Growth in fundamental drivers—energy use, economic productivity and population—can provide quantitative indications of the proposed boundary between the Holocene Epoch and the Anthropocene. Human energy expenditure in the Anthropocene, ~22 zetajoules (ZJ), exceeds that across the prior 11,700 years of the Holocene (~14.6 ZJ), largely through combustion of fossil fuels. The global warming effect during the Anthropocene is more than an order of magnitude greater still. Global human population, their productivity and energy consumption, and most changes impacting the global environment, are highly correlated. This extraordinary outburst of consumption and productivity demonstrates how the Earth System has departed from its Holocene state since ~1950 CE, forcing abrupt physical, chemical and biological changes to the Earth’s stratigraphic record that can be used to justify the proposal for naming a new epoch—the Anthropocene.
A stratigraphic case has been made for a planetary-scale Anthropocene time interval at epoch rank, one that would end the Holocene Epoch at ~1950 CE1. Conceptually, the transition reflects a change from human drivers of environmental change having gradually increasing significance and mostly regionally expressed, to becoming overwhelming and global in extent. But what quantifiable metrics enable direct comparison between the Anthropocene and the preceding Holocene? As a unit of the international Geological Time Scale, the Quaternary Period2,3 formally partitions into Pleistocene (2.58 My to 11.7 ky) and Holocene (11.7 ky to present) epochs4. The Holocene, which follows the end of the last cold episode with the rapid northward movement of the oceanic polar front, is formally subdivided by the International Commission on Stratigraphy (ICS) into three ages:5,6 Greenlandian (11.7 to 8.2 ky), Northgrippian (8.2 to 4.3 ky), and Meghalayan (4.3 to 0 ky). Here, we trace the human footprint through each Holocene age, with focus on two historical and informal intervals: Pre-Industrial (1670–1850 CE) and Industrial (1850–1950 CE), within the Meghalayan Age. The Anthropocene as a potential epoch7,8 is first compared to these earlier Holocene ages, using the human population and its energy consumption and economic productivity, and then assessed by evaluating how human action has disturbed the landscape, altered river discharge (water, particulate and dissolved constituents), and has shifted climate, biogeochemical cycles, biodiversity, and other parts of the Earth System. These changes have already resulted in a sharp distinction in the stratigraphic record between the Holocene and Anthropocene1,7,8. This study formulates a consistent quantitative approach evaluating key Earth-surface parameters and their human drivers to validate the contention that the Anthropocene is an epoch-level planetary interval in Earth’s history, comparable to or exceeding in planetary impact the Holocene Epoch, and greatly exceeding component Holocene ages.
The Anthropocene Epoch is used here as a geological time unit for potential inclusion in the Geological Time Scale. A proposal to formalize the Anthropocene for this purpose is currently being developed by the Anthropocene Working Group (AWG), which includes many authors of this paper, and will require a defining Global Boundary Stratotype Section and Point (GSSP) to be selected and approved, consistent with ICS standard practice.
A Holocene history of the human footprint
The Greenlandian Age (11.7 to 8.2 ky) constitutes the first 3464-y of the Holocene, driven by Milankovitch warming of ~+0.5 °C9, during which the Inter-Tropical Convergence Zone shifted northward10 and Northern Hemisphere ice sheets ablated. Atmospheric CO2 and CH4 concentrations continued a trend of rapid rise initiated in the latest Pleistocene and peaking at ~10 ky11. Coastal human populations retreated inland from initial settlements12, especially on deltas13, as global mean sea level rose ~48.5 m, at a rate of ~15 mm/y between 11.4 ky and 8.2 ky14. Human population was sparse and grew from ~4 M to 8 M (Fig. 1a), at a rate of 0.01%/y (Table 1, Supplementary-Table 1). Regional extinctions of large terrestrial mammals (e.g., ground sloths in North and South America) correlate with the arrival of humans15. Humans lived as foragers, fishers, or hunters, but in a few locations began to cultivate domesticated food crops16. Energy sources were wood-burning and human muscle, and more rarely, animal muscle, with an estimated per capita energy consumption of 6.2 GJ/y, ranging from 5.8 to 6.5 GJ/y (Fig. 1b, Table 1). The human population during the Greenlandian consumed 0.12 zetajoules of energy (with 1 ZJ = 1021 J). Global productivity is used here as a measure of output per unit of input, such as labor, capital or any other resource calculated for the global economy (GDP per capita per unit time), and if meaningful at all for the Greenlandian, was very low (Fig. 1c, Table 1).
During the Northgrippian Age (8.2 to 4.3 ky), global mean sea level rose another ~14.5 m, mostly in the first 1500-y, as the great Northern Hemisphere ice sheets largely had disappeared by 7000-y ago14,17. The Age-averaged rate of global mean sea-level rise was ~3.6 mm/y (Table 1). Global climate was relatively stable at a temperature plateau until 5.48 ky, when the planet cooled ~−0.2 °C, but with regional exceptions9. The trend in atmospheric CO2 and CH4 concentrations changed from slightly falling to slightly rising, at ~8 ky and ~5 ky respectively. Although some have argued that this increase reflected deforestation in response to expanding agriculture, in particular rice cultivation in the case of methane10, others suggest that the rise reflects the gradual adjustment of ocean chemistry towards an equilibrium state following deglaciation18. Some humans, still a minority at the end of the Northgrippian Age, organized into structured agrarian societies. Once sea level stabilized, the human population grew to 27 M (0.03%/y), as urban centers and ports developed (Fig. 1a, Table 1) and the earliest state-level societies originated (Mesopotamia at 3700 BCE, Egypt at 3300 BCE, Peru 3000 BCE, Indus Valley at 2500 BCE, Mesoamerica 1900 BCE, and Yellow River 1700 BCE19,20). Energy sources included wood burning, human and animal muscle, with the per capita energy consumption at 7.1 GJ/y, ranging from 6.5 to 7.8 GJ/y (Fig. 1b, Table 1). Humans expended 0.34 ZJ across the Northgrippian Age, a 332% increase from the Greenlandian, reflecting an increased human population. Human productivity remained low (Fig. 1c, Table 1). The anthropogenic footprint included regional soil erosion from deforestation, a proliferation of pastureland, and some mining21,22. Extinction of large terrestrial mammals correlates with climate change23, though some extinctions have been linked to human actions15.
The Meghalayan Age, as represented here, is the recent ~4.2-ky interval (to ~1950 CE), when global mean sea level rose 1.0 to 1.5 m, or ~0.3 mm/y14, as the global climate cooled ~−0.5 °C9, in what is referred to as Neoglaciation24. Insolation decreased, and there were slight rises in atmospheric CO2 and CH4 concentrations25. Human populations increased by an average 0.2%/y, reaching a population of 2500 M by 1950 CE (Fig. 1a, Table 1). Apparently related to sea-level stabilization, biological productivity on the coastal margin increased dramatically and likely initiated the further movement to large empire level organization in human society facilitating greater demand for goods, increased trade and complex urbanization19,20,26. Large-scale water diversion schemes were built, and extensive farming practices increased21,27. Coal became a common energy supply in the 19th century28. Per capita energy consumption averaged 8.3 GJ/y, ranging from 7.8 to 40 GJ/y, with humans expending 14.2 ZJ across the Meghalayan Age, a 24-fold increase over the Northgrippian Age (Fig. 1b, Table 1). Per capita GDP averaged $144/y (Fig. 1c, Table 1). Humans transferred plant and animal species beyond their native ranges, exemplified by the spread of chickens29, maize30 and Pacific rats31. Human impacts produced extensive regional losses32 and widespread extinctions of land vertebrates33, including the ancestors of domesticated cattle in Eurasia34 and flightless birds in the Pacific35. Introductions and extinctions left a distinctive archeological and fossil signal36,37,38.
Below we discuss two informal intervals, the Pre-industrial and the Industrial, that capture the end of the Meghalayan.
Pre-Industrial interval (1670–1850 CE)
A 180 y-long interval when Holocene sea-level rise was at its slowest ~0.15 mm/y14, with no discernible trend during the 18th century, and a slight fall from 1800 to 1850 CE39, when Alpine glaciers were at their maximum Meghalayan extent40 in response to extensive volcanism41. Earth had no discernible climate trend ~0.0 °C9 during this interval, with cooling pulses varying regionally42. Human population expanded from ~600 M to 1247 M, a growth rate of 0.4%/y (Fig. 2a). The per-capita energy consumption was 18.4 GJ/y, ranging from 13.5 to 22 GJ/y (Fig. 2b, Table 1), with humans expending 2.9 ZJ or 20% of the human energy consumption during the 4,200-y Meghalayan Age (Table 1). Novel energy sources included whale oil43 and stream energy; for example, there were >65,000 water-powered mills in the U.S.A. prior to 1840 CE44,45. Human-enabled species introductions expanded, and transfers happened rapidly, exemplified by the spread of accidentally introduced aquatic mollusks in Europe46. This informal interval represents the fundamental transformation from pre-industrial to full industrial energy use. Prior to 1670 CE, expenditures in England used to obtain basic energy resources (human food, fodder for animals, and wood fuel) amounted to 50–70% of GDP47. By 1850 CE, with the growing use of coal, less than 30% of GDP was allocated to obtaining energy, and <10% after 1950 CE, as fossil fuels dominated energy use47. Global per capita GDP increased by 1750 CE to $178/y in 1990 international dollars (Table 1, Fig. 2c).
