A climate history of the Earth

Climate is the long-term pattern of weather in a particular region, usually measured over 30 years or more. Weather can change every few hours, but throughout the year, similar patterns repeat annually- for example, summers are typically hot and tend to occur during the same months each year. However, these patterns are now shifting due to climate change.¹ ² ³

Our current atmosphere⁴ ⁵ ⁶ ⁷ ⁸ ⁹ ¹⁰ ¹¹ ¹²
A planet’s atmosphere is a layer of gases that blanket the planet because its gravity has caught hold of them. For Earth, this layer begins at the surface of the planet, and extends up to around 10,000 kilometres, though most of the atmosphere lies within the first 100 kilometres.

Our atmosphere at the moment is approximately 78% nitrogen, 21% oxygen, and 1% other gases including carbon dioxide (approximately 0.04% of the atmosphere, which is 420+¹³ ¹⁴ ppm as of 2024), water vapour, and argon. It is now divided into five distinct layers based on how temperature changes with altitude:

1. The Troposphere (0-12 km)¹⁵ ¹⁶
This is the lowest layer where we live and breathe. It contains about 75-80% of all the air in the atmosphere and almost all water vapour, which forms our clouds and weather. Temperature decreases as you go higher- about 6.5°C cooler for every kilometre up. This is where all our weather happens, including storms, rain, and snow. Commercial airplanes typically fly in the upper part of this layer.

2. The Stratosphere (12-50 km)¹⁷
Above the troposphere lies the stratosphere, which contains the ozone layer (formed between 600 to 500 million years ago¹⁸, the Stratosphere contains about 90% of Earth’s ozone). Unlike the troposphere, temperature increases with altitude here because ozone absorbs UV energy from the Sun. This layer is very stable with little weather activity, making it ideal for some aircraft to fly in.

3. The Mesosphere (50-85 km)
The mesosphere is where the temperature decreases again with altitude, reaching as low as -90°C. Most meteors burn up in this layer, creating “shooting stars.” Rare, shimmering noctilucent clouds also appear here sometimes.

4. The Thermosphere (85-600 km)
In this layer temperatures can reach up to 1,500°C or higher, though the air is so thin that you wouldn’t feel hot. This is where the International Space Station orbits and where we see the beautiful aurora (northern and southern lights) when solar particles interact with the atmosphere. Radio waves also bounce off this layer, enabling long-distance communication.

5. The Exosphere (600+ km)
The outermost layer, the exosphere, gradually fades into space. The air here is so thin that molecules rarely collide with each other, and this is where many satellites orbit.

Structure ¹⁹²⁰
The Earth’s orbital parametres, axial tilt, and magnetic field have profoundly shaped our planet’s atmosphere, climate, geology, and ecology throughout its 4.6-billion-year history. Our orbital variations, known as Milankovitch cycles, operate on timescales of tens to hundreds of thousands of years and have been fundamental drivers of climate change throughout our planet’s geological history.

Birth²¹ ²² ²³
When our planet was new (new-ish, around 4.6 billion years ago), it had no atmosphere at all. However, sometime later it likely captured passing helium and hydrogen atoms to cover itself in a flimsy lamina of hydrogen and helium, which are the lightest and most abundant materials in the universe, but later, because early Earth was so hot and these gases were so light, these gases escaped into space, leaving our planet with virtually no air.

Several billion years later, between 4.5-4.0 billion years ago²⁴ ²⁵, the planet had (finally) begun to cool, and massive volcanic eruptions had started spewing gases from the Earth’s interior. These gases included water vapour (steam), carbon dioxide, nitrogen, methane, and ammonia, in a process now named “outgassing”.²⁶ ²⁷ This was our second atmosphere, a thick, steamy, poisonous (to the current inhabitants of the planet) soup largely dominated by carbon dioxide and water vapour, and no oxygen.²⁸

There is evidence from zircon magnetism indicating the planet’s geomagnetic field existed at least 4.2 billion years ago.²⁹ This early establishment coincides with genetic estimates for the age of the Last Universal Common Ancestor (LUCA)³⁰, suggesting the magnetic field provided crucial protection for early life by shielding against solar and cosmic radiation.³¹

Already at this stage early geological changes were shaping climate: as the first solid crust formed and differentiated into early landmasses, these geographical features began affecting atmospheric circulation patterns.³² ³³ Volcanic activity also wasn’t random- it was concentrated along the boundaries of the first primitive tectonic plates, creating regional variations in atmospheric composition and temperature.³⁴

Oceans, Outgassing, CO₂ Reduction
The Earth continued to cool, and the water vapour that dominated the atmosphere started to condense into liquid water and formed the first oceans between 4.0-3.5 billion years ago.³⁵ ³⁶ The bad weather continued for millennia, and much of the atmospheric carbon dioxide that the volcanoes had worked so hard to belch out earlier was dissolved in the rain, now forming carbonate compounds that were deposited as sedimentary rocks.³⁷ ³⁸ This process gradually reduced the amount of CO₂ in the air and helped stabilise Earth’s climate.³⁵ ³⁹ We got lucky here in three distinct ways:
1. We were the right distance from our star: if the planet had been too close to the Sun, the water vapour would never have condensed into liquid, and if we were farther away than we are, our water would have been ice;⁴⁰
2. Our size: Our planet was large enough to have enough gravity to hold on to all the atmosphere and water;⁴¹ ⁴² and
3. The Earth’s molten iron core: The planet has a molten iron core, and due to this we have a magnetic shield (called the “magnetosphere”) protecting us from solar wind (charged particles ejected continuously from the Sun outwards towards the planets.⁴³ ⁴⁴ Solar winds help produce the beautiful auroras our poles are famous for when they interact with our magnetosphere, but damage technology and organisms due to solar radiation. They also affect climate and weather).⁴⁵

This is also when Earth’s first stable continents were being formed, and their development was crucial for shaping climate at the time: as the earliest continental masses formed through volcanic activity and tectonic processes, they created the first true land-ocean contrasts.³⁵ ⁴⁶ These early landmasses absorbed heat differently than oceans, creating the first temperature gradients that drove primitive atmospheric circulation. The beginnings of continental drift also started affecting global heat distribution as landmasses slowly moved to different latitudes.⁴⁶

Life arrives
Around 3.8-3.5 billion years ago, the first life forms appeared in Earth’s oceans.⁴⁷ ⁴⁸ These early organisms were simple prokaryotes (bacteria and archaea) that thrived in the oxygen-free environment.⁴⁸ ⁴⁹ Many of these early life forms were anaerobic, meaning they didn’t need oxygen and actually found it toxic.³⁹ ⁵⁰ Stellar evolution models indicate that the Sun’s luminosity was approximately 25-30% lower during the Archean (3.8-2.5 billion years ago) compared to present-day.⁵¹ ⁵² Despite this “faint young Sun,” geological evidence clearly shows liquid water existed on Earth’s surface throughout this period.⁵¹ ⁵² Some climate models suggest that higher levels of greenhouse gases like CO₂ and methane could warm the early Earth. Lower planetary albedo (meaning less sunlight reflected back into space) and fewer continents would also contribute to these temperatures. Together, these factors may have kept the planet above freezing without extremely high greenhouse gas concentrations.⁵¹ ⁵²

Photosynthesis!
3.5 billion years ago, the first cyanobacteria (the Blue-Green Algae we studied in school) invented photosynthesis: i.e., they began using sunlight to make their own food, while producing oxygen as a waste product.⁵³ ⁵⁴ Initially, this oxygen didn’t accumulate in the atmosphere because it immediately reacted with dissolved iron in the oceans, forming banded iron formations (rust-coloured iron oxide deposits that we can still see in rocks today).⁵⁴ ⁵⁵ This process continued for over a billion years, slowly removing iron from the oceans while cyanobacteria continued producing oxygen.⁵⁴

