Module 7 Part II The Carbon Cycle Chapter 8 Carbon on Earth The Chemistry of Carbon Biotic carbon Abiotic carbon Highly organized molecules within living things After life they become disorganized goo – called kerogen, or humic acids Terrestrial Planets Venus, Earth, and Mars All three planets had about the same amount of carbon: Venus has the carbon content in it’s very dense atmosphere of carbon dioxide and sulfuric acid Earth has the highest concentration of carbon in limestone and rocks Mars has it’s carbon locked up in the polar ice caps that are carbon dioxide dry ice Organic Carbon The backbone of life A means of storing energy Photosynthesis, carbon dioxide, water, and sunlight produces plants that store energy as food The early plants were converted to fossil fuels – more stored energy as fuel instead of food Oxidation states, electron bookkeeping Methane is totally reduced carbon, has an oxidation state of -4 To calculate oxidation states we assign the common states to hydrogen and oxygen, then realize that the molecule has to be neutral, so the leftover number is assigned to carbon Hydrogen is +1, there are four of them in methane, so the carbon must be -4 This is fully reduced carbon Reduced carbon is easily oxidized CH4 + 2 O2 → CO2 + 2 H2O Oxidized carbon CO2 is fully oxidized The oxidation number for carbon is +4 We calculate this by assigning -2 to each oxygen (Group 16 in the periodic table, needs two more electrons) Oxygen is -4, so carbon must be +4 Oxidized carbon is stable, low energy, and the preferred state for carbon Oxidized carbon will not become reduced carbon without a great deal of effort In between is the carbohydrates, where carbon has a zero oxidation state CH2O formaldehyde, is the simplest carbohydrate. O is -2, H is +1(x2) so C must be in the 0 oxidation state Carbon forms Photosynthesis uses oxidized carbon to reduce the carbon to carbohydrates We use carbohydrates as fuel and oxidize the carbohydrate back to CO2 when we exhale during respiration Animals are not the only organisms to breathe! The Land Breathes The land inhales CO2 in the summertime growing season and exhales during the winter months Reversed in the Southern Hemisphere where there is less land The land breathes on an annual cycle The Ocean Breathes The carbon is inorganic, and stable, it involves the carbonate buffer system that we will study in chapter 10, this is called dissolved inorganic carbon The ocean effects atmospheric CO2 on time scales of centuries The glacial-interglacial cycles were amplified somehow by the ocean carbon cycle. The Rocks Breathe The sedimentary rock carbon pool is larger than the ocean, land or atmospheric pools Carbon in the solid Earth exists as limestone CaCO3, and to a lesser extent, organic carbon Most of the organic carbon in sedimentary rocks is kerogen Kerogen is useless as a fossil fuel because it is too diluted The solid Earth is the largest but slowest breathing of the carbon reservoirs The Atmosphere is the Grand Central Station for the CO2 Cycles Glacial-Interglacial Cycles The beat of the ice-age rhythm apparently originates from variation in the Earth’s orbit around the sun The orbit varies through three main cycles, and the orbital variations drive climate by changing the distribution of sunlight at the Earth’s surface 1. Precession Cycle 2. Obliquity Cycle 3. Eccentricity Cycle Precession The axis of rotation spins like a wobbly top Called the precession of season, or the precession of the equinoxes Completes the entire circle in 20,000 years Solar heat influx variability comes from precession Seasonal cycle in the North is weakened and in the South it is intensified because the Earth is closest to the sun in the winter season in the northern hemisphere Precession orbital cycle Obliquity The angle of the pole of rotation relative to the plane of Earth’s orbit Varies between 22 and 25.5 degrees Angle of tilt is currently 23.5 degrees Cycle time is 41,000 years The impact of obliquity on solar heating is strongest in the high latitudes Obliquity of Earth’s Orbit Eccentricity The third cycle involves how elliptical the orbit of the Earth is The eccentricity of the orbit has cycles of 100,000 and 400,000 years At present the orbit of Earth is nearly circular The orbital cycles affect climate by redistributing the energy from one place to another and from one season to another Milankovitch cycles The CO2 Thermostat At the cool surface of the