Industrial interval (1850–1950 CE)
This 100-y interval captures the change in human–nature interactions48. Atmospheric CO2 increased from the spread of industrial activity and drove a planetary warming by ~+0.2 °C49 (~ + 0.6 W/m2)49, on an otherwise essentially flat Milankovitch insolation signal50,51. Solar variability had very little effect, with the number of sunspots rising in 1950 CE to levels slightly lower than that in the 1860s and the 1780s52,53, in contrast to the pre-industrial Maunder Minimum from 1645 to 1715 CE54. Thus, natural variability contributed little to warming, (<0.2 W/m2)49 during this interval, where the main natural changes were brief intervals of cooling related to large volcanic eruptions that ejected reflective material into the stratosphere (e.g. Krakatoa in 1883 CE)55,56. Sea-level rise accelerated to ~0.5 mm/y in the late 1800s, and to ~2.2 mm/y by 1940 CE, before beginning a temporary deceleration57. This pattern is consistent with the natural fluctuations in the warmth of the North Atlantic in responses to changes in the Atlantic Meridional Ocean Circulation that induces regional and slight global warming as it accelerates, reversing as it decelerates58.
Human population grew at 0.8%/y, from 1250 M to 2500 M (Figs. 1a, 2b, Table 1). Energy consumption per capita averaged 27.2 GJ/y, ranging from 22 to 40 GJ/y (Fig. 2b), accounting for 4.9 ZJ or 35% of the energy consumption across just 2.4% of the 4200-y Meghalayan Age (Table 1). In addition to the growing use of coal, new energy sources included hydroelectric power, oil and natural gas, more than offsetting declines in whale oil and stream power (driven by gravity). Many large rivers were engineered, with levees, dams and water diversion schemes59. Some lake60 and marine61 ecosystems started to turn hypoxic. Biodiversity loss increased and introduced species, such as the giant African snail and naval shipworm62,63, spread through terrestrial and aquatic environments21,32,64. Dispersals were facilitated by increasing global trade65. Per capita GDP had increased by 1900 CE to $679/y in 1990 international dollars (Table 1, Fig. 2c), underwriting new global transportation systems and power sources.
Although the European industrial interval began in the 1700s, we use 1850 CE as the start of the interval, given the remarkable change in both global energy use and global productivity (Fig. 2c). For most of the Holocene Epoch, human productivity (GDP per capita: see SOM Historical GDP Consumption Data) increased linearly with a growing population (Fig. 2c). From 1850 CE onwards, human productivity accelerated (Fig. 2c), which explains why that time period was originally suggested as the start of the Anthropocene66,67. For most of the Holocene, the ratio of human productivity to energy use decreased (Fig. 2d). After 1850 CE, human society became more productive per unit of energy use (Fig. 2d). During the 11.7 ky of the Holocene Epoch, including the Industrial interval, the global human population consumed 14.6 ZJ of energy of which 35% was consumed in the final 100 years.
An Anthropocene history of the human footprint
Proposed Anthropocene Epoch from 1950 CE:1,68 Driven by the accelerated burning of hydrocarbon fuels, atmospheric temperatures increased by 0.9 °C in the last 70 years (and by 1.1 °C from 1900 to 2018 CE69), with much of the rise post-dating 1970 CE70, during an interval of limited sunspot influence and a flat Milankovitch signal. Sunspot numbers rose slightly from their 1950 CE levels to peak levels in 1980 CE and 1990 CE that are more or less similar to those reached in the 1780s and the 1860s, and then began declining52 even as warming continues (Box 1).
Sea-ice volume shrinkage: 300 ± 100 km3/y loss (~275 Gt/y) in the Arctic Ocean since 1980 CE72. Antarctic sea ice extent in October 2019 CE was less than for any previous October since satellite observations of sea-ice began in 1978 CE73.
Glacial-ice mass loss: from 113 ± 125 Gt/y during 1992–1996 CE to 665 ± 48 Gt/y during 2012–2016 CE74, with ~5.6 Tt (=1012 tonnes) of land ice loss on Greenland75 and ~5.0 Tt from Antarctica since 1980 CE76.
Sea-level rise acceleration: from 1.53 mm/y (0.96 to 2.11 mm/y) during 1901–1990 CE, to 2.06 mm/y (1.76 to 2.36 mm/y) during 1971–2015 CE, and to 3.07 mm/y (2.70 to 3.7 mm/y) during 1993–2015 CE77,78,79.
Acidification of the global ocean: through the absorption of atmospheric CO2 with open-ocean surface pH declining by a range of 0.017–0.027 pH units per decade since the late 1980s80,81,82, threatening the survival of particularly soluble organisms, such as aragonitic pteropods. Increasing acidity may raise the calcium carbonate compensation depth (CCD) in the deep ocean, causing the demise of carbonate-shelled deep-water benthic organisms.
Since 1950 CE, the human population has rapidly increased, with societal and medical advances extending lifespans. Industrial-scale agriculture, with its global distribution system, presently feeds a global population of 7800 M that grows at an average rate of 1.63%/y, presently 71 M/y. In absolute numbers, human migration within and between continents has reached its historical zenith during the Anthropocene, as many coastal cities have transformed into megacities (>10 M) in just decades83 (Table 2).
1950 CE also marks an important upturn in the global spread of technological knowledge occurring when societies became more economically interdependent (the Great Acceleration48,84). Between 1650 and 1750 CE, the annual citations of scholarly references grew at ~0.15%/y85, increasing by an order-of-magnitude to ~1.5%/y during 1750–1927 CE. After 1927 CE for all subjects, and after 1947 CE for the natural sciences, citation rates have jumped to ~8%/y85 following compulsory education and widespread literacy.
Global per capita GDP has risen rapidly in the Anthropocene, to a current figure of $12,500/y (Fig. 2, Table 2). This inflation-adjusted global productivity is an order-of-magnitude greater than during the Industrial interval just 70 years earlier (Tables 1, 2, Fig. 2c). Since 1950 CE, energy consumption by humanity has averaged 61 GJ/y per capita (range 40 to 75 GJ/y; Fig. 2b, Table 1), enabled by a diversified portfolio of energy sources (coal, oil, gas, nuclear, and renewables). Fossil fuels power more than 80% of the economy86. In total, 60% of all human-produced energy has been consumed since 1950 CE, at 22 ZJ, more than in the entire previous Holocene (~14.6 ZJ: Table 1). Since 1871 CE, the Earth’s oceans have stored ~436 ZJ of solar energy trapped through the increases in anthropogenic greenhouse gases87, and from warming-induced increases in water vapor88, a reinforcing feedback. This is more energy by an order-of-magnitude than associated with direct human production and consumption (at 23.3 ZJ since 1871 CE). Approximately half of the Anthropocene sea-level rise stems directly from this steric effect on ocean volume, with the remainder largely derived from the melt of terrestrial snow and ice49. Since about 1950 CE, the global ocean has progressively warmed both at the surface and increasingly to depths exceeding 2000 m. Heat is transferred vertically by storms and eddies, and by the sinking of surface water made dense by cooling, especially in the Labrador and Norwegian-Greenland seas in the Atlantic and in the Southern Ocean around Antarctica.
Many anthropogenic impacts post-1950 CE are planetary, with greater than regional significance, and scale up with the population of humans and their energy consumption and economic productivity48. Below we offer 16 examples relevant to, and in support of, this Anthropocene Epoch thesis:
The magnitude of the anthropogenic N cycle is roughly equivalent to the global natural N cycle89,90. However, such a simplified numerical comparison underestimates the ecological consequences of such a perturbation which includes impacts on climate change, water and air quality, ozone depletion, and biodiversity loss91,92,93. Globally, reactive nitrogen (Nr) increased by ~50%, between 1600 and 1990 CE, with atmospheric emissions of Nr increasing by 250%, and Nr deposition into marine and terrestrial ecosystems increasing by more than 200%94,95 (Table 2). More than half of human population is alive today because of the production and use of Nr in fertilizers96 and half the nitrogen in our bodies now comes from artificial production. Rates of use of Nr in the U.S.A. have increased from 0.22 g N m−2 y−1, in 1940 CE, to 9.04 g N m−2 y−1, in 2015 CE97. One of many consequences of fertilizer overuse, along with contributions from increased livestock, human sewage and hydrocarbon combustion, is the spread of hypoxia in coastal waters as ‘dead-zones’ inimical to marine life98: world coastal zones now receive ~100 Mt/y of anthropogenic-sourced Nr48. Because industrially derived nitrogen is depleted in 15N, its atmospheric deposition offers a strong and coherent far-field signal in the N isotope ratios of both lake sediments and ice cores, with the main inflection at ~1950 CE99,100.
