Introduction to Biological Oceanography Department of Oceanography Dalhousie

Introduction to Biological Oceanography Department of Oceanography, Dalhousie University Spring, 2004 Marlon R. Lewis Lecture: Biogeochemical Cycles

Readings (Required): Falkowski, P. G. , R. T. Barber, V. Smetacek. 1998. Biogeochemical controls and feedbacks on ocean primary production. Science 281: -200 -206

The Sun’s fusion reactions provide the energy necessary for the physical, chemical and biological processes on Earth. Our sun should have begun rather small and dim and grown in diameter through time. The amount of sunlight reaching the Earth should thus have increased by some 15% to 30% since the earth formed some 4. 5 billion years ago. If nothing else was different than today, this would mean the surface of the earth world have changed in temperature tremendously, and no liquid water could have been present on the Earth prior to 2 billion years ago. However, we see instead by looking at the geological record, that there has been liquid water on the earth since it its crust solidified, and in general the Earth's surface seems to have remained within a surprisingly narrow range. Why is that?

The answer has everything to do with the presence of carbon dioxide in the atmosphere. Here is what’s happened over the last 40 years: What causes annual fluctuations? Seasonal cycle of photosynthesis and the asymmetry in land mass area between the northern and southern hemispheres. What causes the longterm trends? You and Me.

More recent correlations:

What we do know: We know that atmospheric CO 2 is increasing. We know that anthropogenic emissions of CO 2 are increasing. We know the radiative properties of CO 2 quite well. And we know the radiative properties of other “greenhouse” gasses (e. g. methane) well. All else equal, this should translate into warmer Earth. But…. all else is not equal, and a better understanding of global biogeochemical cycles, particularly carbon, is needed to assist in accurate prediction of future habitability of the Earth.

Where is the carbon today? Reservoirs Sub-Reservoir Atmosphere Biota 720 Land Oceans (dissolved) Sediments Amount (10^15 g C) 827 2 38, 000 Organic Matter 15, 000 Carbonate Rocks 20, 000

Two kinds of biogeochemical cycles maintain the Earth's atmospheric levels of CO 2: fast and slow. The fast cycle operates on time scales of hundreds to thousands of years. The second operates on hundred of thousands to millions of years. Both are essential, but are often confused.

First, the fast cycle The critical chemical reactions are: Photosynthesis and Respiration: CO 2 + H 20 + e- = CH 2 O + O 2 Carbonation: CO 2 + H 2 O = H 2 CO 3 = H+ + HCO 3 Calcium Carbonate dissolution and precipitation: Ca 2+ + 2 HCO 3 - = Ca. CO 3 + H 2 O + CO 2 Carbonate equilibrium in seawater: H 2 CO 3 = H+ + CHO 3 - = H+ + CO 32 Photosynthesis and respiration are the clear controllers of the seasonal cycle of CO 2. Note also that any carbon not immediately respired results in the accumulation of O 2 in the atmosphere. We have O 2 in the atmosphere because of the C buried as organic matter in sediments and rocks.

A negative feed back loop keeps O 2 levels from getting too high: If O 2 levels get too high, land biomass will burn and photosynthesis will go down, and O 2 will go down. Also the more carbon is buried, the more nutrients are buried, putting another brake on the system. CO 2 in the atmosphere is in equilibrium with the ocean. The ocean has a vast amount of carbon in it in the form of carbonate (CO 32 -), and bicarbonate (HCO 3 -). Over hundreds to thousands of years, adding more CO 2 to the atmosphere is just sucked up by the ocean, lowering the p. H and thus producing more bicarbonate to neutralize it from carbonate thus driving the equilibrium equation back towards the acid side. Lowering atmospheric CO 2 has the opposite effect, and results in the precipitation of Ca. CO 3. Because the ratio of ocean C to atmospheric C is about 50 to 1, doubling or tripling atmospheric CO 2 does little to the oceans or the net atmospheric CO 2 on the long run. The only reason we are having an effect on the atmosphere is because the RATE of the input exceeds that of the removal by the oceans! Over thousands of year our contribution to the atmosphere via fossil fuel burning would be nil. And I kinda liked the greenhouse effect….