At this time our planet had 17-ish hour days rather than 24-hour days: evidence from ancient banded iron formations suggests the Moon was approximately 60,000 kilometres closer to Earth 2.46 billion years ago.⁵⁶ This closer lunar proximity would have created much stronger tidal forces and more rapid precession cycles, fundamentally altering climate patterns.⁵⁷

For several million years, nearly all the oxygen being produced by the Blue-Green Algae was used up by the free oxygen molecules reacting with other chemicals on our planet or in the atmosphere. However, around 2.4 billion years ago, there was finally enough oxygen in the atmosphere that it could not all be used up in the chemical reactions, and the excess oxygen started building up in the atmosphere.⁵⁸ This critical tipping point is known as the Great Oxidation Event (GOE).⁵⁹

This is the first example of life forms fundamentally altering the planetary atmosphere, and also the first great extinction event. Oxygen was toxic to the anaerobic organisms that had dominated Earth for over a billion years, and it’s accumulation in the atmosphere caused massive die-offs.⁶⁰

Due to this catastrophe, some organisms learnt to tolerate oxygen, which was toxic to them up until this point, by creating special defence mechanisms against the poisonous effects of oxygen such as antioxidants and protective enzymes.⁶¹ ⁶² Other organisms evolved a brand new way of using oxygen- instead of just tolerating it, they started using it for a process called cellular respiration. Before oxygen, organisms had to get energy through anaerobic (meaning “without oxygen”) respiration, which yields much less energy from the same quantity of fuel: using oxygen for energy produces more than seven times more energy than anaerobic respiration.⁶³

This energy revolution resulted pivotal evolutionary advances:⁶⁴ ⁶⁵
1. Cells could now afford to be more complex because they had abundant energy to run more sophisticated machinery;⁶⁶
2. Organisms could grow larger because they had enough energy to power bigger bodies;⁶⁴ ⁶⁵ and
3. More complex behaviours and functions became possible because there was energy to spare for “luxury” activities.⁶⁷ ⁶⁸

These three points led to another evolutionary breakthrough: the evolution of eukaryotic cells (cells with a nucleus).⁶⁹ These cells had a nucleus which works as a control centre, several mitochondria (yes, that one), which works as a (yes, that ^{(mitochondria is the powerhouse of the cell)}), and organelles that all work specialised functions.

So the oxygen produced by photosynthetic organisms completely transformed Earth’s atmosphere, oceans, and even geology: it caused iron to rust out of the oceans, changed the chemistry of rocks, and created new minerals that had never existed before on Earth.⁷⁰ ⁷¹

Snowball Earth⁷² ⁷³
Some of the most extreme climate events in Earth’s history occurred during the Neoproterozoic Era (750-580 million years ago), when the planet experienced several “Snowball Earth” glaciations that covered most of its surface in ice. These events covered most of Earth’s surface in ice and represented the one of the most dramatic climate changes in planetary history. Analysis of banded iron formations from the Sturtian glaciation shows evidence for orbital forcing (which are variations in Earth’s orbit which influence the amount of solar radiation received by the Earth over time⁷⁴), with ice sheets advancing and retreating in response to changes in the planet’s orbit. This orbital control provided crucial refugia where life could survive during these extreme times.

The first migration
Around 600 million years ago, a single lineage of freshwater green algae began evolving adaptations that would eventually enable life to transition to land. These early charophyte algae lived approximately 540-520 million years ago during the early Cambrian Period approximately 540-520 million years ago during the early Cambrian Period in shallow freshwater pools and muddy banks, slowly developing resistant coatings to prevent them from drying out when water levels dropped.⁷⁵ ⁷⁶ This remarkable burst of biological innovation fundamentally transformed things: recent research indicates that only a modest increase in atmospheric oxygen around 540 million years ago was sufficient to trigger major ecological changes. The Cambrian Period featured extraordinarily high atmospheric CO₂- between 4,000 and 7,000 ppm, with some estimates peaking at 8,960 ppm. These levels produced intense greenhouse conditions: global temperatures were significantly warmer than today, sea surface temperatures were likely 10–15°C higher than today, and the planet was entirely ice-free, with no permanent polar ice sheets.⁷⁷ ⁷⁸

One of the most significant developments in this period was the widespread emergence of biomineralisation, which is the ability of organisms to produce hard shells and skeletons. The timing of biomineralisation appears linked to changing seawater chemistry during the formation of the Great Unconformity, when widespread erosion released massive quantities of calcium, iron, potassium, and silica into the oceans.⁷⁹ ⁸⁰ Another transformative evolution was bioturbation- the mixing and burrowing activities of early animals in seafloor sediments. This behaviour changed the interaction between ocean floor sediments and sea water, increased the circulation of nutrients and altered porewater chemistry.⁸¹

Around this time, as oxygen levels continued to increase, oxygen molecules high in the atmosphere continued to be split apart by the Sun’s ultraviolet radiation and recombined to form ozone (O₃).⁸² This thickened the ozone layer, a protective shield that blocks harmful UV radiation, which had been accumulating in the atmosphere since the previous 2 billion years,⁸³ but was now reaching protective capacity due to the additional free oxygen now present in the atmosphere.⁸⁴ This was another crucial planetary development: Before the ozone layer had asserted itself, UV radiation made Earth’s land surface deadly to most life forms.⁸² ⁸⁵

The ozone shield, created entirely by the oxygen from living organisms, made it possible for life to eventually colonise land around 500–470 million years ago.⁸⁶ Without life producing oxygen, there would be no ozone layer, and Earth’s surface would still be uninhabitable. Around 470-485 million years ago,⁸⁶ the first true land plants (called embryophytes) made their appearance. These early pioneers were tiny, simple organisms that looked more like green carpets than modern plants,⁸⁷ and due to this primitive rug oxygen levels started rising again as land-based photosynthesis added to marine oxygen production, and as these plants and organic matter started breaking down rock surfaces, and atmospheric CO₂ started dropping due to photosynthesis (which uses CO₂ as fuel).⁸⁸ ⁸⁹

When plants colonised land, they created another major feedback loop with the atmosphere. Land plants dramatically increased oxygen production through photosynthesis while simultaneously removing carbon dioxide from the air. In time, forests became massive carbon storage systems, locking CO₂ in wood and soil.⁸⁸ ⁸⁹ The rise of plants also affected Earth’s planetary energy balance because green vegetation reflects less sunlight than bare rock, changing Earth’s albedo (reflectivity, with a value between 0 and 1; a high albedo means more light is reflected by the planet or surface in question into space, while a low albedo means more light is absorbed. For example, Earth’s albedo is about 0.31, reflecting approximately 31% of the solar radiation it receives) and affecting global temperature.⁹⁰

Meanwhile between 485-443 million years ago, throughout the Ordovician Period, the most significant and sustained diversification of marine life in Earth’s history occurred, fundamentally transforming oceanic ecosystems.⁹¹ This extraordinary evolutionary radiation lasted nearly 42 million years and represented a fundamental shift from the simple post-Cambrian fauna to complex, multi-tiered marine ecosystems.⁹¹ This is called the Great Ordovician Biodiversification Event (GOBE), and is our planet’s greatest marine evolutionary revolution.⁹¹ Unlike the rapid burst of the Cambrian Explosion, GOBE was a sustained, long-term adaptive radiation that occurred at different times across different regions, driven by the unique paleogeographic configuration of the Ordovician world. Ordovician phytoplankton diversity reached approximately 400 species,^⁹² the highest levels of the entire Paleozoic, which had profound effects on Earth’s carbon cycle and atmospheric composition through enhanced photosynthesis. This contributed significantly to rising atmospheric oxygen levels and increased organic matter production and burial thereby helping draw down atmospheric CO₂, contributing to global cooling trends.⁹² ⁹³

