Paleoclimatology

From abundant geological evidence, we know that only three hundred and fifty years ago, the world was in the depths of a prolonged cold spell called the "Little Ice Age," which lingered for nearly 500 years. Fifty thousand years ago, in the middle of the last glacial period, large continental ice sheets covered much of North America, Northern Europe, and Northern Asia. Fifty million years ago, global temperatures were so high that there were no large ice sheets at all.

The speed at which climate can change has also recently become clear: Transitions between fundamentally different climates can occur within only decades. In order to understand these variations, we need to reconstruct them over a wide range of temporal and geographical scales. The importance of this task is underlined by the growing awareness of how profoundly human activity is affecting climate. As with so many other complex systems, the key to predicting the future lies in understanding the past

We need to ask several questions: What happened? Why did it happen? Has it happened before? Will is happen again? How do we know about it in the first place?

Paleoclimatology
This is the study of past climates. It is a fascinating, multidisciplinary field, combining history, anthropology, archaeology, chemistry, physics, geology, atmospheric, and ocean sciences. Clues about past climate conditions are obtained from proxy indicators, types of evidence that can be used to infer climate. These include:

Isotopic Geochemical Studies: The study of rock isotopic ratios, ice core bubbles, etc.

Isotope Geochemistry
The most important of these for the study of long term change involves isotope geochemistry. We have already discussed the importance of isotopes for rock dating purposes; the carbon-14 radiometric technique, for example, can date as far back as 60,000 years. However, there is another important use of isotopic ratio measurements using oxygen that is not dependent on radioactivity, but rather on the interaction between life processes and isotopes.

Oxygen is composed of 8 protons, and its most common form as 8 neutrons, giving it an atomic weight of 16 (16O) and is also known a "light" oxygen. A small fraction of oxygen atoms have 2 extra neutrons and a resulting atomic weight of 18 (18O), known as "heavy" oxygen. 18O, is a rare form, with about 1 in 500 atoms of O being heavy.

The ratio of these two oxygen isotopes has changed over the ages and these changes are a proxy to changing climate in two ways:

Climate Temperature from Ice Cores
Ice in glaciers has an increased proportional abundance of heavy oxygen if it was deposited during relatively warm periods. To understand why this might be so, we need to think about the process of glacier formation. The water-ice in glaciers originally came from the oceans as vapor, later falling as snow and becoming compacted in ice. When water evaporates, the heavy water (H218O) is left behind and the water vapor is enriched in light water (H216O). This is simply because it is harder for the heavier molecules to overcome the barriers to evaporation. Thus, glaciers are relatively enhanced in 16O, while the oceans are relatively enriched in 18O. This imbalance is more marked for colder climates than for warmer climates. In fact, it has been shown that a decrease of one part per million 18O in ice reflects a 1.5°C drop in air temperature at the time it originally evaporated from the oceans.

While there are complexities with the analysis, a simple measurement of the isotopic ratio of 18O in ice cores can be directly related to climate. Ice cores from Greenland are layered, and the layers can be counted to determine age. The heavy oxygen ratio can then be used as a thermometer of old climate.

Climate Temperatures from Ocean Sediments
Shells of dead marine organisms are made up of calcium carbonate (CaCO3). The oxygen in the carbonate reflects the isotopic abundance in the shallow waters where the creatures lived. Thus if we can find and date ever more ancient sediments made up of old sea shells, we can determine the isotopic ratio of oxygen and infer the sea surface temperature at that time. The more 18O found in the sediment, the colder the climate (inverse relationship to that of glacier ice).

Many ice cores and sediment cores have been drilled in Greenland, Antarctica and around the world's oceans. These cores are actively studied for information on variations in Earth's climate.

The most commonly used indicators include pollen, faunal and floral remains, sediment types or composition and geomorphological features indicating physical conditions. In the ocean, indicators such as microplankton, pollen, and sediments settle to the sea floor, where they accumulate to provide a nearly continuous record of climate for millions of years.

Limitations in Reconstructing Paleoclimates
The limitations in this process result from uncertainties associated with dating the proxy indicators or other evidence. There are two fundamental types of dating:

Absolute dating
Techniques that identify the actual geological time represented by the evidence. Techniques are limited and rely predominately on evaluating the amount of decay of naturally occurring radioactive isotopes.

Relative dating
Techniques that are able to differentiate time relative to other points in time. Stratigraphy establishes a relative sequence of events or characteristics within which the evidence lies. If this same sequence can be identified in multiple locations it can be used to establish the relationship between locations and the relative timing of the indicators.

Current Climate
Climate differs from weather in that it provides a statistical view of seasonal and daily weather events over a long term period. Thus, for example, the passage of a frontal system over Ann Arbor is weather event, while the daily average number of such passages for the month of July (averaged over several years) is part of the climate record.

Climate records are most often expressed in terms of temperatures, winds, precipitation, and pressures - all parameters that can be measured at multiple sites around the globe. Over the years a large data base of weather event measurements has been obtained, leading to a good description of today's climate.

We find that climate varies widely around the globe - we have deserts and rain forests, ice caps and "death valleys". As for most subjects discussed in this course, there is a taxonomy of sub-disciplines and we can speak of the following:

The many factors that control local climates include: intensity of overhead sun - including its latitudinal variation; the distribution of land and water; ocean currents; prevailing winds; positions of semi-permanent high- and low-pressure areas; mountain barriers; altitude. The effects of these controls can be seen in global patterns of temperature and precipitation.

Great differences in climate occur from place to place, even within the continental United States which only accounts for about 2% of the Earth's surface. In 1918, a popular climate terminology was developed by Koppen and is called the Koppen System. It is based on annual and monthly average temperature and precipitation measurements, using evidence from vegetation where data is sparse.

Current Trends
The global average surface temperature has increased by 0.6 ±0.2°C since the late 19th century. It is very likely that the 1990s was the warmest decade and 1998 the warmest year in the instrumental record since 1861.

Most of the increase in global temperature since the late 19th century has occurred in two distinct periods: 1910 to 1945 and since 1976. The rate of increase of temperature for both periods is about 0.15°C/decade. Recent warming has been greater over land compared to oceans; the increase in sea surface temperature over the period 1950 to 1993 is about half that of the mean land-surface air temperature. The high global temperature associated with the 1997 to 1998 El Niño event stands out as an extreme event, even taking into account the recent rate of warming.

Summary