River systems have been largely replumbed during the Anthropocene, with the construction of dams, reservoirs and diversions, with channel-bed mining and levee hardening, and with discharge focusing59,101,102. Only 23% of rivers longer than 1000 km flow uninterrupted to the coastal ocean, and only 10.5% of large rivers in Europe and 18.7% in North America can be considered as free-flowing rivers103. Large dams (>15 m in elevation) are the main cause of fluvial sediment being sequestered upstream, leading to a global decline of 18% in sediment delivery to the coastal ocean compared with pre-human times59,104. Of the 58,519 large dams registered in 2017 CE105, 1.4% were built before 1850 CE, having a combined reservoir capacity of 6.1 km3; 10% were built during 1850–1950 CE, with a total reservoir capacity of 685 km3. 95.7% of the world’s total reservoir capacity was emplaced after 1950 CE, increasingly in Asia106 (Fig. 3a, Table 2). Total reservoir capacity of these large dams today exceeds 15,000 km3; together they trap >3100 Gt of sediment, equivalent to a 5 m-thick deposit covering all of California or Spain. During the Industrial interval, four rivers (Colorado, Nile, Indus, and Yellow) transported 1.5 Gt/y of sediment to the coastal ocean; today they deliver <0.2 Gt/y107. Similarly, smaller dams have greatly reduced discharges to the coastal ocean, a consequence of upstream demands by human consumption and reservoir evaporation107.
In 1904 CE, the U.S.A. had 225 km of paved highways outside of city streets108. Today 4.3 M km of U.S.A. roads are covered in asphalt or concrete; another 2.2 M km of roadway remain unpaved109. Since each road-km requires ~1250 metric tons of sand, and ~1875 metric tons of gravel, the U.S.A. highway system has consumed ~20.6 Gt of sand and gravel. By comparison the Great Wall of China contains only 0.4 Gt of stone59. The 64 M km of global roads and highways110 have consumed ~200 Gt of sand and gravel to support the traffic of 1 billion motor vehicles (Table 2).
Industrial-scale mining has changed the global landscape; for example, the >500,000 abandoned mines and quarries in the U.S.A. alone59, or the removal of mountain tops in West Virginia to access the coal underneath along with the concomitant dumping of spoils in nearby river valleys. Natural processes (ice, wind, water) transport 26 Gt/y of global sediment59, a much smaller value than from modern mining activity. Estimates of global annual coal production (including underground, surface, hard and brown coals) and associated wastes totaled 74 Gt/y (35 km3); other mining and mineral extraction, including overburden and waste removal accounted for another 27 Gt/y (13 km3), as recorded in 2015 CE111. Coal mining in the U.S.A. increased from 0.9 Gt/y in 1905 CE112 to 8.5 Gt/y during 2010–15 CE113. Bitumen (tar) sand-mining in Canada entered commercial production in 1967 CE; in 2012 CE, 1.5 Gt of bituminous sand were processed59. In 1970 CE, 944 Mt of sand and gravel were mined within the U.S.A., compared with 0.5 Mt in 1902 CE108. The Global Aggregate Information Network, representing 70% of global aggregate production (~50 Gt/y), operates 500,000 quarries and pits worldwide, employing 4 M people114. There is now concern that the increasing demand for sand for building megacities is outstripping supply. Offshore dredging for aggregates destroys marine habitats, as does bottom trawling for fish and shellfish, affecting marine biodiversity.
Since industrialization, human mining activities have impacted the global mobilization of naturally occurring elements, particularly the cycles of the chalcophile elements (e.g., As, Cd, Cu- Fig. 3e, Hg, Ni, Pb, Sb, Zn) associated with the smelting and refining of base metal ores, coal combustion and cement production115,116. In recent decades, platinum group elements that are required for advanced materials and technologies have been profoundly affected117,118,119. Increased extraction rates of ores (Table 2) have caused a transfer of metals from the lithosphere to these metal-in-use products and thence to wastes120. While negligible amounts of the industrial metals were extracted and put into use before 1900 CE121, use of metals substantially increased after the 1950s122 causing disturbances in natural biogeochemical cycles. Perturbations of Pb, Hg, Se and Sn geochemical cycles now reach a global scale123, with increasing perturbations for other metals124.
Industrial-scale agriculture accounts for 50% of terrestrial soil loss125,126, leaving nearby rivers with increased sediment and nutrient loads126,127,128. Forest clearing for the creation of agricultural lands has long increased soil erosion rates27,129, but contemporary rates of soil loss from cropland exceed the natural rates of erosion 30-fold130. Cropland represents ~11% of the global land area, but accounts for ~50% of soil erosion131; soil erosion rates from forests are 77 times lower. From 2001 to 2012 CE, when 2.3 Mkm2 of forest was lost, only 4% of this loss was converted to cropland, but was responsible for more than half of the increase in soil erosion132. Remaining soils are then progressively compacted by large agricultural machines and have their organic content gradually reduced, requiring replacement with artificial fertilizers (Fig. 3f). Soils have also become increasingly dry in response to atmospheric warming133. The industrial agricultural system consumes ~10 units of energy for each unit of food energy produced134,135.
Many thousands of anthropogenic contaminants including persistent organic pollutants (e.g. organochlorine pesticides, brominated flame retardants) and pharmaceutical compounds have been deliberately or accidentally released into the environment. Following the discovery of its insecticidal properties in 1939 CE, the total usage of DDT during 1950–1993 CE was ~2.6 Mt136; 5-y emissions of DDT to the atmosphere from 1970 to 1975 CE were ~750 kt137. General use of pesticides in agriculture now reaches ~4 Mt/y138. Compounds such as DDT are highly persistent in the environment despite a 1970s ban in many countries and have left a clear signal in the sedimentary record8. Pesticides are widely released as legacy pollutants from melting glaciers139. Compounds such as PCBs find their way via the atmosphere to Arctic lands where they contaminate the wildlife (e.g. seals) used as food by indigenous peoples. Atmospheric emissions of the refrigerant chlorofluorocarbon CFC-12 (dichlorodifluoromethane, CF2Cl2) was zero in 1930 CE, rising to >460 kt in 1987 CE140. CFC releases have caused the Antarctic Ozone Hole, and their use is now banned under the Montreal Protocol. The combustion of coal, and historical gold and silver mining, has increased atmospheric mercury concentrations by ~450% over pre-industrial levels141. Global anthropogenic emissions of black carbon during 2000–2010 CE were ~6.6 to 7.2 Mt/y142, compared with 0.6 Mt/y in 1875 CE143; the result has been a major increase in carbonaceous fly-ash in natural archives across the world since the 1950s144.
Coastal engineering has globally added thousands of km of groins, jetties, seawalls, breakwaters and harbors to control the movement of coastal sediment, leading either to coastal erosion or to siltation58,145. Lacking the delivery of silt from the interior, along with the rise of coastal aquaculture and coastal megacities (Table 2), river deltas are subsiding at rates of tens to hundreds of mm/y146,147,148. Many coastlines now retreat at highly variable rates of tens to hundreds of m/y145, except where substantial seawalls are emplaced, as in the Netherlands. The global extent of wetlands today is ~10 Mkm2 149. Best estimates suggest that 54–57% of the total area of natural wetlands has already been lost, with the rate of loss accelerating during the 20th and 21st centuries150. In many tropical areas, natural and protective mangrove swamps have been replaced with shrimp and fish farms, further exposing coastlines to erosion145. Consequences of this wetland loss include the oxidation of extensive reserves of organic matter into CO2, reduced water retention and storage, more groundwater infiltration by saltwater, and loss of wildlife habitat and biodiversity.
Plastic production has increased from ~2 Mt/y in the 1950s, to 359 Mt/y in 2018 CE151,152,153, including 526 B/y of plastic beverage bottles and 3000 B/y of plastic cigarette filters154 (Fig. 3c, Table 2). Plastic debris now enters into the ocean at rates between 4.8 and 12.7 Mt/y155, and microplastics are increasingly being transported by aeolian vectors, permitting true global distribution, even to Arctic snowfields156, forming a near-ubiquitous and unambiguous marker of Anthropocene strata8.
Human-mediated mineral species and synthetic mineral-like compounds now exceed 180,000 in number, with most species created since 1950 CE8,157 (Table 2). Earth’s geological processes over the last 4.5 By have only supported the formation of 5,300 naturally occurring mineral species, including those mediated by biological processes157,158.
Concrete production in modern times began in 1824 CE, with the patenting of the Portland Cement recipe. Production remained minor until 1950 CE when 0.13 Gt/y of cement produced ~1 Gt/y of concrete. Today, global cement and concrete production are 4 Gt/y and 27 Gt/y, respectively (Fig. 3d, Table 2), incorporating novel geochemical and mineralogical compositions, such as organic polymer fibers, silica fume, fly ash, nanotubes and nanospherules of silica, iron, graphene and titanium oxide159. Cement production requires the heating of CaCO3 to release CO2, leaving lime in the form of calcium oxide (CaO) or hydroxide.