It is thought that the late Cambrian Steptoean Positive Carbon Isotope Excursion (SPICE) around 500 million years ago which triggered a major atmospheric oxygen increase from 10-18% to 20-28%.⁹⁴ ⁹⁵ ⁹⁶ Full ocean oxygenation to modern levels didn’t occur until approximately 521 million years ago (deep waters remained largely oxygen-poor until around 400 million years ago), and may have played a significant role in GOBE specie diversification and population explosion.⁹³ ⁹⁶

Around 430-450 million years ago (land) plants evolved vascular systems-internal “plumbing” that could transport water and nutrients throughout the plant.⁹⁷ Vascular plants could extend deeper into soils with primitive root systems, accelerating the chemical breakdown of rocks and removing more CO₂ from the atmosphere. This led to plant roots and acids creating the first recognisable soils, fundamentally changing land surface chemistry. Atmospheric CO₂ continued declining as more efficient photosynthesis spread across larger land areas.⁸⁸

Devonian through Carboniferous
Between 419-358 million years ago, called the Devonian Period, true roots evolved,⁹⁸ so plants could now anchor themselves firmly and access deep water and nutrients, trees evolved,⁹⁹p the first seeds evolved¹⁰⁰, and stomata (tiny pores that allow plants to exchange gases) evolved¹⁰¹. This led to a drop in atmospheric CO₂ from 4,000 ppm¹⁰² (parts per million) to around 1,000 ppm¹⁰³ ¹⁰⁴ as vast new forests absorbed carbon. Oxygen levels soared, rising from about 15% to 21%,¹⁰⁵ as forest photosynthesis accelerated, and the first deep, complex soils formed as tree roots penetrated far into bedrock. Tree roots produced organic acids that dramatically increased rock dissolution rates, removing even more CO₂.¹⁰³

The Carboniferous period came next (358-298 million years ago) and was named for the massive coal deposits formed during this time.¹⁰⁶ ¹⁰⁷ This period saw the formation of Earth’s first massive forest ecosystems: seed plants diversified, some trees grew to heights of more than 40 metres, and tree ferns dominated swampy lands. During this period atmospheric CO₂ crashed to 300 ppm.¹⁰⁸ ¹⁰⁹ This was lower than pre-industrial levels (which were around 280 ppm) which triggered the beginning of a major ice age (because CO₂ is a green house gas- it traps heat like a figurative blanket, and if your blanket is thin during winter, you will likely freeze), oxygen levels rose to 35% (compared to today’s 21%), so high that even damp wood could ignite.¹⁰⁵ ¹⁰⁷

Pangaea & Climate Shifts
While the above was happening, 305 million years ago, climate became drier and cooler, causing the “rainforest collapse.”¹¹⁰ This crisis favoured seed plants over spore-bearing plants, fundamentally changing forest composition.¹¹⁰ At the same time (around 300 million years ago), all continents were joined in a supercontinent called Pangaea, and a single massive ocean (Panthalassa) surrounded Pangaea, creating very different heat distribution patterns than today’s multiple ocean basins.¹¹⁰ This massive landmass had profoundly different climate to what we have now. With most land far from moderating ocean influences, the interiors experienced extreme temperature variations and reduced rainfall. Ancient glacial deposits found across today’s southern continents (including India and Australia) demonstrate they were once clustered around the South Pole when they were part of Gondwana (southern Pangaea).¹¹⁰ ¹¹¹

Over the past 540 million years, Earth’s magnetic field strength and atmospheric oxygen levels have correlated strongly. Both peaked between 330 and 220 million years ago and have exhibited remarkably similar patterns throughout the Phanerozoic Eon, suggesting connections between deep Earth processes and surface conditions.¹¹² ¹¹³ ¹¹⁴

Permian-Triassic Mass Extinction¹¹⁵ ¹¹⁶
The Permian–Triassic boundary (252 million years ago) marks Earth’s largest mass extinction, offering insights into how extreme environmental changes can affect life. Atmospheric CO₂ concentrations increased six-fold from approximately 426 ppm to 2,507 ppm within about 75,000 years, primarily due to massive volcanism from the Siberian Traps. These eruptions released approximately 36,000 gigatons of carbon into the atmosphere.¹⁰⁸ The resulting greenhouse effect raised global temperatures by about 10°C and dramatically lowered ocean pH. These conditions eliminated nearly 96% of marine species and about 70% of terrestrial vertebrates.¹⁰⁸

Angiosperm evolution
Beginning around 200 million years ago,¹⁰⁹ Pangaea broke apart into modern continents, forming new oceans, altering heat distribution, and changing global climate patterns. The evolution of flowering plants (angiosperms) during the Cretaceous Period (145-66 million years ago) represents the most recent major plant revolution.¹¹⁰ The breakup of Pangea eliminated the vast desert belts that had dominated Pangaea, replacing them with humid temperate zones¹¹¹ ideal for plant growth¹¹² ¹¹³ and created numerous smaller landmasses and archipelagos,¹¹¹ ¹¹⁴ providing isolated environments perfect for rapid speciation,¹¹⁵ and the creation of the new climactic zones created diverse climate conditions that encouraged angiosperm diversification.¹¹⁶

Mid Cretaceous (100-94 million years ago) sea levels were 100-200 metres higher than today,¹¹⁷ creating extensive coastal wetlands and island systems. The period witnessed high CO₂ levels (up to 1,500 ppm)¹¹⁸ ¹¹⁹ providing abundant carbon for photosynthesis, and warm, humid conditions with minimal temperature gradients between the poles and and the equator.¹¹⁷ ¹¹⁸ All of this favoured plant growth, and contributed to explosive angiosperm diversification (called the “Mid-Cretaceous Angiosperm Radiation”).¹²⁰ ¹²¹ Flowering plants spread from wetlands to floodplains, then to coastal areas¹²¹ and eventually to most terrestrial environments, and some plants evolved into the ancestors of plants we have today (such as orchids, mints, magnolias).¹²² ¹²³ ¹²⁴

By the late Cretaceous (100.5 to 66 million years ago), angiosperms had become dominant in most terrestrial ecosystems.¹²⁰ ¹²⁵ Angiosperm expansion contributed to oxygen level changes, though not as dramatically as earlier plant evolutions, as well as more efficient photosynthesis and rapid turnover rates increased carbon cycling between the atmosphere and the biosphere. Bees, butterflies, and many other pollinating insects, as well as birds evolved alongside flowering plants at this time.¹²⁶ ¹²⁷ New plant tissues and chemicals drove the evolution of specialised plant-eating insects, and this plant-insect coevolution created much more complex terrestrial food webs. This also affected the lives of early mammals (some of our earliest ancestors had arrived, yay!) which evolved to exploit angiosperm fruits, nectar, and the insects they supported.¹²⁶ ¹²⁸ ¹²⁹ ¹³⁰ ¹³¹ ¹³² ¹³³

