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Astrophysical studies indicate that the luminosity of the Sun was much lower during Earth’s early history than it has been in the Phanerozoic. In fact, radiative output was low enough to suggest that all surface water on Earth should have been frozen solid during its early history, but evidence shows that it was not. The solution to this “faint young Sun paradox” appears to lie in the presence of unusually high concentrations of greenhouse gases at the time, particularly methane and carbon dioxide. As solar luminosity gradually increased through time, concentrations of greenhouse gases would have to have been much higher than today. This circumstance would have caused Earth to heat up beyond life-sustaining levels. Therefore, greenhouse gas concentrations must have decreased proportionally with increasing solar radiation, implying a feedback mechanism to regulate greenhouse gases. One of these mechanisms might have been rock weathering, which is temperature-dependent and serves as an important sink for, rather than source of, carbon dioxide by removing sizable amounts of this gas from the atmosphere. Scientists are also looking to biological processes (many of which also serve as carbon dioxide sinks) as complementary or alternative regulating mechanisms of greenhouse gases on the young Earth.
Photosynthesis and atmospheric chemistry
The evolution by photosynthetic bacteria of a new photosynthetic pathway, substituting water (H2O) for hydrogen sulfide (H2S) as a reducing agent for carbon dioxide, had dramatic consequences for Earth system geochemistry. Molecular oxygen (O2) is given off as a by-product of photosynthesis using the H2O pathway, which is energetically more efficient than the more primitive H2S pathway. Using H2O as a reducing agent in this process led to the large-scale deposition of banded-iron formations, or BIFs, a source of 90 percent of present-day iron ores. Oxygen present in ancient oceans oxidized dissolved iron, which precipitated out of solution onto the ocean floors. This deposition process, in which oxygen was used up as fast as it was produced, continued for millions of years until most of the iron dissolved in the oceans was precipitated. By approximately 2 billion years ago, oxygen was able to accumulate in dissolved form in seawater and to outgas to the atmosphere. Although oxygen does not have greenhouse gas properties, it plays important indirect roles in Earth’s climate, particularly in phases of the carbon cycle. Scientists are studying the role of oxygen and other contributions of early life to the development of the Earth system.
Snowball Earth hypothesis
Geochemical and sedimentary evidence indicates that Earth experienced as many as four extreme cooling events between 750 million and 580 million years ago. Geologists have proposed that Earth’s oceans and land surfaces were covered by ice from the poles to the Equator during these events. This “Snowball Earth” hypothesis is a subject of intense study and discussion. Two important questions arise from this hypothesis. First, how, once frozen, could Earth thaw? Second, how could life survive periods of global freezing? A proposed solution to the first question involves the outgassing of massive amounts of carbon dioxide by volcanoes, which could have warmed the planetary surface rapidly, especially given that major carbon dioxide sinks (rock weathering and photosynthesis) would have been dampened by a frozen Earth. A possible answer to the second question may lie in the existence of present-day life-forms within hot springs and deep-sea vents, which would have persisted long ago despite the frozen state of Earth’s surface.
A counter-premise known as the “Slushball Earth” hypothesis contends that Earth was not completely frozen over. Rather, in addition to massive ice sheets covering the continents, parts of the planet (especially ocean areas near the Equator) could have been draped only by a thin, watery layer of ice amid areas of open sea. Under this scenario, photosynthetic organisms in low-ice or ice-free regions could continue to capture sunlight efficiently and survive these periods of extreme cold.
Abrupt climate changes in Earth history
An important new area of research, abrupt climate change, has developed since the 1980s. This research has been inspired by the discovery, in the ice core records of Greenland and Antarctica, of evidence for abrupt shifts in regional and global climates of the past. These events, which have also been documented in ocean and continental records, involve sudden shifts of Earth’s climate system from one equilibrium state to another. Such shifts are of considerable scientific concern because they can reveal something about the controls and sensitivity of the climate system. In particular, they point out nonlinearities, the so-called “tipping points,” where small, gradual changes in one component of the system can lead to a large change in the entire system. Such nonlinearities arise from the complex feedbacks between components of the Earth system. For example, during the Younger Dryas event (see below) a gradual increase in the release of fresh water to the North Atlantic Ocean led to an abrupt shutdown of the thermohaline circulation in the Atlantic basin. Abrupt climate shifts are of great societal concern, for any such shifts in the future might be so rapid and radical as to outstrip the capacity of agricultural, ecological, industrial, and economic systems to respond and adapt. Climate scientists are working with social scientists, ecologists, and economists to assess society’s vulnerability to such “climate surprises.”