As the planet heats up, water vapor evaporated from the oceans, lakes, reservoirs and soils has become the dominant greenhouse gas accounting for ∼50% of the greenhouse effect, followed by clouds (∼25%), CO2 (∼20%), then CH4 and N2O88. Atmospheric carbon dioxide is, however, the main driver of planetary warming. In 1750 CE, humans produced 0.009 Gt/y of atmospheric CO2, increasing to 0.2 Gt/y by 1850 CE, 5.3 Gt/y by 1950 CE, then accelerating to 36.1 Gt/y by 2017 CE160 (Fig. 3b, Table 2). Emission sources include combustion of coal, oil, and gas, and cement production. Similarly, atmospheric methane globally increased from 719 ppb in 1750 CE, to 1162 ppb in 1950 CE, and 1850 ppb in 2017 CE160; atmospheric nitrous oxide concentration shows a similarly increasing trend160 (Table 2).
In 1950 CE, 1% of the high seas (non-territorial open ocean) were fished, with 0% of fishery species considered exploited, overexploited or collapsed, as defined by the UN’s Food and Agriculture Organization. By 2006 CE, 63% of the high seas were fished and 87% of fish species were considered exploited, overexploited, or had collapsed161, with overall marine fish declines of 38%. Certain baleen whale populations have declined by 80–90%162.
Humans, together with their livestock including domesticated poultry, have a cumulative biomass of ~0.165 Gt C163, 4-fold greater than the wild mammal and bird biomass (~0.04 Gt C) ~100 ky ago164. Fully 96% of today’s mammalian biomass is represented by humans and their domesticated animals; the biomass of poultry birds amounts to 70% of all living birds163. Wild bird and mammal totals today have a much-reduced biomass ~0.009 Gt C163. For comparison, the total biomass of modern human-cultivated crops is ≈10 Gt C163. It is estimated that Earth’s current total vegetation biomass is half of potential biomass stocks prior to human perturbation, mainly through forest loss163,165.
Anthropogenic emissions of sulfur-containing gases exceed natural fluxes by 2 to 3 times166. Presently there is a peak in atmosphere emissions of SO2 (~100 Mt/y), although emissions are expected to decline167. Emissions of SO2 from nickel smelting in Sudbury, Ontario, reached their zenith in the 1960s (2.5 Mt/y), but technological innovations have since lowered these by ~95%168. Phosphorus mobilization by human activities currently exceeds the natural global cycle by a factor of 3169. Like N, P is commonly growth-limiting for biota with profound ecological consequences170,171, with both nutrients contributing to surface water eutrophication.
The annual rate of species invasions has greatly increased since the late-20th century172. Species inventories of ecosystems record rapid or substantial changes in many seas173, rivers174, estuaries175 and terrestrial settings176,177, often leaving a biostratigraphical signature of change46,178. Many invasive species signal highly human-disturbed ecosystems179.
The most widespread and globally synchronous human signal is the fallout from nuclear weapons testing commencing in 1945180. Liberation of radioactivity to the atmosphere via thermonuclear explosions from more than 500 tests between 1952 and 1980 CE, have left a clear signature of anthropogenic radionuclides on or near the surface of the entire planet180. Approximately 300 kg of 137Cs and 120 kg of 90Sr were released in those atmospheric explosions181, along with 2900 kg of 239Pu, corresponding to about 6.5 PBq of radioactivity182. 239Pu occurs naturally in the Earth’s crust but its pre-1950 CE concentration is extremely low, ~0.05 mBq/kg in typical soils183. Due to its long persistence (half-life 24,110 y), this naturally rare radionuclide will be detectable for ~100 ky into the future184.
Human population has exceeded historical natural limits, with 1) the development of new energy sources, 2) technological developments in aid of productivity, education and health, and 3) an unchallenged position on top of food webs. Humans remain Earth’s only species to employ technology so as to change the sources, uses, and distribution of energy forms, including the release of geologically trapped energy (i.e. coal, petroleum, uranium). In total, humans have altered nature at the planetary scale, given modern levels of human-contributed aerosols and gases88,160, the global distribution of radionuclides, organic pollutants and mercury123,139,141,144, and ecosystem disturbances of terrestrial185,186 and marine environments187. Approximately 17,000 monitored populations of 4005 vertebrate species have suffered a 60% decline between 1970 and 2014 CE188, and ~1 million species face extinction, many within decades189. Humans’ extensive ‘technosphere’, now reaches ~30 Tt, including waste products from non-renewable resources190.
Such vast alterations to Earth’s natural atmospheric, hydrologic, pedologic, biologic, biogeochemical and sedimentary systems not only have changed the Earth System considerably191,192,193 but have also created innumerable globally detectable and preservable signals. These changes are now being used to justify a new geochronologic epoch, the Anthropocene1,194.
A thought experiment in measuring human impact
Humans, like all living organisms, inject a biological force into their environment. Individualized, this human force should collectively scale up with a growing population. With that logic and other things held constant, one billion humans would offer 1000 times the environment force of one million people. Early humans with their limited numbers (Fig. 1a), had a recognizable but minimal impact on the planet’s terrestrial and marine environments through most of the Holocene (Table 1). Population grew slowly (Table 1, Supplementary-Table 1), and energy use remained low (Figs. 1b, 2b) even with the advances of tool-based hunting, use of fire, employment of animals in agriculture or travel, and the development of settlements. Earth’s surface environment also has some ability to repair itself, such that 1000 humans across 1000 y would likely have a smaller lasting environmental impact than one million humans in just one year. The time-averaged human population in the Holocene is 97 M, compared with the Anthropocene’s population of 4940 M (Supplementary-Table 1). Using a constant per capita energy consumption of say 1 GJ/y, human-derived energy use during the Holocene (to 1950 CE) would be 1.13 ZJ (97.2 M × 11,630 y × 1 GJ/y), and just 0.35 ZJ in the Anthropocene, a longer Holocene duration being more important than a larger Anthropocene population. However, per capita energy consumption increased by an order-of-magnitude across 11,700 years (Table 1, Fig. 1b). As a consequence, humans have already consumed more energy in the short space of the Anthropocene than in the entire Holocene (21.7 ZJ versus 14.6 ZJ).
Humans became a geological force over the last 300 y, particularly after the start of the global industrial revolution in 1850 CE when excess energy (fossil fuel) became widely available. There are strong relationships amongst three parameters: global population, global energy use, and global productivity (Table 2, Figs. 2 and 4). Increases in human productivity support larger populations that consume higher levels of energy and materials that in turn support increases in productivity. The harnessing of fossil fuels has allowed humans to apply this excess in available energy beyond simple food production and survival. As a result, the growth rate in human population increased rapidly, peaking during the mid-20th century (Fig. 2a), as did the associated rates of energy consumption and productivity (Figs. 1 and 2d, Tables 1 and 2). The result has been the mid-20th century ‘Great Acceleration’ when humanity began to dominate many of the planetary cycles as outlined above. Like the intertwining of global human population, energy consumption and productivity, major environmental tracers also appear tightly coupled to each other and to these three human forces (Table 2, Figs. 3 and 4). It should be of no surprise then that the global reservoir capacity of large dams, or atmospheric CO2, each track closely with global energy use (Fig. 3a, b, Table 2), or that global plastic or cement production closely follows economic productivity (Fig. 3c, d, Table 2), or that the global production of ammonia (NH3) and copper correlate highly with global human population (Fig. 3e, f, Table 2), as with many other human environmental signals outlined in Table 2: shrimp farming, production of gypsum, salt, iron, steel, sulfur, helium, aluminum, mineral species, atmospheric gases (CO2, N2O, CH4), terrestrial freshwater budgets, surface temperatures, and sea levels. These major environmental parameters have been strongly altered by the mid-20th century (and beyond, Table 2).
The environmental parameters discussed above should be understood as the societal forcings that lead to stratigraphic markers that will characterize the Anthropocene, such as horizons identified by extinctions or invasive species, radioisotopes, elevated natural and novel chemical compounds, etc. In and of themselves, the societal metrics that we have identified here may not define the Anthropocene, but they can lead to the markers that do and, if present trends continue, will.
Proposed Anthropocene versus Holocene epochs
The Holocene Epoch, the most recent of the Quaternary interglacials, was a time of warm, relatively stable (±0.5 °C) climate that fluctuated in response to variations in Earth’s natural systems (e.g., Milankovitch): ice sheet volume decreased, and sea levels rose at an Epoch-averaged rate of 5.54 mm/y, larger than for the proposed Anthropocene Epoch (although if warming continues modern rates will quickly rise). The proposed Anthropocene Epoch sees many other key Earth-surface parameters change in response to human action (Table 2). Parameters with 200% to 300% variances or larger, compared to the Holocene Epoch, include atmospheric and ocean temperatures, atmospheric CO2, CH4, and N2O levels, global reactive nitrogen, environmental mercury and many other metals, phosphorus release194,195, sediment transport, terrestrial soil loss, and terrestrial and marine biomass losses. Parameters with order-of-magnitude increases, compared to the Holocene Epoch, include anthropogenic CO2 emission rates, human-produced energy, upstream sequestration of sediment, number of “mineral” species, concrete production, rates of species extinction32, declines in river runoff, and increased coastal hypoxia. There are also phenomenological changes without precedent in the Holocene, including a warmer and more acidic global ocean, global dispersal of new materials (plastics, ceramics, aluminum metal, radioisotopes, persistent organic pollutants, pharmaceutical compounds, fly-ash particles), and modern alterations to the biodiversity of marine and terrestrial ecosystems, with a globally distributed invasive species component172 and a greatly raised rate of species extinction33. Even Earth’s crustal process, such as earthquakes, can now have an anthropogenic imprint196.