Grasses
Early grasses evolved around 65-70 million years ago,¹³⁴ and were mainly shade-tolerant species that lived under forest canopies, and used C3 photosynthesis (C3 Photosynthesis is the typical pathway in most plants). C4 photosynthesis evolved around 35 million years ago during the Oligocene and is used by plants like corn and sugarcane to minimize photorespiration.¹³⁴ ¹³⁵ Photospiration is a light-dependent plant process that consumes oxygen and releases carbon dioxide which is more efficient in hot environments. It acts as a counter-process to photosynthesis, and improves plant efficiency in hot environments.¹³⁴ ¹³⁵ C4 photosynthesis evolved over 60 times independently in grasses.¹³⁶

Extraterrestrial visitor
The Cretaceous-Paleogene (K-Pg) extinction event happened 66 million years ago, and is one of the most dramatic and well-documented climate and ecological catastrophes in Earth’s history.¹³⁷ A massive asteroid approximately 10-15 kilometres in diametre struck the Yucatán Peninsula in Mexico, creating the 180 kilometre wide Chicxulub crater.¹³⁸ This impact occurred precisely at 66.043 ± 0.043 million years ago, and eliminated approximately 75% of all species on Earth, including non-avian dinosaurs, and fundamentally reshaped the planet’s climate, atmosphere, and ecosystems.¹³⁹ ¹⁴⁰ ¹⁴¹

The asteroid impact created temperatures hot enough to ignite vegetation globally for the first hours after the event.¹⁴² ¹⁴³ Evidence suggests 15,000-70,000 teragrams (1 teragram is 1,000,000,000,000 grams, or 383,523,886,956.52 tsp of all purpose flour for our bakers) of soot¹⁴⁴ was injected into the atmosphere from burning biomass and hydrocarbons and massive amounts of pulverized rock were ejected into the stratosphere. These events eventually led to soot and dust particles blocking 50-90% of sunlight from reaching the Earth’s surface, causing a planetary twilight lasting 1-2 years which then caused food webs to collapse due to unavailability of sunlight for photosynthesis.¹⁴⁵ ¹⁴⁶ Global average temperatures dropped by 7-28°C on land and 11°C in oceans: mid-to-high latitudes experienced more severe cooling than tropical regions, and temperatures remained below freezing for at least 3 years in many regions.¹⁴⁴ ¹⁴⁵ Ocean cooling persisted for decades after the impact, affecting ocean circulation.¹⁴⁴ ¹⁴⁵

The impact also vaporised 67 ± 39¹³⁷ Gigatonnes of sulphur from gypsum-rich target rocks (Pure gypsum (calcium sulfate dihydrate) contains about 18.5% to 18.6% sulphur by weight. However, agricultural-grade gypsum typically has other impurities and may contain a slightly lower percentage of sulphur, often in the range of 13% to 17% depending on the source¹⁴⁷). This led to the formation of aerosols in the stratosphere, creating acid rain and further cooling. sulphur aerosols persisted for 10+ years longer than dust particles.¹⁴⁸

Simultaneously, stratospheric heating from soot absorption caused extreme ozone layer depletion, and the ¹⁴⁵ release of nitrogen oxides and other compounds created a toxic atmosphere.¹⁴⁵ Sulphuric, nitric, and carbonic acid rain acidified land and freshwater, due to which ocean pH decreased by 0.25 units within 100-1,000 years after impact, leading to acidic conditions dissolving the shells and skeletons of marine organisms.¹⁴⁵ Overall land precipitation decreased by over 85% in the months following impact, and tropical areas experienced severe drought while maintaining milder cooling.¹⁴⁴ Normal precipitation patterns took more than 10 years to reestablish.¹⁴⁴

This event devastated oceanic and terrestrial ecosystems: most living beings were killed,¹⁴⁰ ¹⁴⁵ and those that lived had few ways to find or make food.

Deccan volcanism
Coincident with the impact, the Deccan Traps in present day western India were experiencing one of the largest volcanic eruptions in Earth’s history.¹⁴⁹ ¹⁵⁰ These eruptions created lava flows over 2 kilometres¹⁵¹ thick covering an area larger than modern France (There is some controversy about the timing, but it is thought that most intense eruptions occurred within ~250,000 years¹⁵² of the boundary, and some evidence suggests the Chicxulub impact may have triggered intensified Deccan volcanism¹⁵⁰ ¹⁵³). Due to these eruptions, volcanic sulphur dioxide was released into the air creating aerosols that temporarily cooled climate and volcanic ash blocked sunlight to an extent, these eruptions also released enormous amounts of CO₂. Some sources saying it could have caused 2-8°C¹⁵⁴ warming in some regions, while others peg the warming at a much lower level.¹⁵⁵ However, unlike the impact cooling caused by the asteroid, the volcanic warming persisted for thousands of years,¹⁵⁶ ¹⁵⁷ and also contributed to ocean acidification before and after the impact due to the release of sulphur, chlorine, and other toxic gases into the air which dissolved in rain.¹⁵⁸ ¹⁵⁹ ¹⁶⁰

Climate began recovering within 10-30 years of impact,¹⁶¹ helped on by the Deccan CO₂ emissions. Hydrological cycles took a few decades to recover.¹⁴⁰ ¹⁴⁴ Life eventually snapped back.¹⁶² ¹⁶²

While there are several evolutionary consequences of the impact, the extinction of dinosaurs allowed mammals to diversify and eventually dominate terrestrial ecosystems (yay, us!).¹⁶³ Angiosperms filled many ecological niches left vacant by extinct plant groups: currently approximately 300,000 of the world’s 400,000 plant species are angiosperms.¹⁶⁴ The K-Pg event marked the beginning of modern Cenozoic ecosystems.¹⁶⁵

Paleocene–Eocene Thermal Maximum (PETM)
The Paleocene–Eocene Thermal Maximum (PETM) was a brief but extreme global warming event that occurred about 56 million years ago, marking one of the fastest natural climate shifts in Earth’s history.¹⁶⁶ Roughly 2,000–7,000 gigatons of carbon (as CO₂ and methane) were injected into the atmosphere and oceans over 2,000–20,000 years,¹⁶⁷ likely from volcanic activity and the destabilisation of deep-sea methane hydrates.¹⁶⁸ Global average temperatures rose by 5–8 °C and remained elevated for 170,000-220,000 years,¹⁶⁹ profoundly warming both land and sea surfaces.

The extra CO₂ made oceans more acidic, leading to rapid extinctions among marine microorganisms like foraminifera.¹⁷⁰ But on land, forests expanded poleward,¹⁷¹ animal-pollinated flowers became much more common (insects and early mammals co-evolved), forest diversity exploded as new climate zones opened up, and plants could suddenly grow in previously impossible places.¹²⁰ ¹⁷⁵

Mammal groups underwent evolutionary bursts as new niches opened up: primates (ancestors’ alert!) spread from Asia to Europe to North America for the first time, even-toed ungulates (ancestors of deer, pigs, cows) emerged, and odd-toed ungulates (ancestors of horses, rhinos, tapirs) punched in their evolutionary attendance as well.¹⁷² ¹⁷³ This is also when mammals became smaller due to heat stress and lower-quality plant nutrition from high CO₂, and several species went extinct as per available fossil records.¹⁷⁰ ¹⁷⁴

The PETM wasn’t isolated- it was followed by ETM2, H1, H2, and other “hyperthermals” that collectively created the Early Eocene Climate Optimum, the warmest period of the last 65 million years. Recovery from this level of warming took over 200,000 years.¹⁶⁹ ¹⁷⁶

