# Lomagundi-Jatuli Carbon Isotope Excursion

The Lomagundi-Jatuli Carbon Isotope Excursion or Lomagundi-Jatuli Event (LJE) was a carbon isotope excursion that occurred in the Paleoproterozoic between 2.3-2.1 Ga, possessing the largest magnitude and longest duration of positive δ$^{13}$C values found in marine carbonate rocks. The δ$^{13}$C values range from +5 to + 30‰. Carbon isotope compositions in marine carbonates typically fluctuate around zero per mil (‰) through time. To coincide with the LJE global δ$^{13}$Ccarb levels, the amount of buried organic carbon would have needed to double or triple, and over millions of years.
Measuring δ$^{13}$Ccarb values within marine carbonate rocks provides scientists with a window into the history of fluxes in the global carbon cycle over the course of Earth history.
In the context of the global carbon cycle, "flux" refers to the movement or flow of carbon between different reservoirs or components of the Earth system. This includes the atmosphere, oceans, terrestrial biosphere (plants and soil), and geosphere (rocks and sediments). These carbon fluxes are driven by various processes, including photosynthesis (which removes CO$_2$ from the atmosphere and incorporates it into plant biomass), respiration and decay (which return CO$_2$ to the atmosphere), weathering of rocks (which can transfer carbon from the geosphere to the hydrosphere and atmosphere), and the dissolution and precipitation of carbonate minerals in the ocean
Understanding these fluxes, especially within the LJE, is crucial for studying the global carbon cycle. They determine the concentration of carbon dioxide in the Earth's atmosphere, which in turn influences the planet's climate. While the LJE's high δ$^{13}$C$_{carb}$ values were first thought to show a substantial local increase in organic carbon (f$_{org}$) in the localities in which the elevated values were found, marine carbonate outcrops with similarly elevated values have since been found around the world, shifting consideration that this event reflects a global increase.
Changes in carbon fluxes can lead to significant variations in atmospheric CO$_2$ levels and thus have been a major focus of research, and debate, especially in the context of anthropogenic climate change.