The Anthropocene Working Group (AWG) has voted to affirm a) the Anthropocene be treated as a formal chronostratigraphic unit defined by a GSSP, and b) the primary guide for the base of the Anthropocene be one of the stratigraphic signals around the mid-twentieth century of the Common Era1,7,68. Geological records characterizing the base of the Anthropocene are being assembled, and in due course the Group’s recommendations will require approval by the International Commission on Stratigraphy. The narrative and quantitative data presented here strongly underpin the trajectory of the Earth System away from a Holocene state of the system, substantially and globally, around the mid-20th century, circa 1950 CE192. Establishing the proposed new epoch would formalize the use of the term Anthropocene, which already has been used widely in research describing changes induced by human actions and recorded in geological archives.
The datasets analyzed during the current study are provided as tables within the main paper or within the accompanying online material file, along with the original data references to peer-reviewed sources including persistent government web links.
Waters, C. N. et al. The Anthropocene is functionally and stratigraphically distinct from the Holocene. Science 351 aad2622 (2016).
Gibbard, P. L. & Head, M. J. The newly ratified definition of the Quaternary System/Period and redefinition of the Pleistocene Series/Epoch, and comparison of proposals advanced prior to formal ratification. Episodes 33, 152–158 (2010).
Gibbard, P. L., Head, M. J. & Walker, M. J. C., The Subcommission on Quaternary Stratigraphy. Formal ratification of the Quaternary System/Period and the Pleistocene Series/Epoch with a base at 2.58 Ma. J. Quaternary Sci. 25, 96–102 (2010).
Head, M. J. Formal subdivision of the Quaternary System/Period: present status and future directions. Quaternary Int. 500, 32–51 (2019).
Walker, M. et al. Formal ratification of the subdivision of the Holocene Series/Epoch (Quaternary System/Period): two new Global Boundary Stratotype Sections and Points (GSSPs) and three new stages/subseries. Episodes 41, 213–223 (2018).
Walker, M. et al. Subdividing the Holocene Series/Epoch: formalisation of stages/ages and subseries/subepochs, and designation of GSSPs and auxiliary stratotypes. J. Quaternary Sci. 34, 173–186 (2019).
Zalasiewicz, J. et al. The Working Group on the ‘Anthropocene’: summary of evidence and recommendations. Anthropocene 19, 55–60 (2017).
Zalasiewicz, J. Waters, C. N., Williams, M. & Summerhayes, C. (Eds) The Anthropocene as a Geological Time Unit: A Guide to the Scientific Evidence and Current Debate. 1st Ed. (Cambridge Univ. Press, Cambridge, 2019).
Marcott, S. A., Shakun, J. D., Clark, P. U. & Mix, A. C. A reconstruction of regional and global temperature for the past 11,300 years. Science 339, 1198 (2013).
Ruddiman, W. F. The Anthropocene. Annu. Rev. Earth Planet. Sci. 41, 45–68 (2013).
Monnin, E. et al. Atmospheric CO2 concentrations over the last glacial termination. Science 297, 112–114 (2001).
Turney, C. S. M. & Brown, H. Catastrophic early Holocene sea level rise, human migration and the Neolithic transition in Europe. Quaternary Sci. Rev. 26, 2036–2041 (2007).
Stanley, D. J. & Warne, A. G. Worldwide initiation of Holocene marine deltas by deceleration of sea-level rise. Science 265, 228–231 (1994).
Lambeck, K., Rouby, H., Purcell, A., Sun, Y. & Sambridge, M. Sea level and global ice volumes from the Last Glacial maximum to the Holocene. Proc. Natl Acad. Sci. USA 111, 15296–15303 (2014).
Steadman, D. W. et al. Asynchronous extinction of late Quaternary sloths on continents and islands. Proc. Natl Acad. Sci. USA 102, 11763–11768 (2005).
Barker, G. The Agricultural Revolution in Prehistory: Why Did Foragers Become Farmers. 1st Ed, (Oxford Univ. Press, Oxford, 2006).
Clark, P. U. et al. Consequences of twenty-first-century policy for multi-millennial climate and sea-level change. Nat. Clim. Change 6, 360–369 (2016).
Broecker, W. S. et al. Evidence for a reduction in the carbonate ion content of the deep sea during the course of the Holocene. Paleoceanography 14, 744–752 (1999).
Day, J., Gunn, J., Folan, W., Yanez, A. & Horton, B. The influence of enhanced post-glacial coastal margin productivity on the emergence of complex societies. J. Island Coastal Arch. 7, 23–52 (2012).
Gunn, J., Day, J., Folan, W. & Moerschbaecher, M. Geo-cultural time: advancing human societal complexity within worldwide constraint bottlenecks – A chronological-helical approach to understanding human-planetary interactions. Biophys. Econ. Resource Quality https://doi.org/10.1007/s41247-019-0058-7 (2019).
Ellis, E. C. et al. Used planet: a global history. Proc. Natl Acad. Sci. USA 110, 7978–7985 (2013).
ArchaeoGLOBE Project. Archaeological assessment reveals Earth’s early transformation through land use. Science 365, 897–902 (2019).
Graham, R. W. et al. Timing and causes of mid-Holocene mammoth extinction on St Paul Island, Alaska. Proc. Natl Acad. Sci. USA 113, 9310–9314 (2016).
Denton, G. H. & Porter, S. C. Neoglaciation. Sci. Am. 222, 101–110 (1970).
Ruddiman, W. F. et al. Late Holocene climate: natural or anthropogenic? Rev. Geophys. 54, https://doi.org/10.1002/2015RG000503 (2016).
Kennett, D. J. & Kennett, J. P. Early state formation in southern Mesopotamia: Sea levels, shorelines, and climate change. J. Island Coast. Archaeol. 1, 67–99 (2006).
Jenny, J. P. et al. Human and climate global-scale imprint on sediment transfer during the Holocene. Proc. Natl Acad. Sci. USA 116, 22972–22976 (2019).
Malanima, P. Energy in world history. In: The Basic Environmental History, Eds. M. Agnoletti & S. N. Serneri. (Springer, New York, 2014).
Bennett, C. E. et al. The broiler chicken as a signal of a human reconfigured biosphere. R. Soc. Open Sci. https://doi.org/10.1098/rsps.180325 (2018).
Williams, M. et al. The palaeontological record of the Anthropocene. Geol. Today 34, 188–193 (2018).
Matisoo, S. et al. Patterns of prehistoric human mobility in Polynesia indicated by mtDNA from the Pacific rat. Proc. Natl Acad. Sci. USA 95, 15145–15150 (1998).
Bomgardner, D. L. The trade in wild beasts for Roman spectacles: a green perspective. Anthropozoologica 16, 161–166 (1992).
Ceballos, G. et al. Accelerated modern human–induced species losses: entering the sixth mass extinction. Sci. Adv. 1, e1400253 https://doi.org/10.1126/sciadv.1400253 (2015).
Mona, S. et al. Population dynamic of the extinct European aurochs: genetic evidence of a north-south differentiation pattern and no evidence of post-glacial expansion. BMC Evol. Biol. 10, 83 (2010).
Allentoft, M. E. et al. Extinct New Zealand megafuna were not in decline before human colonization. Proc. Natl Acad. Sci. USA 111, 4922–4927 (2014).
Burney, D. A. et al. Fossil evidence for a diverse biota from Kaua’i and its transformation since human arrival. Ecol. Monogr. 7, 615–641 (2001).
Rijsdijk, K. F. et al. Mid-Holocene vertebrate bone concentration-Lagerstätte on oceanic island Mauritius provides a window into the ecosystem of the dodo (Taphus cucullatus). Quaternary Sci. Rev. 28, 14–24 (2009).
Crowther, A. et al. Ancient crops provide archaeological signature of the westward Austronesian expansion. Proc. Natl Acad. Sci. USA 113, 6635–6640 (2016).
Jevrejeva, S., Moore, J. C., Grinsted, A. & Woodworth, P. L. Recent global sea level acceleration started over 200 years ago? Geophys. Res. Lett. 35, L08715 https://doi.org/10.1029/2008GL033611 (2008).
Sigl, M. et al. 19th century glacier retreat in the Alps preceded the emergence of industrial black carbon deposition on high-alpine glaciers. Cryosphere 12, 3311–3331 (2018).
Wood, G. Tambora: the eruption that changed the world (Princeton Univ. Press, Princeton, 2014).
Pages2K-Consortium, Ahmed, M. et al. Continental-scale temperature variability during the past two millennia. Nat. Geosci. 6, 339–346 (2013).
Tower, W. S. A history of the American whale fishery. (University of Philadelphia, 1907).
Walter, R. C. & Merritts, D. J. Natural streams and the legacy of water-powered mills. Science 319, 299–304 (2008).