Eocene and Himalayas
The Early Eocene period from 52 to 50 million years ago had global mean temperatures of ~30°C (compared to ~15°C today).¹⁷⁷ Antarctica and Greenland were completely ice-free with subtropical forests (fossil evidence shows crocodiles and palm trees in Arctic regions, tropical mollusks and sharks found in Alaska and Norwegian Arctic, and modern mammals expanded around the planet).¹⁷⁷ ¹⁷⁸ ¹⁷⁹ ¹⁸⁰ ¹⁸¹ Atmospheric CO₂ levels remained above 800 ppm, more than double pre-industrial levels.¹⁸²

While this was happening, around 50 million years ago,¹⁸³ the Indian subcontinent plate started crashing into what we now call Asia (the Eurasian plate) after drifting up from near Antarctica,¹⁸⁴ thus raising the mighty Himalayas and closing the Tethys Sea ¹⁸⁴ (an ancient ocean between India and Asia, 50-15 million years ago).¹⁸⁴ ¹⁸⁵ ¹⁸⁶ This had several profound climactic effects:
1. The rising Himalayas (50-15 million years ago) created a massive topographic barrier that blocked winter winds from Siberia¹⁸⁷ and channeled warm, moist air from the Indian Ocean creating the Asian monsoon system that now affects billions of people;¹⁸⁸
2. The Tibetan Plateau acts as a “giant attractor of fresh water” in the Northern Hemisphere, fundamentally altering global precipitation patterns and ocean circulation;¹⁸⁹
3. It helped shut down deep water formation in the Pacific while enhancing it in the Atlantic, contributing to our current global ocean circulation pattern;¹⁹⁰ and
4. The massive amounts of fresh rock exposed by Himalayan uplift increased chemical weathering rates, removing more CO₂ from the atmosphere and contributing to global cooling over millions of years.¹⁹¹ ¹⁹²

The closure of the Tethys Sea also had pivotal consequences for planetary climate:
1. The Tethys Sea had allowed warm water to flow from the Atlantic to the Indian Ocean. Its closure forced major reorganization of global ocean currents;¹⁹³ ¹⁹⁴
2. As the Tethys closed, the Mediterranean Sea formed as a remnant, fundamentally changing European and North African climate;¹⁹⁵ and
3. Tethys closure helped intensify the Asian monsoon by creating stronger temperature contrasts between land and sea (since there was now no water mass between the Eurasian plate and the Indian plate).¹⁹⁶ ¹⁹⁷

Drake Passage, Antarctic isolation, and grass 2.0
While all this was happening, the separation of South America from Antarctica created the Drake Passage between 40 and 30 million years ago.¹⁹⁸ When this passage opened, it allowed the formation of the Antarctic Circumpolar Current- the world’s largest ocean current that now transports between 130 million cubic metres¹⁹⁸ to 173 million cubic metres¹⁹⁹ of water per second around Antarctica. This isolated Antarctica from warm ocean water flowing south, leading to its rapid glaciation and the formation of permanent ice sheets.²⁰⁰ These events contributed to the major global cooling that occurred between 33-34 million years ago, ending the warm Eocene period, altered global ocean heat transport, and altered climate worldwide.¹⁹⁸ ²⁰⁰

The expansion of grasslands helped draw down atmospheric CO₂ during the late Miocene (23.03 to 5.33 million years ago) to help cool the planet again by promoting widespread chemical weathering through plant roots, which drew down CO₂ and facilitated global cooling.²⁰¹ ²⁰² This process was driven by geological factors like the uplift of mountain ranges (such as the Himalayas), that changed land configurations, and climate patterns that created open, arid, and seasonally dry environments ideal for grassland proliferation,²⁰³ ²⁰⁴ ultimately reinforcing climate feedbacks that further decreased greenhouse gases and enhanced cooling.²⁰⁵ Once again, changes in vegetation patterns changed our planet’s climate.²⁰⁶

Later, the rise of the Isthmus of Panama (between 15 and 3 million years ago) was one of the most climate-altering geological events in recent Earth history by cutting off deep water exchange between the Atlantic and Pacific was cut off by 9.2 million years ago²⁰⁷ (shallow water exchange continued until about 3 million years ago²⁰⁷). This created the modern Gulf Stream that keeps northwestern Europe 10°C warmer than it would otherwise be,²⁰⁸ ²⁰⁹ made the Atlantic saltier (because trade winds carried moisture from the Atlantic to the Pacific, increasing evaporation in the Atlantic which helped drive the formation of modern deep water circulation in the North Atlantic),²⁰⁷ and contributed to the glaciation of the North by providing the moisture needed for glacier formation.²⁰⁸

Grasses 3.0
While early C4 grasses were restricted to open, disturbed habitats with high light and temperature, by 8-4 million years ago²⁰⁴ they had expanded globally. Due to drying climate at this time trees that evolved in humid, wet weather conditions found difficult to hold on to areas they had earlier conquered.²⁰⁴ ²⁰⁹ So grasses went from minor components of ecosystems to dominating vast landscapes: savannas, prairies, and steppes as we know them formed during this period. This concurrently created entirely new ecosystems that significantly transformed regional climates and atmospheric conditions by promoting open areas with sparse vegetation. These changes altered albedo (how much light the planet is reflecting back into space, and grasslands have highly variable albedo- dark green during wet seasons, light brown/yellow during dry seasons),²¹⁰ ²¹¹ increased evapotranspiration (the total process by which water moves from the land surface and plants into the atmosphere, combining evaporation from soil and water bodies with transpiration from plants),²¹² and influenced local and global climate patterns.

Grasslands create fire-climate feedbacks because they create continuous fine fuel that burns easily,²¹³ increasing fire frequency from once per century to every 1-3 years.²¹⁴ When burning, they produce smoke and particles that can cool regional climate by blocking sunlight, but grasses also re-grow within weeks of burning,²¹³ quickly restoring carbon uptake. Fire-climate interactions also help grasslands expand, since fire kills off forests, but as mentioned, grass has the advantage over trees since it can regrow quickly in those previously forested areas.²¹⁵

Grasslands store 80-90% of their carbon underground in massive root systems,²¹⁶ compared to trees that store most carbon aboveground, which means if there is a fire above ground, the underground carbon storage won’t be destroyed. Later, grassland-supported herbivores became major methane producers, adding an interesting layer to the workings of grasslands as greenhouse gas stores.²¹⁷ Atmospheric CO₂, already lower than in ancient times, was further drawn down: grasslands, soil formation, and slower growth of woody plants reduced the amount of carbon being released back to air.²¹¹ ²¹⁸

Ice age intensification
2.6 million years ago, our planet crossed a threshold: the climate cooled enough for glaciers to form.²¹⁹ The planet entered the Pleistocene epoch, defined by cycles:²¹⁹ cold glacials (big ice sheets advancing) and warmer interglacials (ice retreating), repeatedly, in roughly 40,000‑year cycles.²¹⁹ ²²⁰ The cycling between cold and warmth in long glacial-interglacial rhythms were driven by subtle changes in Earth’s orbit (Milankovitch cycles).²²⁰ These rhythms controlled how much sunlight different parts of the planet received, and with them came massive atmospheric and ecological changes.²²¹ ²²²

These ice sheets locked up huge amounts of water and also reflected a lot of sunlight (ice has high albedo) which meant less solar heating of Earth’s surface, leading to lower sea levels, ecosystem retreat (due to cold weather), and the retreat of high-latitude forests areas (tundra and steppe replaced them).²²³ ²²⁴ ²²⁵ ²²⁶ Animal life in the cold areas either adapted to the frigid weather (for example by developing thick fur),²²⁷ ²²⁸ or moved to warmer locations.²²⁷ ²²⁹ Plant communities also shifted poleward or downslope, depending on latitude and geography.²²⁹ ²³⁰ Meanwhile, atmospheric CO₂ levels fluctuated: during glacial periods CO₂ dropped²³¹ (as colder oceans hold more CO₂, fewer plants ²³² in cold areas which meant more ice reflecting the Sun’s heat and light into space, etc.), then rose in interglacials.

