chemistry During OAE 2

“…A link has been drawn between LIPs and oceanic anoxic events, particularly with respect to the Caribbean and High Arctic Large Igneous Provinces as possible triggers for OAE 2 (e.g., Snow et al, ; Tegner et al, ; Zheng et al, ). Osmium‐isotope records from across the world have identified periods of volcanism or some form of basalt–seawater interaction around the Cenomanian–Turonian boundary, indicating likely LIP activity immediately prior to the onset of OAE 2 (Du Vivier et al, , ; Scaife et al, ; Schröder‐Adams et al, ; Turgeon & Creaser, ). Basalt–seawater interactions would not have just affected seawater Nd and Os but also other trace metals and isotopes, which further complicates the interpretation of their sedimentary records.…”

Finding the VOICE: organic carbon isotope chemostratigraphy of Late Jurassic – Early Cretaceous Arctic Canada

“…deep basin ventilation), decreased sea-surface productivity (Weissert & Channell, 1989;Weissert & Erba, 2004), increased flux of 12 C into surface waters by upwelling of 12 C-rich bottom waters (Küspert, 1982) or intensified weathering and riverine input of dissolved inorganic carbon (Weissert & Mohr, 1996). A geological rapid release of 12 C into the atmosphere associated with volcanism, methane release from dissociation of gas hydrates or combustion of organic matter associated with emplacement of large igneous bodies are other mechanisms that can cause a negative excursion in δ 13 C (Dickens et al 1995;Hesselbo et al 2000;Padden et al 2001;Schröder-Adams et al 2019).…”