Merritts, D. et al. Anthropocene streams and base-level controls from historic dams in the unglaciated mid-Atlantic region, USA. Philos. Trans. R. Soc. 369, 976–1009 (2011).
Himson, S., Kinsey, N. P., Aldridge, D. A., Williams, M. & Zalasiewicz, J. Invasive mollusc faunas of the River Thames exemplify biostratigraphical characterization of the Anthropocene. Lethaia 53, 267–279 (2020).
Fizaine, F. & Court, V. Energy expenditure, economic growth, and the minimum EROI of society. Energy Policy 95, 172–186 (2016).
Steffen, W., Grinevald, J., Crutzen, P. & McNeill, J. The Anthropocene: conceptual and historical perspectives. Phil. Trans. R. Soc. A 369, 842–867 (2011).
IPCC, Climate Change 2014: Synthesis Report. Contribution of Working Groups I, II and III to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change (eds. R. K. Pachauri, L. A. Meyer.) (IPCC, Geneva, 2014).
Berger, A. & Loutre, M. F. Insolation values for the climate of the last 10 million years. Quaternary Sci. Rev. 10, 297–317 (1991).
Berger, A., Loutre, M. F. & Crucifix, M. The Earth’s climate in the next hundred thousand years (100 kyr). Surveys Geophys. 24, 117–138 (2003).
Clette, F., Svalgaard, L., Vaquero, J. M. & Cliver, E. W. Revisiting the sunspot number. Space Sci. Rev. 186, 35–103 (2014).
Clette, F., Cliver, E. W., Lefevre, L., Svalgaard, L. & Vaquero, J. M. Revision of the sunspot number(s). Space Weather 13, https://doi.org/10.1002/2015SW001264 (2015).
Vaquero, J. M. Historical sunspot observations: a review. Adv. Space Res. 40, 929–941 (2007).
Neukom, R. et al. Consistent multidecadal variability in global temperature reconstructions and simulations over the Common Era. Nat. Geosci. 12, 643–649 (2019).
Neukom, R. et al. No evidence for globally coherent warm and cold periods over the preindustrial Common Era. Nature 571, 550–554 (2019).
Dangendorf, S. et al. Reassessment of 20th century global mean sea level rise. Proc. Natl Acad. Sci. USA www.pnas.org/cgi/doi/10.1073/pnas.1616007114 (2017).
Chen, X. & Tung, K. K. Global surface warming enhanced by weak Atlantic overturning circulation. Nature 559, 387–391 (2018).
Syvitski, J. P. M. & Kettner, A. J. Sediment flux and the Anthropocene. Phil. Trans. R. Soc. A 369, 957–975 (2011).
Jenny, J. P. et al. Global spread of hypoxia in freshwater ecosystems during the last three centuries is caused by rising local human pressure. Glob Chang Biol. 22, 1481–1489 (2016).
Gooday, A. J. et al. Historical records of coastal eutrophication-induced hypoxia. Biogeosciences 6, 1707–1745 (2009).
Wilkinson, I. P. et al. Microbiotic signatures of the Anthropocene in marginal marine and freshwater palaeoenvironments. In A Stratigraphical Basis for the Anthropocene (eds. Waters, C. N., Zalasiewicz, J. A., Williams, M., Ellis, M. A. & Snelling, A. M.) 185–219 (Geological Society, London, Special Publications, 2014).
Hausdorf, B. The giant African snail Lissachatina fulica as potential index fossil for the Anthropocene. Anthropocene 23, 1–4 (2018).
Williams, M. et al. The biostratigraphic signal of the neobiota. In The Anthropocene as a Geological Time Unit (eds. Zalasiewicz, J., Waters, C. N., Williams, M. & Summerhayes, C.) (Cambridge Univ. Press, Cambridge, 2019).
Seebens, H. et al. No saturation in the accumulation of alien species worldwide. Nat. Commun. 8, 14435 (2017).
Crutzen, P. J. & Stoermer, E. F. The “Anthropocene”. Global Change Newslett. 41, 17–18 (2000).
Crutzen, P. J. Geology of mankind. Nature 415, 23 https://doi.org/10.1038/415023a (2002).
Zalasiewicz, J. et al. When did the Anthropocene begin? A mid-twentieth century boundary level is stratigraphically optimal. Quaternary Int. 383, 196–203 (2015).
Hansen, J. E., Sato, M., Ruedy, R., Schmidt, G. A. & Lo, K. Global Temperature in 2018 and Beyond (2019). figshare https://doi.org/10.1029/2018JD029522. http://data.giss.nasa.gov/gistemp/; http://www.columbia.edu/~mhs119/Temperature
NASA, 2019, figshare https://climate.nasa.gov/vital-signs/global-temperature/
Schweiger, A., Zhang, J., Lindsay, R., Steele, M. & Stern, H. Polar Science Center (2019). figshare http://psc.apl.uw.edu/research/projects/arctic-sea-ice-volume-anomaly/
NSIDC (2019). figshare http://nsidc.org/arcticseaicenews/
Bamber, J. L., Westaway, R. M., Marzeion, B. & Wouters, B. The land ice contribution to sea level during the satellite era. Environ. Res. Lett. 13, 063008 (2018).
Mouginot, J. et al. Forty-six years of Greenland Ice Sheet mass balance from 1972 to 2018. Proc. Natl Acad. Sci. USA 116, 9239–9244 (2019).
Rignot, E. et al. Four decades of Antarctic Ice Sheet mass balance from 1979–2017. Proc. Natl Acad. Sci. USA 116, 1095–1103 (2019).
Church, et al. Sea level change. In Climate Change 2013: The Physical Science Basis. Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change, (eds. Stocker, T. F., et al.) (Cambridge University Press, Cambridge, UK and New York, NY, USA, 2013).
NASA, figshare https://climate.nasa.gov/vital-signs/sea-level/ Satellite data 1993-2018, Data source: Satellite sea level observations (2018).
Oppenheimer, M. et al. Sea level rise and implications for low-lying islands, coasts and communities. In IPCC Special Report on the Ocean and Cryosphere in a Changing Climate (eds. H.-O. Pörtner, et al.), (IPCC, Geneva, 2019).
Orr, J. C. et al. Anthropogenic ocean acidification over the twenty-first century and its impact on calcifying organisms. Nature 437, 681–686 (2005).
Chen, C.-T. A. et al. Deep oceans may acidify faster than anticipated due to global warming. Nat. Clim. Change https://doi.org/10.1038/s41558-017-0003-y (2017).
IPCC, IPCC Special Report on the Ocean and Cryosphere in a Changing Climate (eds. H.-O. Pörtner, et al.) (IPCC, Geneva, 2019).
Syvitski, J. P., Zalasiewicz, J. & Summerhayes, C. Changes to Holocene/Anthropocene patterns of sedimentation from terrestrial to marine, In The Anthropocene as a Geological Time Unit: A Guide to the Scientific Evidence and Current Debate (eds. Zalasiewicz, J., Waters, C., Williams, M. & Summerhayes, C.) (Cambridge Univ. Press, Cambridge, 2019).
Steffen, W., Broadgate, W., Deutsch, L., Gaffney, O. & Ludwig, C. The trajectory of the Anthropocene: the Great Acceleration. Anthropocene Rev. https://doi.org/10.1177/2053019614564785 (2015).
Bornmann, L. & Mutz, R. Growth rates of modern science: a bibliometric analysis based on the number of publications and cited references. J. Assoc. Info. Sci. Tech. 66, 2215–2222 (2015).
Day, J. et al. The energy pillars of society: Perverse interactions of human resource use, the economy, and environmental degradation. Biophys. Econ. Resource Qual. 3, 2 https://doi.org/10.1007/s41247-018-0035-65 (2018).
Zanna, L., Khatlwala, S., Gregory, J. M., Ison, J. & Helmbach, P. Global reconstruction of historical ocean heat storage and transport. Proc. Natl Acad. Sci. USA 116, 1126–1131 (2019).
Schmidt, G. A., Ruedy, R. A., Miller, R. L. & Lacis, A. A. Attribution of the present‐day total greenhouse effect. J. Geophys. Res. 115, D20106 (2010).
Gruber, N. & Galloway, J. N. An Earth-system perspective of the global nitrogen cycle. Nature 451, 293–296 (2008).
Fowler, D. et al. The global nitrogen cycle in the twenty-first century. Philos. Trans. R. Soc. B Biol. Sci. 368, https://doi.org/10.1098/rstb.2013.0164 (2013).
Erisman, J. W. et al. Consequences of human modification of the global nitrogen cycle. Philos. Trans. R. Soc. B Biol. Sci. 368, https://doi.org/10.1098/rstb.2013.0116 (2013).
Vitousek, P. M. et al. Human alteration of the global nitrogen cycle: sources and consequences. Ecol. Appl. 7, 737–750 (1997).
Galloway, J. N. The global nitrogen cycle. Treatise Geochem. 10, 475–498 (2013).
Galloway, J. N. & Cowling, E. B. Reactive nitrogen and the world: 200 years of change. AMBIO: J. Hum. Environ. 31, 64–71 (2002).