The Mid‑Pleistocene Transition (~1.2 to 0.7 million years ago)
The glacial cycle now expanded to roughly 80‑ 100,000 years²³³ from the previous approximately 40,000 year cycles. It is thought that there were multiple interacting factors that over time caused ice sheets to grow larger and last longer, which contributed to a cooler planet.²³¹ Cooler global temperatures meant CO₂ drawdowns during glacials were deeper,²³¹ and ecosystems had to cope with even longer cold periods. With bigger ice sheets, land that had been vegetated became barren under ice, further reducing photosynthesis and raising local albedo, all amplifying cooling.²³²

Homo Sapiens
300,000 years ago the planet was in the grips of a glacial period. Vast ice sheets covered much of the Northern Hemisphere, stretching down over what is now Canada, northern Europe, and Russia.²³⁴ Sea levels were over 100 metres lower than today- so much water was locked in ice that entire land bridges emerged: Siberia connected to Alaska, Australia was linked to New Guinea, and the British Isles were part of mainland Europe.²³⁴ Forests shrank, pushed back by advancing ice or cold, dry air. Grasslands, steppe, and tundra spread. Deserts expanded in some regions, while other regions were cooler and wetter.²³⁴ ²³⁵ Dust from dry landscapes filled the air, carried by powerful winds into the atmosphere, affecting solar reflection and local climate. The planet was dry, windy, and colder by around 5-8°C on average compared to today.²³⁴ ²³⁵ Atmospheric CO₂ levels hovered around 180-200 ppm, far lower than modern concentrations.²³⁴ ²³⁵

These are the conditions that birthed our first recognisably human ancestors.²³⁶ ²³⁷

Several hominin species were alive at the time, and we persisted through the frequent freezes, as well as brief warm intervals like the Eemian (130,000 to 115,000 years ago). During the Eemian, the ice retreated, CO₂ rose to approximately 280-300 ppm, forests expanded again into higher latitudes, and savannas and wetlands bloomed across parts of Africa and Eurasia.²³⁵ ²³⁸ These were golden times for human evolution: food sources diversified,²³⁹ ²⁴⁰ migration became easier (remember, lots of land bridges were still available),²⁴¹ and new ecological niches²⁴² opened up, and our ancestors left our original home in Africa and started colonising our planet 100,000 to 70,000 years ago.²⁴³ ²⁴⁴ Along the way, they encountered different biomes (a distinct geographical region with specific climate, vegetation, and animal life): such as forests, deserts, coasts, grasslands, and adapted to each with tools, social cooperation, and eventually, fire.²⁴² ²⁴⁵

Fire
Fire was the first way hominins exerted any control over the atmosphere.²⁴⁶ Controlled burning is among the oldest forms of ecological management. Early Homo sapiens and even earlier hominins like Homo erectus and Neanderthals used fire not just for warmth or cooking, but likely to clear land, encourage new growth, or drive animals.²⁴⁶ By setting fires, they released stored carbon in vegetation back into the atmosphere as CO₂.²⁴⁶ While these emissions were small compared to modern levels, over tens of thousands of years they changed regional vegetation patterns, created more open savanna-like landscapes, and influenced albedo (burned land reflects differently than dense forest).²⁴⁶ This fire-land-atmosphere feedback was the beginning of human involvement in biogeochemical cycles.²⁴⁶

Ecosystem Engineering
Homo sapiens spread into Europe and Asia (by about 70,000– 50,000 years ago),²⁴⁷ and immediately started redecorating the landscape. They entered terrain with healthy populations of megafauna such as woolly mammoths, giant ground sloths, cave bears, mastodons, all ecosystem engineers in their own right that kept forests open, trampled plants, redistributed nutrients²⁴⁸ ²⁴⁹ until hominins hunted them down to nothing.²⁵⁰ The decline of megafauna had major ecological and atmospheric consequences:
1. Fewer grazers meant that open ecosystems like steppe and savanna could revert to denser forests, drawing down more CO₂ (however, in other regions human fire regimes maintained grasslands, potentially stabilising CO₂ through fire-vegetation balance).²⁴⁶ ²⁵¹ ²⁵²
2. Loss of large herbivores reduced methane emissions (methane is a potent greenhouse gas).²⁵³

This shifting mosaic of forest, grassland, wetland, and desert reshaped the carbon cycle on a continental scale even before agriculture began.²⁴⁹ ²⁵¹ ²⁵³ ²⁵⁴

Laschamps Magnetic Excursion
The most recent example of magnetic field impacts on climate and ecology occurred during the Laschamps excursion 42,000-41,000 years ago.²⁵⁵ ²⁵⁶ During this brief magnetic reversal, the field strength dropped to only 6% of its current value during the transition period.²⁵⁵ ²⁵⁶ This magnetic weakening correlated with:
1. Sudden climate cooling recorded in sediment and ice core records globally;²⁵⁷
2. Megafauna extinctions, including woolly mammoths and giant Australian marsupials;²⁵⁷
3. Changes in human behaviour including increased use of caves and red ochre (possibly as sunscreen);²⁵⁶ and
4. Ozone depletion which allowed increased cosmic radiation to reach Earth’s surface.²⁵⁵

The Last Glacial Maximum
The Earth descended into its last major glacial phase between 26,500 to 19,000 years ago.²⁵⁸ Once again ice sheets locked up water, and covered vast areas of the northern hemisphere,²⁵⁸ sea levels dropped,²⁵⁹ and atmospheric CO₂ bottomed out at around 180 ppm while methane fell to 350–400 ppb.²⁶⁰ ²⁶¹ These greenhouse gas levels were among the lowest in millions of years.²⁶⁰ ²⁶¹ Human populations during this time survived in isolated refuges, like parts of southern Europe, Africa, and Asia.²⁶² ²⁶³ ²⁶⁴ But they continued to hunt, migrate, and use fire, and these interactions shaped the ecosystems they worked with.²⁴⁶ ²⁶⁵ In some areas, especially Australia, the combination of fire and human hunting dramatically changed plant communities and may have contributed to extinction of large marsupials.²⁶⁶ ²⁶⁷

Holocene
Between 19,000 and 11,700 years ago, the Earth began transitioning out of the icy grip of the glacial period once again.²⁶⁸ Glaciers melted, CO₂ began to rise naturally (due to warmer seas, lesser albedo, more vegetation, thawing soil) from around 180 to 260 ppm.²⁶⁹ ²⁷⁰ This warming triggered profound changes:
1. Sea levels rose by over 120 metres, redrawing coastlines;²⁷¹
2. Forests reclaimed northern latitudes as tundra and ice receded;²⁷²
3. Wetlands expanded, becoming methane sources;²⁷³ and
4. Animals and plants shifted ranges dramatically- some followed the climate northward; others were stranded.²⁷⁴ ²⁷⁵

For the first time in over 100,000 years, humans experienced a world with reliably warm temperatures, regular rainfall, and stable sea levels.²⁶⁹ ²⁷⁶ This period was not just a reprieve from glacial chaos: it was the cradle of civilisation.²⁶⁹ ²⁷⁶ The Holocene (named after the Greek words for “entirely recent.”²⁷⁷ ²⁷⁸) gave humans everything they needed to shift from a mobile, foraging species to sedentary builders of complex societies.²⁷⁹ ²⁸⁰ ²⁸¹ We began to shift the biosphere, and the atmosphere shifted with us.²⁸²