Earth, oxidized carbon wants to be calcium carbonate – limestone In the hot interior of the Earth, oxidized carbon wants to be free, as CO2 The CO2 thermostat regulates atmospheric CO2 and climate on geologic time scales of hundreds of thousands of years It is possible to change the set point of the thermostat, creating a hot house world like that of the dinosaurs, or an icy world like today The thermostats of Venus and Mars are broken Take home points of chapter 8 1. the most stable form of carbon on Earth is oxidized. Photosynthesis stores energy from the sun by producing organic carbon, which is the backbone of life 2. There is less carbon in the atmosphere that any other carbon reservoir. These other reservoirs tug on atmospheric CO2 seasonally for the land, and on glacial interglacial 100,000 year time scales from the ocean 3. The weathering of igneous rocks on land controls the partial pressure of CO2 in the atmosphere on million year time scales. The thermostat is broken on Venus because no water, and on Mars because there is no volcanic activity left. Chapter 9 Fossil Fuels and Energy Energy All energy comes from the stars, Mostly from our sun Previous definition: watts = joules/second terawatts = 1012 watts, written TW 1,000,000,000,000 watts Energy sources Wind (Denmark) Hydroelectric (2% globally) Solar Biomass energy Energy sources Renewable Geothermal Solar Wind Wood Waste electric power Non-renewable Fossil fuels Radioactive elements Fossil Fuels “Only a small fraction of the buried organic carbon is in a convenient form for fuel” Traditional fossil fuels Largest reservoir is coal: it was produced in swamps where the organic material was protected from the atmosphere by water Freshwater has less sulfur, burns “cleaner” Saltwater swamps contains sulfur, burns to forms aerosols and produce acid rain as sulfuric acid Coal Begins as plant material (carbon based) Carbon Peat Coal By a pressure and temperature process that takes millions of years. The oldest coal is the cleanest coal. “Coal is the most abundant fossil fuel, and the future of the Earth’s climate depends mostly on what happens to that coal” Coal in power plants Coal fired power plants are established They produce cheap energy Would be very expensive to replace with a cleaner fuel source until the necessity arises “Oil is probably the most convenient but the least abundant of the fossil fuels, so it is the most expensive.” Source of oil Organic rich sediments buried 2-5 km 50 – 150 ° C Temperature and pressure converts some of the organics to oil Higher temperatures produce natural gas, mostly methane Only a tiny fraction of the oil and gas produced can be harvested Oil is the most expensive Oil fuels the transportation industry More energy per weight than any battery (so far) Convenient liquid form as opposed to: Coal, not used in transportation since the steam engine Natural gas which must be a pressurized container Sources Traditional: Oil fields – pumped from under ground or water largest fields in Saudi Arabia, and in Kuwait Non-traditional: Oil shales – low grade fuel for power plants, Estonia produces about 70% Tar sands – requires steam (Canada) How long will it last? We have differing opinions here: The oil industry has been saying forty years for a long time but new sources and initiatives keep adding time. “There is enough oil to keep pumping for decades, but the peak rate of oil extraction could be happening right now.” Natural gas Coal – solid Oil – liquid Natural gas – gas usually in the form of methane CH4 Energy of methane “Methane carries more energy per carbon that the others because methane is the most chemically reduced form of carbon.” Reduced form + oxygen → oxidized form + water Along with a release of energy (the ability to do work). Global sources of Energy in 2001 Biggest users of energy China India Brazil U.S. France Denmark Japan Energy consumption per dollar GPD (Gross Domestic Productivity). Energy Consumption per person U.S. Japan France Denmark Brazil China India Source? U.S. Japan France Denmark Brazil China India petroleum, gas, coal petroleum, gas, coal petroleum, gas, coal petroleum, gas, coal petroleum, gas, coal coal, petroleum, gas coal, petroleum, gas New coal plants China and India are building new coal fired plants at an alarming rate. http://ingienous.com/?page_id=8399 Bottom Line “Coal is the form of fossil fuel with the potential of increasing the temperature past the turning