Schlesinger, W. H. On the fate of anthropogenic nitrogen. Proc. Natl Acad. Sci. USA 106, 203–208 (2009).
Erisman, J.-W. Director, Louis Bolk Institute, Netherlands, personal communication (2016).
Cao, P., Lu, C. & Yu, Z. Historical nitrogen fertilizer use in agricultural ecosystems of the contiguous United States during 1850–2015: application rate, timing, and fertilizer types. Earth Syst. Sci. Data 10, 969–984 (2018).
Zhang, J. et al. Natural and human-induced hypoxia and consequences for coastal areas: synthesis and future development. Biogeosciences 7, 1443–1467 (2010).
Holtgrieve, G. W. et al. A coherent signature of anthropogenic nitrogen deposition to remote watersheds of the northern hemisphere. Science 334, 1545 (2011).
Wolfe, A. P. et al. Stratigraphic expressions of the Holocene–Anthropocene transition revealed in sediments from remote lakes. Earth Sci. Rev. 116, 17–34 (2013).
Vörösmarty, C. et al. Anthropogenic sediment retention: major global-scale impact from the population of registered impoundments. Glob. Planet. Change 39, 169–190 (2003).
Best, J. Anthropogenic stresses on the world’s big rivers. Nat. Geosci. 12, 7–21 (2019).
Grill, G. et al. Mapping the world’s free-flowing rivers. Nature 569, 215–221 (2019).
Syvitski, J. P. M., Vörösmarty, C., Kettner, A. J. & Green, P. Impact of humans on the flux of terrestrial sediment to the global coastal ocean. Science 308, 376–380 (2005).
Milliman, J. D. & Farnsworth, K. L. River discharge to the coastal ocean: a global synthesis. (Cambridge Univ. Press, Cambridge, 2011).
Syvitski, J. P. M. & Milliman, J. D. Geology, geography and humans battle for dominance over the delivery of sediment to the coastal ocean. J. Geol. 115, 1–19 (2007).
Beiser, V. The World in a Grain. (Riverhead Books, NY, 2018).
BTS Public road and street mileage in the United States by type of surface. Publ. Bureau of Transportation Statistics (2019). https://www.bts.gov/archive/publications/national_transportation_statistics/2000/1-4
IRF WRS (2019). https://www.worldroadstatistics.org/contents.html
Cooper, A. H., Brown, T. J., Price, S. J., Ford, J. R. & Waters, C. N. Humans are the most significant global geomorphological driving force of the 21st century. Anthropocene Rev. 5, 222–229 (2018).
Bauerman, H. Coal. In Encyclopædia Britannica (ed. Chisholm, H.) 6 (11th ed.) (Cambridge Univ. Press, Cambridge 1911).
Nriagu, J. O. Global inventory of natural and anthropogenic emissions of trace metals to the atmosphere. Nature 279, 409–411 (1979).
Nriagu, J. O. & Pacyna, J. M. Quantitative assessment of worldwide contamination of air, water and soils by trace elements. Nature 333, 134–139 (1988).
Klee, R. J. & Graedel, T. E. Elemental cycles: a status report on human or natural dominance. Annu. Rev. Environ. Resources 29, 69–107 (2004).
Chen, W. Q. & Graedel, T. E. Anthropogenic cycles of the elements: a critical review. Environ. Sci. Technol. 46, 8574–8586 (2012).
Sen, I. S. & Peucker-Ehrenbrink, B. Anthropogenic disturbance of element cycles at the Earth’s surface. Environ. Sci. Technol. 46, 8601–8609 (2012).
Gordon, R. B., Bertram, M. & Graedel, T. E. Metal stocks and sustainability. Proc. Natl Acad. Sci. USA 103, 1209–1214 (2006).
Lifset, R. J., Gordon, R. B., Graedel, T. E., Spatari, S. & Bertram, M. Where has all the copper gone: the stocks and flows project, part 1. J. Mineral Metals Mater. Soc. 54, 21–26 (2002).
Graedel, T. E. & Cao, J. Metal spectra as indicators of development. Proc. Natl Acad. Sci. USA 107, 20905–20910 (2010).
Thorne, R. J., Pacyna, J. M., Sundseth, K. & Pacyna, E. G. Fluxes of trace metals on a global scale. In The Encyclopedia of the Anthropocene. (eds. DellaSala, D. A. & Goldstein, M. I.) Vol. 1, 93–102 (Oxford: Elsevier 2018).
Gordon, R. B. et al. The characterization of technological zinc cycles. Resources Conserv. Recycl. 39, 107–135 (2003).
Montgomery, D. R. Soil erosion and agricultural sustainability. Proc. Natl Acad. Sci. USA 104, 133268–133272 (2007).
Walling, D. E. & Fang, D. Recent trends in the suspended sediment loads of the world’s rivers. Glob. Planet. Change 39, 111–126 (2003).
Restrepo, J. D. & Syvitski, J. P. M. Assessing the effect of natural controls and land use change on sediment yield in a major Andean river: the Magdalena drainage basin, Colombia. Ambio 35, 65–74 (2006).
Wang, H. et al. Recent changes of sediment flux to the western Pacific Ocean from major rivers in East and Southeast Asia. Earth Sci. Rev. 108, 80–100 (2011).
Hooke, R. L. On the history of human as geomorphic agents. Geology 28, 843–846 (2000).
Wilkinson, B. H. & McElroy, B. J. The impact of humans on continental erosion and sedimentation. Bull. Geol. Soc. Am. 119, 140–156 (2007).
Borrelli, P. et al. An assessment of the global impact of 21st century land use change on soil erosion. Nat. Commun. 8, 2013 (2017).
Gu X. et al. Intensification and expansion of soil moisture drying in warm season over Eurasia under global warming. JGR Atmos. https://doi.org/10.1029/2018JD029776 (2019).
Heller, M. & Keoleian, G. Life cycle-based sustainability indicators for assessment of the U.S. food system. (Univ. Michigan Center for Sustainable Systems, Ann Arbor, pub. CSS00-04, 2000).
Hamilton, A., Balogh, S., Maxwell, A. & Hall, C. Efficiency of edible agriculture in Canada and the U.S. over the past three to four decades. Energies 6, 1764–1993 (2013).
Voldner, E. C. & Li, Y. F. Global usage of toxaphene. Chemosphere 27, 2073–2078 (1993).
Schenker, U., Scheringer, M. & Hungerbühler, K. Investigating the global fate of DDT: model evaluation and estimation of future trends. Environ. Sci. Technol. 42, 1178–1184 (2008).
Davis, F. R. Insecticides, agriculture, and the Anthropocene. Glob. Environ. 10, 114–136 (2017).
Bogdal, C. et al. Blast from the past, melting glaciers as a relevant source for persistent organic pollutants. Environ. Sci. Technol. 43, 8173–8177 (2009).
McCulloch, A., Midgley, P. M. & Ashford, P. Releases of refrigerant gases (CFC-12, HCFC-22 and HFC-134a) to the atmosphere. Atmos. Environ. 37, 889–902 (2003).
UN Global Mercury Assessment 2018, UN Environment Programme Chemicals and Health Branch. (Geneva, Switzerland, 2019).
Klimont, Z. et al. Global anthropogenic emissions of particulate matter including black carbon. Atmos. Chem. Phys. 17, 8681–8723 (2017).
Novakov, T. et al. Large historical changes of fossil‐fuel black carbon aerosols. Geophys. Res. Lett. 30, 1324 https://doi.org/10.1029/2002GL016345 (2003).
Rose, N. L. Spheroidal carbonaceous fly-ash particles provide a globally synchronous stratigraphic marker for the Anthropocene. Environ. Sci. Technol. 49, 4155–4162 (2015).
Syvitski, J. P. M. et al. Dynamics of the coastal zone. In Global fluxes in the Anthropocene. (eds. Crossland C. J. et al.) (Springer Publ., Berlin, 2005).
Syvitski, J. P. M. et al. Sinking deltas due to human activities. Nat. Geosci. 2, 681–689 (2009).
Higgins, S., Overeem, I., Tanaka, A. & Syvitski, J. P. M. Land subsidence at aquaculture facilities in the Yellow River delta, China. Geophys. Res. Lett. 40, 3898–3902 (2013).
Tessler, Z. et al. Profiling risk and sustainability in coastal deltas of the world. Science 349, 638–643 (2015).
Davidson, N. C. How much wetland has the world lost? Long-term and recent trends in global wetland area. Marine Freshw. Res. 65, 934–941 (2014).
Davidson, N. C., Fluet-Chouinard, E. & Finlayson, C. M. Global extent and distribution of wetlands: trends and issues. Marine Freshw. Res. 69, 620–627 (2018).
Zalasiewicz, J. et al. The geological cycle of plastics and their use as a stratigraphic indicator of the Anthropocene. Anthropocene 13, 4–17 (2016).
Geyer, R., Jambeck, J. R. & Law, K. L. Production, use, and fate of all plastics ever made. Sci. Adv. 3, e1700782 (2017).