The Younger Dryas event (12,900 to 11,600 years ago) is the most intensely studied and best-understood example of abrupt climate change. The event took place during the last deglaciation, a period of global warming when the Earth system was in transition from a glacial mode to an interglacial one. The Younger Dryas was marked by a sharp drop in temperatures in the North Atlantic region; cooling in northern Europe and eastern North America is estimated at 4 to 8 °C (7.2 to 14.4 °F). Terrestrial and marine records indicate that the Younger Dryas had detectable effects of lesser magnitude over most other regions of Earth. The termination of the Younger Dryas was very rapid, occurring within a decade. The Younger Dryas resulted from an abrupt shutdown of the thermohaline circulation in the North Atlantic, which is critical for the transport of heat from equatorial regions northward (today the Gulf Stream is a part of that circulation). The cause of the shutdown of the thermohaline circulation is under study; an influx of large volumes of freshwater from melting glaciers into the North Atlantic has been implicated, although other factors probably played a role.
Paleoclimatologists are devoting increasing attention to identifying and studying other abrupt changes. The Dansgaard-Oeschger cycles of the last glacial period are now recognized as representing alternation between two climate states, with rapid transitions from one state to the other. A 200-year-long cooling event in the Northern Hemisphere approximately 8,200 years ago resulted from the rapid draining of glacial Lake Agassiz into the North Atlantic via the Great Lakes and St. Lawrence drainage. This event, characterized as a miniature version of the Younger Dryas, had ecological impacts in Europe and North America that included a rapid decline of hemlock populations in New England forests. In addition, evidence of another such transition, marked by a rapid drop in the water levels of lakes and bogs in eastern North America, occurred 5,200 years ago. It is recorded in ice cores from glaciers at high altitudes in tropical regions as well as tree-ring, lake-level, and peatland samples from temperate regions.
Abrupt climatic changes occurring before the Pleistocene have also been documented. A transient thermal maximum has been documented near the Paleocene-Eocene boundary (56 million years ago), and evidence of rapid cooling events are observed near the boundaries between both the Eocene and Oligocene epochs (33.9 million years ago) and the Oligocene and Miocene epochs (23 million years ago). All three of these events had global ecological, climatic, and biogeochemical consequences. Geochemical evidence indicates that the warm event occurring at the Paleocene-Eocene boundary was associated with a rapid increase in atmospheric carbon dioxide concentrations, possibly resulting from the massive outgassing and oxidation of methane hydrates (a compound whose chemical structure traps methane within a lattice of ice) from the ocean floor. The two cooling events appear to have resulted from a transient series of positive feedbacks among the atmosphere, oceans, ice sheets, and biosphere, similar to those observed in the Pleistocene. Other abrupt changes, such as the Paleocene-Eocene Thermal Maximum, are recorded at various points in the Phanerozoic.
Abrupt climate changes can evidently be caused by a variety of processes. Rapid changes in an external factor can push the climate system into a new mode. Outgassing of methane hydrates and the sudden influx of glacial meltwater into the ocean are examples of such external forcing. Alternatively, gradual changes in external factors can lead to the crossing of a threshold; the climate system is unable to return to the former equilibrium and passes rapidly to a new one. Such nonlinear system behaviour is a potential concern as human activities, such as fossil-fuel combustion and land-use change, alter important components of Earth’s climate system.
Humans and other species have survived countless climatic changes in the past, and humans are a notably adaptable species. Adjustment to climatic changes, whether it is biological (as in the case of other species) or cultural (for humans), is easiest and least catastrophic when the changes are gradual and can be anticipated to large extent. Rapid changes are more difficult to adapt to and incur more disruption and risk. Abrupt changes, especially unanticipated climate surprises, put human cultures and societies, as well as both the populations of other species and the ecosystems they inhabit, at considerable risk of severe disruption. Such changes may well be within humanity’s capacity to adapt, but not without paying severe penalties in the form of economic, ecological, agricultural, human health, and other disruptions. Knowledge of past climate variability provides guidelines on the natural variability and sensitivity of the Earth system. This knowledge also helps identify the risks associated with altering the Earth system with greenhouse gas emissions and regional to global-scale changes in land cover.
Stephen T. Jackson