Global Warming

Climate Climate: the average weather conditions over a period of years in a particular place Climate is influenced by a variety of processes, including geologic processes –Volcanism –Sea-floor spreading –Configuration of landmasses due to plate tectonics Climate changes impact geologic processes –Rates of erosion and deposition –Types of sediments deposited and sedimentary rocks formed –Geomorphology (surface features) –Fossil record

The Climate System Multidimensional System, many interacting parts Atmosphere, hydrosphere, geosphere, biosphere, and cryosphere Exchange of energy and moisture

The Climate System

Paleoclimatology – the study of past climates. Earth’s climate varies in cyclical fashion over a number of time-scales The study of natural climate processes is important to understand the role of humans in climate change. Scientists measure climate change in the past in many different ways, depending on the time- scale.

Paleoclimatology – Study of past climates What can paleoclimatology tell us about climate change that is relevant to society in the future?

Is the last century of climate change unprecedented relative to the last 500, 2000, and 20,000 years? Do recent global temperatures represent new highs, or are they just part of a longer cycle of natural variability? Is the recent rate of climate change unique to the present or was it commonplace in the past? Can we find evidence in the paleoclimate record for mechanisms or climate forcings that could be causing recent climate change?

Proxy Climate Indicators Instrumental records (from thermometers, rain gauges, etc.) only exist for the last 150 years. Proxy climate indicators provide indirect indications of climate change. These include: –Seafloor Sediments –Oxygen Isotopes –Glacial Ice Cores –Corals –Pollen –Historical Data

Proxy climate indicators and their useful time range

Climate Data from Historical Records Wine is a serious business in Europe! Careful records of the first day of the grape harvest in Europe have been kept since the 14 th century. Trends in these records show changes in climate, as the harvest started earlier or later in the year.

Tree rings Trees can live for thousands of years. The width of tree rings provides information about growing conditions, including temperature conditions and CO 2 concentrations.

Oxygen Isotope Analysis One of the most important ways that proxy data indicators reveal climate information is through the use of oxygen isotope analysis.

Oxygen Isotope Analysis Isotope – varieties of an element with different numbers of neutrons, resulting in different atomic masses. The most common isotope of oxygen has an atomic mass of 16 and is called 16 O. A heavier, less common variant is 18 O. Both occur naturally, and neither is radioactive. You breathe both kinds. Both isotopes bond with 2 hydrogen atoms to make water, H 2 O. Water made of 16 O evaporates more easily. Water made of 18 O condenses more easily. 18 O has two extra neutrons

Oxygen Isotope Analysis During colder weather, more light 16 O evaporates, leaving ocean water with more heavy 18 O. This oxygen is incorporated into coral, plankton shells and sediments at the ocean bottom. In colder climates, these proxy indicators will be enriched in 18 O. The ratio of 18 O to 16 O, (δ 18 O) can be correlated to temperature. For benthic (deep-water sediments), colder temperatures are related to higher values of δ 18 O.

Reading the Graph Horizontal (x) axis: Note older data as you move right. Left vertical (y) axis - δ 18 O ratios. A value of zero indicates the “standard” value for ocean water. The higher the value, the more 18 O, and the colder the ocean waters. Note colder is down on this graph. Right vertical (y) axis - ∆T (temperature difference from “normal” annual average ocean temperature) Zero (dashed line) indicates “normal”.

Conversely, glacial ice cores are made of evaporated water that precipated. Precipitation water always has a negative value of of δ 18 O. Colder temperatures are related to lower (negative values) of δ 18 O. The arrow points to a sudden cooling event that occurred over 10, 000 years ago, known as the Younger Dryas Event. Oxygen Isotope Analysis

Great website explaining oxygen isotope analysis aleoclimatology_OxygenBalance/

Left: The type of fossil can indicate the temperature range in ocean waters. Their shells can be analyzed chemically to measure CO 2 concentrations and oxygen isotope ratios Oxygen isotope analysis (below): the ratio of O-18 (heavier, less common) to O-16 (lighter, more common) is a proxy measurement of temperature.

Ice Cores – a very valuable proxy data indicator Ice cores have annual rings, like trees, so age of core can be determined Air bubbles trapped in the ice can be analyzed for oxygen-isotope data, carbon dioxide concentration, presence of aerosols etc. The ice itself can be melted and analyzed for these proxy data indicators.

Vostok Ice Core Data This is partial data from an ice core from Antarctica. Temperature data from oxygen/hydrogen isotopes. Interglacial” is a warm period between ice ages. Peak of last ice age about 20,000 years ago.

The modern atmosphere Two most abundant gases: –78% N 2 –21% O 2 Less abundant gases (< 1%) –Argon –Water vapor –CO 2 (only about.035%) It’s up to almost.040% now! Non-gaseous components –water droplets –dust, pollen, soot and other particulates

Fig. 17.6, p.437

Thermal Structure of Atmosphere: Upper Layers Troposphere - Extends to about 12 km (40,000 ft) elevation. Where we live. Stratosphere – heated primarily by solar radiation –Ozone (O 3 ) layer absorbs UV energy, causing temperatures to rise –Above 55km (stratopause) temps fall again Mesosphere – thin air (can’t absorb energy), very cold up to 80km Thermosphere – above 80km, temps rise rapidly (to just below freezing!)

Solar Energy (Insolation) –Also called solar radiation, although NOT radioactive! –Composed of electromagnetic waves with different properties depending on wavelength, frequency Longwave (low frequency): includes heat (infrared), radio waves Shortwave (high frequency): includes visible light as well as ultraviolet, x rays, gamma rays Electromagnetic spectrum – shows EM wavelengths by frequency and wavelength.

Electromagnetic Spectrum

Solar Radiation in the atmosphere Reflection/scattering – bounces off with no effect Absorption – eventual re-emission in a different form

Reflection and Albedo Reflection–electromagnetic radiation bouncing of from a surface without absorption or emission, no change in material or energy wavelength Albedo – proportional reflectance of a surface –a perfect mirror has an albedo of 100% –Glaciers & snowfields approach 80-90% –Clouds – 50-55% –Pavement and some buildings – only 10-15% –Ocean only 5%! Water absorbs energy.

Typical Albedos of Materials on the Earth

Absorption and Emission Absorption of radiation – electrons of absorbing material are “excited” by increase in energy –Increase in temperature; physical/chemical change –Examples: sunburn, cancer Emission of radiation – excited electrons return to original state; radiation emitted as light or heat Earth absorbs short wave radiation from sun (i.e. visible light) and emits longwave (infrared or heat) into the atmosphere.

“Greenhouse gases” (water vapor, carbon dioxide, methane, etc.) let shortwave energy pass, but absorb longwave energy radiated upward by the Earth. The longwave energy is then re-radiated by the gases in all directions, some of it returning to the Earth’s surface.

The greenhouse effect keeps our atmosphere at a livable temperature of about 15 degrees C (59 degrees F). If all heat escaped, the average temperature of Earth would be about C (0 0 F).