Zalasiewicz, J., Gabbott, S. E. & Waters, C. N. Chapter 23: Plastic waste: how plastic has become part of the Earth’s geological cycle. In Waste: A Handbook for Management (eds. Letcher, T. M. & Vallero, D. A.) 2nd Ed. (Elsevier, New York, 2019).
Cuthbert, L. Our addiction to plastic. Natl. Geogr. 2019, 68–81 (2019).
Jambeck, J. R. et al. Plastic waste inputs from land into the ocean. Science 347, 768–771 (2015).
Bergmann, M. et al. White and wonderful? Microplastics prevail in snow from the Alps to the Arctic. Sci. Adv. 5, eaax1157 (2019).
Hazen, R. M., Grew, E. S., Origlieri, M. J. & Downs, R. T. On the mineralogy of the “Anthropocene Epoch”. Am. Mineral. 102, 595–611 (2017).
Heaney, P. J. Defining minerals in the age of humans. Am. Mineral. 102, 925–926 (2017).
Waters, C. N. & Zalasiewicz, J. Concrete: the most abundant novel rock type of the Anthropocene. Reference Module in Earth Systems and Environmental Sciences https://doi.org/10.1016/B978-0-12-409548-9.09775-X (2017).
Ritchie, H. & Roser, M. CO2 and greenhouse gas emissions. Our World in Data https://ourworldindata.org/co2-and-other-greenhouse-gas-emissions (2019).
UN Resumed Review Conference on the Agreement Relating to the Conservation and Management of Straddling Fish Stocks and Highly Migratory Fish Stocks. Publ. United Nations Department of Public Information DPI/2556 D (2010).
McCauley, D. J. et al. Marine defaunation: animal loss in the global ocean. Science 347, 1255641 (2015).
Bar-On, Y. M., Phillips, R. & Milo, R. The biomass distribution on Earth. Proc. Natl Acad. Sci. USA 115, 6506–6511 (2018).
Barnosky, A. D. Colloquium paper: megafauna biomass tradeoff as a driver of Quaternary and future extinctions. Proc. Natl Acad. Sci. USA 105, 11543–11548 (2008).
Erb, K.-H. et al. Unexpectedly large impact of forest management and grazing on global vegetation biomass. Nature 553, 73–76 (2017).
Rodhe, H. Human impact on the atmospheric sulfur balance. Tellus 51, 110–122 (1999).
Brimblecombe, P. The global sulfur cycle. Treatise Geochem. 10, 559–591 (2013).
Gunn, J. Forced Innovation: The Sudbury, Canada example. In Environmental Reality: Rethinking the Options (eds. Kessler, E. & Karlqvist, A), 47–51. (Royal Swedish Academy of Sciences Press, Stockholm, 2017).
Yuan, Z. et al. Human perturbation of the global phosphorus cycle: changes and consequences. Environ. Sci. Technol. 52, 2438–2450 (2018).
Filippelli, G. M. The global phosphorus cycle: past, present, and future. Elements 4, 89–95 (2008).
Chen, M. & Graedel, T. E. A half-century of global phosphorus flows, stocks, production, consumption, recycling, and environmental impacts. Glob. Environ. Change 36, 139–152 (2016).
Seebens, H. et al. Global rise in emerging alien species results from increased accessibility of new source pools. Proc. Natl Acad. Sci. USA 115, E2264–E2273 (2018).
Schmidt, C. et al. Recent invasion of the symbiont-bearing foraminifera Pararotalia into the Eastern Mediterranean facilitated by the ongoing warming trend. PLoS ONE 10, e0132917 (2015).
Aldridge, D. C., Elliott, P. & Moggridge, G. D. The recent and rapid spread of the zebra mussel (Dreissena polymorpha) in Great Britain. Biol. Conserv. 119, 253–261 (2004).
Cohen, A. N. & Carlton, J. T. Accelerating invasion rate in a highly invaded estuary. Science 279, 555–557 (1998).
Witt, A. B. R., Kiambi, S., Beale, T. & Van Wilgen, B. W. A preliminary assessment of the extent and potential impacts of alien plant invasions in the Serengeti-Mara ecosystem, East Africa. Koedoe 59, 1–16 (2017).
Yang, Q.-Q., Liu, S.-W., He, C. & Yu, X.-P. Distribution and the origin of invasive apple snails, Pomacea canaliculata and P. maculata (Gastropoda: Ampullariidae) in China. Sci. Rep. 1185 https://www.nature.com/articles/s41598-017-19000-7 (2018).
McGann, M., Sloan, D. & Cohen, A. N. Invasion by a Japanese marine microorganism in western North America. Hydrobiologia 421, 25–30 (2000).
Eichler, P. P. B. et al. The occurrence of the invasive foraminifera Trochammina hadai Uchio in Flamengo inlet, Ubatuba, Sao Paulo State, Brazil. Micropalaeontology 64, 391–402 (2018).
Waters, C. N. et al. Can nuclear weapons fallout mark the beginning of the Anthropocene Epoch? Bull. Atomic Sci. 71, 46–57 (2015).
UNSCEAR Sources and Effects of Ionizing Radiation. Volume 1, UNSCEAR Report to the General Assembly, New York http://www.unscear.org/unscear/en/publications/2000_1.html (2000).
Choppin, G., Liljenzin, J.-O., Rydberg, J. & Ekberg, C. Behavior of radionuclides in the environment. In Radiochemistry and Nuclear Chemistry (Academic Press, Cambridge, 2013).
Taylor, D. M. Environmental plutonium-creation of the universe to twenty-first century mankind. Radioactiv. Environ. 1, 1–14 (2001).
Hancock, G. H., Tims, S. G., Fifield, L. K. & Webster, I. T. The release and persistence of radioactive anthropogenic nuclides. In A Stratigraphical Basis for the Anthropocene (eds. Waters, C. N., Zalasiewicz, J. A., Williams, M., Ellis, M. A. & Snelling, A. M.) 265–281 (Geological Society, London, Special Publications, 2014).
Ellis, E. C. & Ramankutty, N. Putting people in the map: anthropogenic biomes of the world. Front. Ecol. Environ. 6, 439–447 (2008).
Ellis, E. C. Anthropogenic transformation of the terrestrial biosphere. Philos. Trans. R. Soc. A 369, 1010–1035 (2011).
Halpern, B. S. et al. Spatial and temporal changes in cumulative human impacts on the world’s ocean. Nat. Commun. 6, 7615 (2015).
WWF, Staggering extent of human impact on planet (2018). https://www.worldwildlife.org/press-releases/wwf-report-reveals-staggering-extent-of-human-impact-on-planet
IPBES, Global Assessment Report on Biodiversity and Ecosystem Services (2019). https://ipbes.net/global-assessment-report-biodiversity-ecosystem-services
Zalasiewicz, J. et al. Scale and diversity of the physical technosphere: a geological perspective. Anthropocene Rev. 4, 9–22 (2017).
Steffen, W. et al. Stratigraphic and Earth System approaches to defining the Anthropocene. Earth’s Future 4, 324–345 (2016).
Steffen, W. et al. Trajectories of the Earth System in the Anthropocene. Proc. Natl Acad. Sci. USA 115, 8252–8259 (2018).
Steffen, W. et al. The emergence and evolution of Earth System Science. Nat. Rev. 1, 54–63 (2020).
Waters, C. N. et al. Global Boundary Stratotype Section and Point (GSSP) for the Anthropocene Series: where and how to look for potential candidates. Earth Sci. Rev.178, 379–429 (2018).
Carpenter, S. R. & Bennett, E. M. Reconsideration of the planetary boundary for phosphorus. Environ. Res. Lett. 6, 014009 (2011).
Ellsworth, W. Injection-induced earthquakes. Science 341, https://doi.org/10.1126/science.1225942 (2013).
Contributing authors are mainly members of the Anthropocene Working Group (AWG), of the Subcommission on Quaternary Stratigraphy (SQS), a component body of the International Commission on Stratigraphy (ICS). We thank Paul Crutzen for his initiatives, beginning with the International Geosphere-Biosphere Programme and later the AWG, in pioneering the Anthropocene narrative upon which this paper builds. We thank colleagues M. Storozum, L. Edwards, and H. Haberl for their guidance in our paper’s data presentation.
The authors declare no competing interest.
Peer review information Primary handling editor: Joe Aslin
Publisher’s note Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
The original online version of this article was revised: Full information regarding the change(s) made can be found in the correction for this article.
About this article
Cite this article
Syvitski, J., Waters, C.N., Day, J. et al. Extraordinary human energy consumption and resultant geological impacts beginning around 1950 CE initiated the proposed Anthropocene Epoch. Commun Earth Environ 1, 32 (2020). https://doi.org/10.1038/s43247-020-00029-y
This article is cited by
Nature Reviews Earth & Environment (2022)
Anthropocene Science (2022)
A Method of Evaluating Safe Operating Space: Focus on Geographic Regions, Income Levels and Developing Pathway
Environmental Management (2022)
npj Urban Sustainability (2021)
Non-uniform tropical forest responses to the ‘Columbian Exchange’ in the Neotropics and Asia-Pacific
Nature Ecology & Evolution (2021)