## Locations and duration

Assuming this excursion is globally synchronous in its commencement and termination, the duration has been dated to range from a maximum of 249 ± 9 Myr (2306 ± 9 Ma to 2057 ± 1 Ma) to a minimum of 128 ± 9.4 Myr (2221 ± 5 Ma to 2106 ± 8 Ma).
| Region | Formation | Age (Ma) | Method | Max or Min |
| Wyoming, USA | Fletcher Park Rhyolite | 1780 +- 6 | ID-TIMS | Min |
| Wyoming, USA | Keystone Quartz Diorite | 1781 +- 7 | ID-TIMS | Min |
| Uruguay | Uruguayan Dyke swarm | 1790 +- 5 | ID-TIMS | Min |
| Pilbara Craton, Australia | June Hill Volcanics | 1795 +- 7 | SIMS | Min |
| Gabon, Africa | Francevillian Basin | 2050 +- 30 | ID-TIMS | Max |
| South Africa, Africa | Rooihoogte Formation | 2316+-7 | TIMS (Re-Os) | Max |
| Russia, Kola Craton | Polisarka Sedimentary Formation | 2434 +-1.2 | ID-TIMS | Max |
Table 1: Lomagundi-Jatuli Event localities presenting similarly elevated δ$^{13}$C values, formations of occurrence, dated age of formation, and procedural method of δ$^{13}$C value analysis.
The extremely positive carbon isotope values having occurred during the LJE can be seen on all continents, with the notable exception of Antarctica, having stratigraphic thickness ranging from several to tens of meters The highly elevated δ$^{13}$C values were first found in the Lomagundi Group in Zimbabwe and the Jatuli group in Fennoscandia at a time when the LJE was first hypothesized to have been a local event.
| Geographic and geological location | Carbonate lithology | δ13Ccarb variation (‰) | Stratigraphic Thickness | References |
| Africa | | | | |
| Lomagundi Group, Zimbabwe | Dolostones | 4.0 to +13.4 | 300 m | |
| Francevillian Series, Gabon | Dolostones | 2.6 to +6.3 | 600–2040 m | [6] [7] |
| Gumbu Group, South Africa | Limestones | 4.6 to +7.0 | | |
| Duitschland Formation, Pretoria Group | Dolostones | −2.0 to +10.1 | 1000m | |
| Sengoma formation, Botswana | Dolostones and limestones | 7.6 to 9.2 | 167 m | |
| Silverton formations Pretoria Group, South Africa | Dolostones and limestones | 8.3 to +11.2 | 500 to 700 m | |
| Lucknow Formation, Elim Group | Dolostones | 8.7 to +10.4 | 200m | |
| Australia | | | | |
| Bubble Well Member, Juderina Formation, Nabberu Basin | Dolostones | 5.7 to +8.8 | 160m | [12] [13] |
| Asia | | | | |
| Jhamarkotra Formation, Aravalli Supergroup, India | Dolostones | 5.4 to +11.1 | 1500m | |
| South America | | | | |
| Cercadinho Formation, Minas Supergroup, Brazil | Dolostones | 3.3 to +5.4 | 317m | |
| Fecho do Funil Formation, Minas Supergroup, Brazil | Dolostones | 5.6 to +7.4 | 38-50m | |
| Rio Itapicuru Greenstone Belt, Brazil | Dolostones | 5.5 to +9.0 | 20-30m | |
| Ipueira-Medrado, Itabuna-Salvador-Curaçá orogen, Brazil | Dolostones | 2.2 to +6.9 | 30-40m | |
| Paso Severino Fm., Río de la Plata craton, Uruguay | Dolostones | −5.6 to +11.6 | 2100-2700 | |
| North America | | | | |
| Gordon Lake Formation, Canada | Dolostones | -1 to +8.2 | 300-700 meters | |
| Kona Dolomite, United States | Dolostones | 1.9 to +9.5 | 870 meters | |
| Nash Fork Formation, United States | Dolostones | 0.2 to 28.2 | 1700m | |
| Slaughterhouse Formation, United States | Dolostones | 5.6 to +16.6 | 500m | |
Table 2: Carbonate lithology within global formations, including associated δ13Ccarb variation (‰) values, and stratigraphic thicknesses of each.

## Methods

Scientists choose which geochronology method is best suited for the types of rocks and sediments they work with. Attempting to find the age of marine carbonate rocks is not without challenge, especially in the use of uranium (U) and lead (Pb). These rocks do not have an initially high composition of uranium, and contain too much lead, both of which can further undergo modification over geologic time (diagenetic overprinting).
Isotope Dilution-Thermal Ionization Mass Spectrometry (ID-TIMS) has been utilized for the analysis of marine carbonate rock δ13 values due its precision <1‰ (single analysis or weighted mean dates) in evaluating $^{206}$Pb/$^{238}$U dates. This method involves a two-step process: isotope dilution, where a known amount of isotopically enriched tracer is mixed with the sample to quantify the concentration of elements, and thermal ionization mass spectrometry, where the sample is ionized at high temperatures to measure the isotopic ratios of elements.
Secondary ion mass spectrometry (SIMS) is a form of desorption mass spectrometry, which is used to analyze the composition of solid surfaces and thin films by sputtering the surface of the specimen with a focused primary ion beam and collecting and analyzing ejected secondary ions. The principle behind SIMS is straightforward but involves sophisticated instrumentation and techniques to achieve detailed surface compositional analysis at the micro to nano scale.
Thermal Ionization Mass Spectrometry (TIMS) is a highly precise and sensitive analytical technique used primarily for isotopic analysis (Rhenium-Osmium) and the determination of elemental concentrations in samples. TIMS operates on the principle of thermal ionization, where a sample is vaporized and ionized in a high-temperature environment, allowing for the separation and measurement of isotopes based on their mass-to-charge ratios.
The Re-Os (Rhenium-Osmium) geochronology method is based on the decay of $^{187}$Re to $^{187}$Os, which occurs over a long half-life, making it suitable for dating geological samples that range in age from millions to billions of years. This method is particularly useful for dating organic-rich rocks, such as black shales, and relies on the principle that the ratio of these isotopes in a sample will change over time due to the radioactive decay of $^{187}$Re to $^{187}$Os. By measuring the present-day isotope ratios and knowing the decay rate of $^{187}$Re, scientists can calculate the age of the sample.
One of the challenges in Re-Os geochronology is dealing with the error correlations that arise from measuring these isotopes, particularly because $^{188}$Os, which is used in the denominator of the isotope ratio calculations, is associated with larger mass spectrometer uncertainties. This issue can lead to strong error correlations and potentially obscure geologically significant trends.