point of 2° C. The future of the earth depends most on what happens to that coal.” Take home points, Chapter 9 Ultimately, the energy available to humankind includes instantaneous solar energy, which is abundant but spread out; stored solar energy is in the form of fossil fuels; and stored solar energy from stellar explosions in the form of radioactive elements. Of the fossil fuels, coal is the most abundant. Oil may run out in the coming decades, and the peak rate of oil extraction may be upon us even now. continued…. We can project energy demand in the future as the product of population, economic growth, and energy efficiency. Chapter 10 The Perturbed Carbon Cycle The atmosphere ain’t what it used to be! Ozone Three oxygen atoms Very reactive O2 bonds break with UV-c, forming O free radical, recombines with an O2 to form O3 Stratospheric O3 absorbs (filters) UV-b radiation, forming O2 Montreal Protocol 1987 Phased out production and release of chlorofluorocarbons because it breaks down stratospheric ozone (Freon, aerosol propellants, refrigerants) Asthma and allergy suffers feel it, plant leaves get burned and scarred Stratospheric Ozone Is a Good thing CO2 in the stratosphere sheds heat as IR to space The ozone depletion causes cooling in the stratosphere Result: the stratosphere is cooling Surface/tropospheric Ozone Tropospheric ozone comes from several sources. Biomass burning and industrial activity produce carbon monoxide (CO) and volatile organic compounds (VOCs) which are oxidized to form ozone. Nitrogen oxides (NOx) from industrial processes, biomass burning, automobile exhaust and lightning also form tropospheric ozone. A small amount of tropospheric ozone also comes from the stratospheric ozone layer. http://earthobservatory.nasa.gov/Features/Aura/Images /TroposphericOzone_HiRes.jpg Ozone Ozone Hole Ozone hole located over Antarctica is a different problem than the ozone as a greenhouse gas HNO3 acid clouds react with chlorine, which in turn, consumes the ozone Satellite was programmed to throw out data that violated common sense, so the hole was a surprise Revisiting discarded satellite data revealed that the hole had been growing for some time Methane Natural Sources Human Sources Wetland degradation Termites Organic carbon in freshwater swamps Energy emissions Landfills – “swamp gas” Ruminant animals Rice agriculture Biomass burning Methane Clathrates – Fire Ice http://www.youtube.com/watch?v=U46XOoU0DrM Overall human impact has doubled since pre-human levels CH4 is responsible for 25% of anthropogenic greenhouse heat trapping Carbon Dioxide Methane is transient, but CO2 accumulates Background levels were around 280 ppm until ~ 1750, coinciding with the New World, “pioneer effect” Deforestation for agriculture and development is one source of atmospheric CO2 The second source is fossil fuel combustion CO2 and CH4, 1000 years Atmospheric CO2 CO2 is complicated, and the atmosphere is the exchange place for the three remaining carbon reservoirs Land cycles annually Oceans cycle by centuries or more Rock cycles by millennia or more The Missing Sink Deforestation releases about 1.5 Gtons C /year Fossil fuels release about 8.5 Gtons C /year Release is about 10 Gtons C /year Atmospheric levels are rising by about 4 Gtons C /year Mathematically we are missing about 6 Gtons C /year There is a missing carbon sink – about 6 Gtons /year Terrestrial Carbon Sink The measurements are variable The research indicates that the land is taking up the missing carbon Studies conclude that the “missing sink” is located in the high latitudes of the northern hemisphere CO2 Fertilization Higher concentrations of CO2 encourages plants to grow faster (greenhouses) The growth is an initial spurt, and tends to level off Higher CO2 concentrations fro plants means less water loss when plants open the stomata to take in the CO2 Respiration in Soils As organic carbon is oxidized to CO2, the soil releases the CO2 Warmer soils decompose faster Tropical soils contain very little carbon The permafrost is full of carbon As soils warm, the CO2 emissions get higher Ocean uptake CO2 Ultimately the fossil fuel CO2 will be cleaned up by the oceans 60 years ago, scientists thought it would be a quick process 50x more CO2 in the ocean 70% of the Earths surface, average 4 km deep But… The surface of the ocean limits the contact between the atmosphere and the deep ocean The ocean uptake of fossil fuel carbon depends