There are 2 principal avenues of inquiry relevant to reconstructing the his
tory of the sulfur cycle. One avenue relies on the comparison of molecular
sequences derived fi om biologically essential proteins and genetic materia
l. Most sequence information is available from the small subunit of the rRN
A molecule and from these sequences a Tree of Life emerges providing a reco
nstruction of the evolutionary relationships among organisms. Near the root
of the tree are numerous bacteria(1)metabolizing sulfur species including
organisms living from dissimilatory elemental sulfur reduction, dissimilato
ry sulfate reduction, and anoxygenic photosynthesis. These metabolisms are
likely very ancient. Many of the deep-branching bacteria of the sulfur cycl
e are active at very high-temperatures (hyperthemophiles) and are commonly
found in modern sulfide-rich hydrothermal systems. One can imagine a primit
ive early Earth terrestrial ecosystem housed around active hydrothermal are
as with anoxygenic photosynthesis producing organic matter and oxidized sul
fur species. These oxidized sulfur species could have been used as electron
accepters in the mineralization of organic matter, completing the carbon c
ycle. The evolution of oxygenic photosynthesis provided for dramatically in
creased rates of carbon production, and a much wider range of ecosystems fo
r both carbon production, and carbon oxidation. Either associated with, or
following, the evolution of oxygenic photosynthesis is the emergence of lin
eages housing most of the bacteria of which we are familiar, including most
of the bacteria of the sulfur cycle.
The geologic record can provide direct evidence fbr the state of chemical o
xidation of the Earth-surface, with possible indications of when specific b
acterial metabolisms first occurred. We offer the following scenario for th
e evolution of the Earth-surface environment based on the available geologi
cal evidence. By 3.5 Ga anoxygenic photosynthesis was established and provi
ded a weak source of sulfate to the global ocean with sulfate concentration
s likely much less than 1 mM. In some instances locally high concentrations
of sulfate could accumulate and precipitated as evaporitic sulfate mineral
s. There is no compelling evidence for sulfate reduction at this time. The
first evidence for sulfate reduction is found between 2.7 and 2.5 Ga, and t
he first evidence for oxygen production by oxygenic photosynthesis is found
at around 2.8 Ga. Even so, levels of seawater sulfate remained low, below
I mM, and did not increase to >1 mM until around 2.3 Ga This increase in su
lfate levels may have been promoted by a rise in atmospheric oxygen concent
ration at this time. Throughout the Archean and early Proterozoic the deep
oceans contained appreciable concentrations of dissolved ferrous iron, and
banded iron formations (BIFs) were a common form of chemical sediment.
Sulfate levels increased slowly, and by 1.8 Ga sulfate concentrations were
sufficient to increase rates of sulfate reduction to greater than the deliv
ery flux of iron to the oceans. Sulfide accumulated and precipitated ferrou
s iron from solution. It is proposed that the oceans remained sulfide-rich
until the Neoproterozoic, where renewed deposition of banded iron formation
s occurred at around 0.75 Ga. It is possible that during the Neoproterozoic
, decreased carbon production resulted from an ice covered "Snowball Earth"
reducing rates of sulfate reduction below rates of iron delivery to the oc
eans, promoting BIF formation. At around this time high carbon burial rates
increased levels of atmospheric oxygen to >10 percent present-day levels,
promoting the widespread oxidation of marine surface sediments and an evolu
tionary radiation of sulfide oxidizing bacteria.