Why is the atmosphere at 250 -350 ppm instead of other amounts? This must be a function of the amount of carbonate in the oceans. That is controlled by the long term cycle of carbon. Thus, the burial of organic carbon and carbonate carbon (ocean biology) are the controllers of O 2 in the atmosphere and the carbonate pool in the oceans, respectively. The latter controls the CO 2 in the atmosphere. Because of plate tectonics nearly all of this buried carbon is returned via subduction and metamorphism over about 200 million years. In total about 0. 2 x 10^15 g of C is buried each year and just about that is returned by outgassing.

In the above diagram, Corg is organic carbon, primarily the breakdown products of carbohydrates produced by photosynthesis. THUS, THE ATMOSPHERIC CO 2 IS JUST WHAT REMAINS BETWEEN THE OUTGASSING CO 2 FROM IGNEOUS AND METAMORPHIC SOURCES AND CONSUMPTION OF CO 2 BY PHOTOSYNTHESIS AND WEATHERING. The most important lesson of all this, is that, the composition of the Earth's atmosphere is constantly maintained by life.

OK, in the long run, no worries (and I was hoping for a “Costa del Newf”). But what about short-time scale (100’s of years) variability? The buried Corg is being removed to fuel our houses, cars etc. , and advancing the geochemical cycle. Exchange of atmospheric CO 2 with the oceans proceeds at a much faster rate. The sea takes up CO 2 in its surface layer, and slower processes then exchange some of this CO 2 with deeper waters and ocean sediments. Much of the carbon residing in the shallow oceans is in the form of dissolved CO 2. The capacity of ocean water to store dissolved CO 2 is diminished as the water temperature increases. This constitutes a positive feedback mechanism whereby an increase in global temperature results in more atmospheric CO 2, which results in an increase in global temperature, etc.

Much of the exchange of carbon between ocean and atmosphere is (in the short term – see above), purely physical/chemical. This is called the solubility pump. It is quite active in areas where deep water is formed, for example in the North Atlantic. But what about the short term biological impacts? Here, the nutrient cycles, and in particular vertical exchange of nutrients between surface and deep ocean, play a role. It is complicated.

The distribution of the marine phytoplankton is not uniform over the global ocean. This leads to questions: A. What limits the growth and accumulation of biomass in the world’s oceans? B. What are the consequences for fluxes and distributions of biogeochemical compounds? C. How do these processes translate into higher trophic levels, and fluxes to the sea bottom?

Photosynthesis mg. C (mg Chl)-1 h-1 Hypothesis: A large body of evidence leads to the conclusion that light limits the growth of phytoplankton. The distribution of phytoplankton should reflect the distribution of light. “High Light” Cells “Low Light” Cells Irradiance (mmol quanta m-2 s-1)

Well…looks like light kills phytoplankton. Hypothesis rejected

Maximum Growth Rate (d-1) Hypothesis: There is also evidence leads to the conclusion that higher temperatures enhance the growth of phytoplankton. The distribution of phytoplankton should reflect the distribution of surface temperature. Temperature (o. C)

SST Looks like phytoplankton have a low boiling point. Hypothesis rejected.

Well, its not light, not temperature, what could it be? Mar. Aug. Perhaps something to do with the fluid dynamical environment? Mixed Layer Depths

But how might this translate into biological production? Annual “average” surface nitrate concentration. Vigorous fluid mixing introduces a net flux of nitrate (read nutrients) into the surface, well-lit layer.

Solubility Pump Biological Pump NO 3 - CO 2

Explain this one!

How about this?

OK, how about these?

Conclusions: The chemistry of ocean, atmosphere, and land, is largely related to biological oceanographic processes, on both short and long time-scales. The chemistry of carbon, which concerns us quite a bit due to its increases and radiative properties, is intimately tied up with cycles of major (nitrate, phosphate, silicate) and minor (e. g. iron) nutrients. In turn, the supply of these nutrients, which control the biological processes, is controlled by the physical oceanography…which in turn is related to the air-sea heat exchange…which is related to atmospheric radiation…. which is related to biological production…Gaia lives!