Agriculture
Humans had been domesticating plants and animals in small ways for thousands of years before the Holocene, but around 9,000–10,000 years ago, the process accelerated and spread across multiple regions nearly simultaneously.²⁸³ ²⁸⁴ In the Fertile Crescent, people began cultivating wheat, barley, and legumes. In China, rice and millet. In India, wheat, barley, and rice. In the Americas, maize, squash, and potatoes. In Africa, sorghum and yams.²⁸⁵ ²⁸⁶

Our earliest agriculturist ancestors cleared forests to plant crops, often using fire- thus releasing CO₂ into the atmosphere. They also tilled soil, exposing carbon-rich topsoil to oxygen, further increasing emissions. Further, as irrigation and livestock practices developed, they emitted methane, a more potent (though shorter-lived) greenhouse gas.²⁸⁷ ²⁸⁸ ²⁸⁹ By some estimates, early farmers increased atmospheric methane by enough to delay the next ice age.²⁹⁰ ²⁹¹ William Ruddiman’s “Early Anthropogenic Hypothesis” suggests that without early agriculture, Earth’s natural orbital cycles might have sent us sliding into another glaciation by now.²⁹⁰

Civilisation
As agriculture spread, forests fell across Mesopotamia, the Indus Valley, Egypt, China, and Mesoamerica.²⁹² ²⁹³ Wetlands were drained.²⁹² Terraces were carved into mountains.²⁹² ²⁹³ Rivers were redirected.²⁹² ²⁹³ Every alteration changed local climate and hydrology, and increasingly, the global atmosphere.²⁹² ²⁹³ By around 5,000 years ago, large-scale civilisations were flourishing: the Sumerians in Mesopotamia, the Harappans in the Indus Valley, dynastic Egypt, and the early Chinese states.²⁹⁴ ²⁹⁵ ²⁹⁶ ²⁹⁷ ²⁹⁸ These societies built cities, roads, irrigation systems, and often concentrated millions of people in tightly packed regions, relying on surrounding land to feed them.²⁹⁴ ²⁹⁵ ²⁹⁶ ²⁹⁷ ²⁹⁸

With increasing population came a growing demand for timber, grazing land, and even more land for crop farming.²⁹⁹ Every hectare converted from wildland to farmland shifted the carbon budget of the Earth. By 2,000 BCE, the cumulative effects were measurable in the ice core records: atmospheric CO₂ began creeping upward again, alongside methane.³⁰⁰ ³⁰¹

Collapse
At this time, human societies were entirely dependent on the planet’s bounty, and its moods. Around 2,200 BCE a sudden drying period affected the Middle East, India, and parts of Africa.³⁰² ³⁰³ ³⁰⁴ Crop failures and societal strain may have helped collapse the Akkadian Empire, disrupted the Indus Valley Civilisation, and weakened Old Kingdom Egypt. The Mycenaeans, Hittites, and other Eastern Mediterranean powers fell together around 1,200 BCE due to what are thought to be volcanic eruptions, droughts, and migration pressures.³⁰² ³⁰³ ³⁰⁴ Three massive volcanic eruptions (536, 540, and 547 CE), contributed to global cooling, failed harvests, and pandemics.³⁰⁵ ³⁰⁶ Tree ring records and ice cores show a drop in temperatures of 1-2°C globally.³⁰⁷ ³⁰⁸ Famine, migration, and disease followed.³⁰⁹ ³¹⁰

By around 1,000 CE, the cumulative impact of human land use was enormous: half of Europe’s original forests were gone, Asian rice agriculture had become a major methane source, pastoralism spread across Central Asia, North Africa, and the Andes, and indigenous Americans managed landscapes on a continental scale through fire, terracing, and irrigation.³¹¹ ³¹² This was a warmer period, known as the Medieval Warm Period (950– 1250 CE), temperatures in some regions (especially Europe) rose modestly.³¹³ This led to population booms in China and Europe, longer growing seasons, and even encouraged the Viking expansion to Greenland.³¹³ ³¹⁴

But the Earth’s climate system remained dynamic: we once again had a cooler period, now named the Little Ice Age (1300– 1850 CE), possibly linked to solar minima, increased volcanic activity, and a slight dip in CO₂ and methane levels- partly due to reforestation after pandemics (e.g., the Black Death) reduced human populations.³¹⁵ ³¹⁶ ³¹⁷ Glaciers advanced,³¹⁸ winters became harsher,³¹⁹ ³²⁰ European rivers like the Thames froze,³²¹ and crops failed more often.³²²

Coal
Beginning around 1750 CE, the Industrial Revolution marked humanity’s first major leap from regional to global atmospheric influence.³²³ this period fundamentally altered the relationship between human society and Earth’s atmosphere through the large-scale burning of fossil fuels.³²³ The shift to steam-powered manufacturing created the first truly industrial cities.³²³ Places like Manchester, Birmingham, and Glasgow became centres of coal-burning factories that blackened skies with soot and smoke.³²⁴ By the first half of the 19th century, manufacturing contributed over 30% of GDP in early industrializing countries like Britain and Belgium.³²⁴ Steam engines weren’t just for factories- they powered the first steamships (1807)³²⁵ and railways (1825).³²⁶ These transportation networks built using coal-smelted iron and steel created a feedback loop: more coal was needed to power the very systems that moved coal around the world.³²⁶ ³²⁷ ²²⁸ ³²⁹

The era is documented visually by artists like Claude Monet, along with other pioneering artists like J.M.W. Turner, who painted the smoke, haze, and atmospheric changes brought by the Industrial Revolution. Recent scientific studies have revealed that the hazy, dreamlike quality of many Impressionist paintings is a faithful rendering of the actual air pollution these artists experienced in cities like London and Paris during the 19th and early 20th centuries.³³⁰ ³³¹ ³³² Interestingly, as sulphur dioxide and particulate pollution increased during the Industrial Revolution, the contrast in Monet’s paintings dropped and his palette shifted toward paler, hazier colours.³³⁰ ³³³ This trend closely matched real rises in air pollution;³³⁴ ³³⁵ Monet and Turner literally painted what they saw. The result is an atmospheric “polluted realism”. The diffuse, foggy quality of many Impressionist masterpieces provides a unique artistic record of environmental change that complements scientific air quality data from the era.

The widespread use of coal led to the first anthropogenic air pollution on an industrial scale.³³⁴ ³³⁵ Urban areas developed thick smog, rivers became dumping grounds for industrial waste, and forests were cleared for fuel and construction.³³⁴ ³³⁵ While the environmental impacts were initially local, the atmospheric effects were beginning to accumulate globally.³³⁵ By 1850, atmospheric CO₂ had risen from pre-industrial levels of 275 ppm to approximately 285 ppm- a seemingly small increase that represented the beginning of exponential growth.³³⁶ ³³⁷ Methane levels also started rising from pre-industrial levels of around 722 parts per billion (ppb).³³⁸ Earth’s average surface temperature began its upward trajectory during this period, warming by approximately 0.1-0.2°C by 1850.³³⁹ ³⁴⁰

This early warming was subtle compared to later changes, but it marked the end of the natural climate variability that had characterized the Holocene.

Electricity
The late 19th century brought two revolutionary technologies: electricity and the internal combustion engine. By 1909, 23% of industrial power was generated by electrical motors; by 1929, this had soared to 77%.³⁴¹ ³⁴²

Meanwhile, Rudolf Diesel’s engine (1897) and the Ford Motor Company (1903) launched the automotive age. In 1919, there were 6.7 million cars in the US; by 1929, there were 23 million.³⁴³ Between 1920 and 1929 alone, global motor vehicle production soared from 2.2 million to 5.3 million annually.³⁴³ This was a fundamental shift from coal-powered stationary industry to oil-powered mobile transportation.

