Russian State Agrarian University of KA Timiryazev, Moscow, Russia
Received date: December 27, 2016; Accepyed date: December 28, 2016; Published date: December 30, 2016
Citation: Ivlev AA (2016) Comments on the Role of Photosynthesis in the Global Redox Carbon Cycle. J Ecosys Ecograph 6:e125. doi: 10.4172/2157-7625.1000e125
Copyright: © 2016 Ivlev AA. This is an open-access article distributed under the terms of the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original author and source are credited.
Visit for more related articles at Journal of Ecosystem & Ecography
In a recently published works devoted to the global redox cycle of carbon [1-3], some points require further explanation. Applied to the global carbon cycle term “photosynthesis” should be understood more broadly as “global photosynthesis” what is somewhat different from normal photosynthesis of individual organisms.
Global photosynthesis is the term describing the cumulative photosynthesis all organisms living at the moment on the Earth. In contrast to the photosynthesis of individual organisms, global photosynthesis is not limited by ontogenesis and doesn't depend on time. Photosynthesis conditions for each habitat on the Earth are regarded as unchangeable.
However, "global photosynthesis" has the same features that characterize a normal photosynthesis. It consists of two reciprocal processes of CO2 assimilation and photorespiration. The strengthening of one of them is accompanied by the weakening of the other. The effect of each of the processes on the total biomass growth is opposite and depends on the concentration ratio of the CO2 and O2 in the environment. The increase of CO2 concentration enhances the CO2 assimilation and supplies the total biomass growth whereas the increase in oxygen concentration stimulates photorespiration and reduces the total biomass.
Like a normal photosynthesis, global photosynthesis is accompanied by carbon isotope fractionation. CO2 assimilation is followed by the enrichment of the total biomass in a "light" isotope 12C relative to the assimilated carbon, while photorespiration leads to the enrichment of the total biomass in a "heavy" isotope 13C. The carbon isotope composition of the total biomass depends on the relative contribution of the two above processes to the biosynthesis. The increase in the concentration of CO2 in the environment leads to the enrichment of the biomass with 12C, whereas the O2 growth in the atmosphere provides 13C enrichment of the total biomass.
We also used the term “living matter”, introduced by Vernadsky, which includes the total biomass of all living organisms, including photosynthesizing ones. Taking into account that photosynthesizing biomass is the first unit of the food chain, the “living matter” can be regarded as a product of photosynthesis and can be used in the photosynthesis reaction. The assertion is particularly true since it is known that carbon isotope fractionation in heterotrophic assimilation is negligible and isotope effect of “living matter” is mainly determined by photosynthesizing biomass.
When studying the global natural carbon cycle the isotope composition of carbonate carbon is usually applied as arguments to substantiate isotopic variations of CO2. The reason for this is isotopeexchange equilibrium observed in the modern natural “carbon dioxide – bicarbonate – carbonate” systems. Due to equilibrium the isotopic composition of carbonates reflects the changes of the isotopic composition of CO2. Similarly, the isotopic composition of organic matter of sedimentary rocks is considered to be analogous to the isotopic composition of contemporary "living matter".
Indeed, a rationale for this analogy is the fact that the sedimentary organic matter is a product of transformation of "living matter" and hence inherits its isotopic composition. Some differences between them can be explained by isotope heterogeneity of the "living matter" which is a result of intracellular isotope fractionation and subsequent partial oxidation of the fractions after burial. However, the associated isotopic shifts are insignificant.
If one takes into consideration the maximal isotopic differences observed between lipid - protein and carbohydrate fractions are around 5% (in most cases much less), and keep in mind that the range of isotopic differences related to the photosynthesis conditions in different ecosystems are up to 20% or more, it can be argued that the isotopic composition of sedimentary organic matter should be determined mainly by the photosynthesis conditions in the ecosystems. Following this logic and having compared the isotopic composition of carbon in carbonates and coeval organic matter sampled in the same facies (i.e., the same ecosystem), it can be claimed that the ε difference (δ13Ccarb - δ13Corg. matter) is analogous to the isotopic discrimination Δ13C, widely used for the characterization of carbon isotope fractionation in modern photosynthesizing organisms. In other words, the value of ε is the isotopic discrimination in photosynthetic organisms in the past. Another important conclusion derived from the above is the following: in the reaction of global photosynthesis sedimentary organic matter can be regarded as photosynthesis product whereas carbonates can be used instead of ??2 as substrate.
In conclusion one more assertion associated with regulatory role of photosynthesis in global carbon cycle should be underlined. As was said, the increase of oxygen in the environment causes the intensification of photorespiration in the photosynthesizing organism. It increases till the moment when photorespiration becomes equal to the ??2 assimilation. This state is called compensation point. With oxygen growth a photosynthesizing organism spontaneously strive to the compensation point. Below this point the physical existence of the organisms is impossible. Due to this ability of photosynthesizing organisms global photosynthesis has the same feedback mechanism which makes the global carbon cycle to move spontaneously to the point when the amount of the reduced carbon (the amount of total biomass produced in photosynthesis), becomes equal to the amount of the reduced organic carbon converting back into the oxidized inorganic form. This state is called ecological compensation point. Since the emergence of the photosynthesis and up to the achievement of ecological compensation point, the carbon balance was shifted to the production of the reduced carbon. It means that the excess of the reduced carbon was accumulated in sediments in the form of organic matter. Correspondingly another product of photosynthesis, oxygen, is accumulated in the atmosphere. Upon reaching the ecological compensation point the global carbon cycle reaches a steady state, in which there is a stabilization of oxygen and carbon dioxide concentrations in the atmosphere. Further accumulation of organic matter in sedimentary rocks is terminated. Orogenic cycles on the Earth that appeared with photosynthesis origin turned into climatic oscillations.