Oxygen in the Atmosphere
For the first 2 billion years (2Ga) of the earth’s existence (4.5Ga - 2.5Ga) the atmosphere consisted largely of nitrogen and carbon dioxide, along with significant amounts of methane, ammonia, sulphuric acid and water vapor. Free oxygen was non-existent or, at best, present as a trace gas.
A depiction of the earth’s surface and atmosphere as it might have been during the first 0.5Ga of its existence (the Hadean Eon). A recently separated moon looms large on the horizon. Painting by Steve Munsinger.
Evolving in this anoxic reducing environment, anaerobic single-celled prokaryotic life first appeared in the waters of the world around 3.6Ga, deriving its energy from volcanic heat. After a few hundred million years of evolution, one of these organisms called cyanobacteria (a.k.a. blue-green algae) developed the ability to split the CO2 dissolved in oceans and seas into its constituent components of carbon and oxygen using solar radiation as an energy source.
As the name implies, taxonomists classify the blue-green algae as a class of bacteria, but they were a transitional species to the first true first plants. Taxonomists always have great trouble positioning transitional species: there are no hard boundaries in evolution.
The biochemical process that the cyanobacteria invented is known as photosynthesis. The carbon was used to make the organic compounds of life, releasing oxygen back to the atmosphere as a waste product.
The cyanobacteria turned out to be an extraordinarily successful and enduring class of life. They are still with us today.
In the warm tropical waters of the intertidal zone at Shark Bay in Western Australia, thin films of cyanobacteria cement sand to form layered, dome-shaped mounds known as stromatolites. Fossil stromatolite structures in the stratigraphic record go back almost 2 billion years.
The 0xygen content of the atmosphere slowly increased.
The greater part of the solar energy used in the photosynthesis process was stored by the plant in the chemical bonds of its organic compounds. Excepting only the nuclear energy of the radioactive elements, photosynthesis is the most efficient energy storage system that we know.
Between 2.4Ga and 1.8Ga, the evolution of the eukaryotic cell and multicellular life forms made photosynthesis more efficient and plant life more abundant and widespread. More CO2 was consumed, more O2 was released. An initial slow increase in atmospheric oxygen became, around 2.5Ga, a step increase. This was the most important change in the evolution of the earth’s atmosphere and is known as the Great Oxidation Event, or GOE.
Today our atmosphere contains, by volume, around 21% oxygen and 79% nitrogen. A mere trace of carbon dioxide remains, making up just 0.0042% or 420 parts per million. Methane is even more trace at 1.3 parts per billion while Sulphuric Acid is less than 1 part per trillion.
The reverse process to photosynthesis in plants and animals is respiration. In respiration, living things power their activities by burning a small proportion of their stored carbohydrate in oxygen, thus releasing some carbon back to the atmosphere as CO2. On the death of the organisms, the bulk of their carbon accumulated as organic-rich deposits on the sea floor. There, sealed from oxygen by later sediment, with time they transformed to coal, oil and gas.
The Role of Iron
Iron is a heavy element (atomic number 26) that arrived in the early accreting days or the early earth through continuous meteor impact. Today, iron is the most abundant element in the planet. In the crust it is the 4th most abundant element. In basaltic rocks, iron constitutes around 10-15%.
The early crust was dominated by rocks of basaltic composition.
Iron comes in two flavours called valency states: ferrous iron, written Fe 2+ (or 2 electrons short of the full set of 8 in its outer shell) and ferric iron written Fe 3+ (3 electrons short). The metal thus has great capacity for combining with elements of negative charge, particularly oxygen, which is ever hungry for a positively charged valency partner. If only a small amount of oxygen is available to it, iron forms low-oxidation ferrous oxide. Where there is abundant oxygen, it forms high-oxidation ferric oxide compounds.
But note, there is an important distinction between the two states of iron. Ferrous iron compounds are generally soluble in water; ferric iron compounds are not.
In the low oxygen reducing atmosphere of the first 2 billion years of earth history, chemical erosion of basaltic rocks at surface produced soluble ferrous iron oxide compounds, which, washed to the sea, slowly accumulated in the oceans of the world. Trillions of tons of dissolved iron. During the GOE, over a relatively short time span (geologically speaking) of a few hundred million years or so, the oceanic reservoir of ferrous iron became oxygenated to ferric iron which, being insoluble, settled as chemical sediment to the sea floor to form thick iron rich sequences of great thickness and lateral extent.
In later geological periods, chemical sediments were dominantly carbonates. In the late Archaean to early Proterozoic, it was mainly ferric iron.
These distinctive iron rich deposits are known as Banded Iron Formations (BIF). They are preserved today around all the ancient shield areas of the world: Western Australia, Brazil, Venezuela, North America, India, West Africa and parts of eastern Asia.
Banded iron formation in the Karinjini National Park, Hamersley Range, Western Australia. Image by the WA Tourist Department
But another process was at play during the GOE..
High levels of free oxygen in the atmosphere are highly corrosive. It breaks down the minerals of rocks in contact with it. It puts a limit on the individual life spans of all living things, including us. Every wildfire is a demonstration of what unstoppable explosive oxidation looks like. Some have referred to the Great Oxidation Event as the Great Oxygen Catastrophe.
The GOE (or, depending on your point of view, the GOC) supercharged erosion of all exposed land surfaces especially as, back then, there were no land plants to bind soils and constrain river channels. Beginning around 2.5Ga, increasing floods of clastic sediment poured off the land creating, for the first time at volume, wide sedimentary shelves and shallow marginal seas around the great continental land masses. At the base of these sequences, interspersed with silica and aluminium rich clastic sediment, are the Banded Iron Formations.
The Economic Importance of Banded Iron Formations
Iron, by a very large margin, is the cheapest, most abundant and most useful metal available to us today. We first learnt how to smelt it from oxide ores more than 2000 years ago, thus initiating the Iron Age and supplanting the previous Bronze Age. Ore suitable to smelt iron is practically ubiquitous, whereas copper and tin ores (especially tin) that are needed to make bronze are geographically restricted.
BIFs overall contain around 30% iron by weight, but natural processes, operating over time, have locally upgraded them to 60-65% iron: almost pure iron oxide (Fe2O3). These high-grade zones are extracted in vast open cast mines which, after smelting, are the source of 95% of our iron and steel. Around the world, ship-borne high-grade BIF ore have now almost totally supplanted local low-grade deposits
Four point eight billion tons of iron ore were mined in 2025. The four biggest producers are Australia (980mt), Brazil (410mt), China (340mt) and India (125mt).
Abundant iron in the form of its alloy steel builds the skeletal frameworks of our civilisation. From bridges to buildings, ships to railroads, cars to trucks to turbines to tanks, we owe our ready supply of ore to the Great Oxidation Event, and to the fossil remains of plant material with which we reduce it to iron and steel.
But will this Bonanza Last?
Nothing is forever. No resource is inexhaustible. However, although 4.8 billion tons may sound like a large number, it is trivial compared to the ore available to us.
There is no prospect of it running out within this millennium.