on circulation Ocean ventilation – at high latitudes the cold water sinks and takes gases with it – it takes centuries to make the loop Also… The thermocline is a few hundred meters deep, and the ventilation to the atmosphere is a few decades The surface ocean mixed layer (driven by the wind) is about 100 meters deep and ventilation to the atmosphere is annually Buffer chemistry of inorganic carbon In seawater, freshwater lakes, rivers, reservoirs, swimming pools and human blood The major ions in seawater are Na+, Mg2+, Ca2+, K+, Sr2+, Cl-, SO42- (sulfate), HCO3- (bicarbonate), Br-, B(OH)3 (boric acid), and F-. Together, they account for almost all of the salt in seawater. Carbonate/bicarbonate buffer Atmospheric CO2 dissolves in seawater and is hydrated to form carbonic acid, H2CO3. Carbonic acid is diprotic; that is, it can undergo two de-protonation reactions to form bicarbonate (HCO3-), and carbonate (CO32-). The coexistence of these species in seawater creates a chemical buffer system, regulating the pH and the pCO2 of the oceans. Most of the inorganic carbon in the ocean exists as bicarbonate (~88%), with the concentrations of carbonate ion and CO2 comprising about 11% and 1%, respectively. http://oceancolor.gsfc.nasa.gov/SeaWiFS/TEACHERS/CHEMISTRY/ What does that mean? pH reactions, CO2 reacts with H2O to form carbonic acid (carbonated soda drinks) CO2 + H2O H2CO3 Carbonic acid loses a hydrogen, forms an acidic proton and bicarbonate (hydrogen carbonate) H2CO3 H+ + HCO3 Hydrogen carbonate loses the second acidic proton and forms more acid and the carbonate ion HCO3- H+ + Co32- Lets Assume We can ignore the tiny input of the Hydrogen ion and recombine the equations to show and easier illustration of le Châtelier’s principal CO2 + CO32- + H2O 2 HCO31% 11% 88% Any additional CO2 is reacted with the carbonate ion to produce the hydrogen carbonate ion pH Chemistry A bucket of seawater can absorb or release more CO2 because of the pH chemistry The buffer stabilizes the pH and the concentrations of the CO2 The amount of CO2 that can be absorbed depends on the concentration of the carbonate It is about 11% and CO2 is about 1%, so it works well This buffer system also keeps your blood pH in balance Perturbation If you perturb, stress, or change the system, it will react in such a way to relieve the perturbation, stress, or change in the system – it will reach a new equilibrium le Châtelier’s Principle Le Châtelier's Principle states that if a dynamic equilibrium is disturbed by changing the conditions, the position of equilibrium moves to counteract the change. In other words, look at the equation, if you add products, it will shift to reactants If you take away reactants, it will shift to reactants It will shift to overcome the stress Seawater pH The relative concentrations of carbon dioxide and carbonate ion in seawater determine its pH Fossil fuel CO2 makes seawater more acidic The buffer helps resist the change in pH Life forms in the ocean that make their shells out of CaCO3 will suffer at lower pH Think of putting baking soda (sodium bicarbonate) into vinegar (a weak acid) and watch the CO2 fizz out Equilibrium Models Eventually after a long period of time, the CO2 will spread out among the carbon reservoirs of the atmosphere, ocean and land surface Models indicate that the atmospheric levels of CO2 will be higher than before the CO2 was released Eventually the budget for dissolved CaCO3 in the ocean has to balance As the buffer chemistry recovers, atmospheric CO2 drops Recovery The climate cycle will ultimately recover from the fossil fuel era when the carbon returns to the solid Earth as a result of the silicate weathering CO2 thermostat from Chapter 8. How long? First we have to stop adding CO2 to the atmosphere. The longevity of the global warming climate event stretches out into time scales of glacial – interglacial cycles, time scales that are longer than the age of human civilization. Take home points, chapter 10 The ozone hole problem is not the same as global warming. They are different issues. Methane has about a 10 year lifetime in the atmosphere, so its concentration reaches an equilibrium after about this long. The land surface and the ocean are absorbing some of our fossil fuel CO2, but this could slow or reserve in a changing climate. Releasing fossil CO2 to the atmosphere will affect climate for hundreds of thousands of years – as far as we are concerned, forever.