War
The period between the World Wars saw unprecedented industrial expansion.³⁴⁴ Steel production, powered by improved blast furnaces reaching temperatures of 1000°F and heights of 80+ feet, enabled massive construction projects.³⁴⁵ The 75,000 miles of railroad track laid in the US during the 1880s represented the largest railroad expansion in world history.³⁴⁴ By the 1920s, the environmental consequences were becoming visible:³⁴⁵ urban areas developed thick smog, and automotive emissions were already recognised as problematic- accounts from the 1890s described petrol motors as notably “dirty”.³⁴⁶ However, systematic efforts to address emissions wouldn’t begin until decades later.

World War II (1939-1945) triggered the largest industrial mobilization in human history.³⁴⁷ Factories converted to military production, aircraft manufacturing exploded, and petroleum consumption reached new heights. This wartime surge established the industrial infrastructure and energy-intensive mindset that would characterize the post-war boom. By 1950, global CO₂ emissions had reached 6 billion tonnes annually- a massive increase from pre-industrial levels of essentially zero,³⁴⁷ and atmospheric CO₂ concentrations had risen from 280 ppm to approximately 310 ppm.³⁴⁷ This represented the steepest change in atmospheric chemistry in over 10,000 years.³⁴⁷

Anthropocene
Antonio Stoppani first proposed the idea of a new geological era named after human impact on the planet in 1873. He proposed we call our age the “Anthropozoic”.³⁴⁸ A century later, in the 1980s, Eugene Stoermer coined the term “Anthropocene” (Anthropo = man, Cene = new)³⁴⁹.³⁴⁸ In 2019 a panel of scientists voted to nominate Anthropocene as a new geologic era that began in 1950.³⁵⁰

This proposal of formal geological recognition was rejected in March 2024. Even so, the Anthropocene remains scientifically valid as a descriptor of human impact. The International Union of Geological Sciences (IUGS) voted down the formal epoch proposal with 12 against, 4 in favour, with 2 abstentions out of 18 total voting members, not because they dismissed human impact, but because they couldn’t constrain it within traditional geological frameworks.^351352353The IUGS concluded: “Despite its rejection as a formal unit of the Geologic Time Scale, Anthropocene will nevertheless continue to be used not only by Earth and environmental scientists, but also by social scientists, politicians and economists, as well as by the public at large”, and “Anthropocene” remains “an invaluable descriptor of human impact on the Earth system”.³⁵²

Since 1950, humans have:
1. Doubled fixed nitrogen on the planet through industrial fertiliser production³⁵⁴ ³⁵⁵
2. Created a hole in the ozone layer through CFC releases³⁵⁶ ³⁵⁷
3. Released enough greenhouse gases to cause planetary-level climate change³⁵⁸ ³⁵⁹
4. Created tens of thousands of synthetic compounds that don’t naturally occur on Earth³⁶⁰
5. Caused one-fifth of river sediment to no longer reach oceans due to dams³⁶¹ ³⁶²
6. Geologists have identified novel “anthropogenic rocks” (Plastiglomerates, which are rock-plastic composites formed by melting, Pyroplastics, plastics altered by fire, Plasticrusts, plastic crusts on natural rock surfaces, and Plastisandstones, sandstones cemented with plastic particles)³⁶³
7. Human-made materials now exceed natural geological processes. We move more sediment and rock annually than all natural processes combined.³⁶⁴ ³⁶⁵
8. Beyond nuclear weapons, nuclear power and accidents have left distinct radioactive signatures in sediments worldwide.³⁶⁶ ³⁶⁷
9. Coal and fossil fuel burning since 1950 has created distinct carbon particle layers in ice cores and sediments globally.³⁵⁸ ³⁵⁹

The 2019 UN IPBES Global Assessment confirmed that about one million species are at risk of extinction within decades. A 2023 study suggests two million species are threatened. This is double the previous estimates:
1. 12% of all bird species are threatened with extinction;³⁶⁸ ³⁶⁹
2. 48% of monitored species are experiencing population declines;³⁷⁰
3. Only 3% have increasing populations;³⁷⁰ and
4. 81% of megaherbivores went extinct during Late Pleistocene human expansion.³⁷¹

Microplastics have become ubiquitous geological markers.³⁶³ Since mass plastic production began in the early 1950s, microplastics are “forming a near-ubiquitous and unambiguous marker of Anthropocene”. Microplastics now appear in archaeological dig sites as deep as 7.35 metres (24+ feet) below surface in deposits as old as the first century CE.³⁶³ This contamination shows how rapidly plastic pollution has infiltrated Earth’s sedimentary record (or maybe this is proof of time travel, who can say?).

So unprecedented is the scale of human-made changes to the planet, that we’re now adding 2-3 ppm of CO₂ every single year³⁷² ³⁷³ ³⁷⁴ (2024 saw the largest one-year increase on record at 3.75 ppm³⁷³), when before us, even during the fastest (non volcanic) natural changes (like after ice ages), CO₂ rose by 1-2 ppm every 1,000 years.³⁷⁵ ³⁷⁶ When CO₂ levels changed naturally, it usually took between 1,000-7,000 years to add 1-2 parts per million ppm to the atmosphere, which means that a natural change of 100 ppm would normally take 5,000-20,000 years.³⁷⁷ ³⁷⁸ We did it in just 120 years.³⁷⁹ ³⁸⁰ We’ve warmed the planet about 1°C in just 150 years, 10 times faster than any climate change in the past 65 million years.³⁸¹ ³⁸² ³⁸³ If we examine the rate of human-attributable (whether caused or accelerated) species extinction, it is now 1,000 times higher than what would happen naturally³⁸⁴ (normally, about 1-5 species per million go extinct each year³⁸⁵): so difficult have we made life for others we share this planet with, even whales don’t feel like singing any longer.³⁸³ ³⁸⁴ ³⁸⁵ ³⁸⁶

At current rates, we might match the total PETM carbon release by 2159- in just 4-5 generations.³⁸⁷ Even during that ancient catastrophe, CO₂ rose 5-27 times slower than today, and the PETM lasted for more than 200,000 years.³⁸⁸ ³⁸⁹ This also means various species had time to adapt to the new (well, old) normal, which is not to mention the planet took another 200,000 years to recover from it.³⁹⁰ We’re doing in months and years what took millennia.

Had the proposal to call the age Anthropocene been approved, the first age of the Anthropocene would have been called “Crawfordian” after Crawford Lake. This naming reflects the precision with which the 1950 boundary can be identified in geological records (The first atomic bomb test on July 16, 1945, in New Mexico spread radioactive isotopes globally, creating an unambiguous geological marker. Crawford Lake in Ontario, Canada was chosen as the candidate site because its sediments clearly show the spike in plutonium from hydrogen bomb tests starting in the 1950s).³⁶⁷

Perhaps most telling: Future geologists will find a sharp spike in CO₂, methane, and artificial materials in sediments beginning around 1950³⁹⁴ ³⁹⁵– a Boudica layer marking the human footprint.

Sources (Some citations are repeated but now I’ve forgotten which ones, so this list does not correspond exactly to the citation list, but is nevertheless a comprehensive repository of the sources I consulted while writing this post.)

Author: Finrod Bites Wolves

A blogger. View all posts by Finrod Bites Wolves

A climate history of the Earth

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