## Genesis of the LJE
### Synchronous, global-scale disturbance

The global view concludes that during the Lomagundi carbon isotope excursion carbonates were deposited world-wide with large amounts of 13C enrichment. The hypothesis that the LJE is related to the Great Oxidation Event (GOE), with the LJE causing a large deviation in the global carbon reservoir, which in turn led to disequilibrium of the carbon cycle and released oxygen.
To explain this global 13C enrichment, the oxidation of siderite (FeCO3, with other Fe(2+) carbonate minerals), was proposed as a hypothesis because it produces 4 times the amount of CO2 than it consumes O2. The oxidation of siderite was the driver for the carbon needed in burial and further oxidation, as well as the accumulation of O2, making the length of the LJE dependent on the size of the Archean siderite reservoir.
Another hypothesis to explain the global nature of the LJE, is large tectonic change leading to increased degassing of volcanic CO2, which could have increased deposition of carbonates and organic matter, due to higher weathering rates and nutrients to the ocean. Similar to a tectonic change, the formation of subaerial continents or global glaciations could have also enhanced volcanic CO2 leading to the same outcome of CO2 and O2 in carbonates and atmosphere. Supporting this, there is evidence for the first large continental plates around 2.2-2.1 Gyr experiencing rifting and a global orogeny. During this time frame there was an increase in seawater 87Sr/ 86Sr, which indicates there was higher levels of continental erosion. To reinforce the effect of high 87Sr/86Sr, the first known glaciations occurred during 2.2-2.1 Gyr as well which favours weathering rates by lowering sea level.

### Localized, Facies driven process

This hypothesis acknowledges that there is a global change to the carbon cycle, and agrees that it was a globally synchronous event, but with the idea that different facies environments drive the high C-isotope values. This meaning that the values of d13C and changes in the values are because of processes in individual basins, depending on where the locality is along a carbonate platform/slope. Using 13C carbonate data from locations worldwide and the stratigraphic descriptions, the values can be organized into open marine, nearshore marine-inner shelf and intertidal-coastal-sabka, with a noticed correlation between facies and 13C carbonate values. For open marine the mean 13C carbonate value was +1.5 ± 2.4‰, +6.2 ± 2.0‰ for inner-shelf, and +8.1 ± 3.8‰ for intertidal settings. Using this hypothesis, the extremely positive d13C values can be explained by changes in local dissolved inorganic carbon (DIC) pools, influenced in individual basins, not representative of world-wide change in ocean DIC.

### Localized, Diagenesis or Methanogenesis

For a global carbon isotope excursion, sedimentary organic carbon (shales) tend to show a trend as well, as an excursion would affect the d13C value of the biosphere and therefore sedimentary organic matter. Between 2.60 and 1.60 Ga there is no trend within organic carbon. Fluctuations in d13C can be linked to isotopic alteration from breakdown of organic matter due to diagenesis and metamorphism.
A process in sediment columns that can contribute to carbonates with high levels of 13C, methanogenesis, could have caused carbonates enriched in 13C, creating an explanation for the d13C values reaching +28‰. To explain the LJE, a deeper methanic zone in oceans during the start of ocean oxygenation (the GOE) would push pore water DIC to higher d13C values. The carbonates forming at this time would record d13C enrichment.