Dynamics and longevity of the Designing a dissimilatory iron magmatic system of Furnas volcano, reducer. Reconstitution of the Fe(III)- São Miguel, Azores reducing electron transport chain of
GERTISSER , J. L. GASPAR , J. M. PACHECO ,
Shewanella oneidensis MR-1 in Escherichia coli
1School of Physical and Geographical Sciences, Earth
GESCHER , C. CORDOVA-ARDY AND A. SPORMANN
Sciences and Geography, Keele University, Keele, ST5
Dept. of Civil and Environmental Engineering, Stanford
2Centro de Vulcanologia e Avaliação de Riscos Geológicos,
University, Stanford, USA (spormann@stanford.edu)
Universidade dos Açores, 9501-801 Ponta Delgada,
Universitaet Freiburg, Institut fuer Mikrobiologie, Freiburg,
Germany (johannes.gescher@biologie.uni-freiburg.de)
3Department of Earth Sciences, The Open University, Milton
Shewanellaoneidensis uses several electron acceptors to
support anaerobic respiration including soluble species and
Furnas is the easternmost of the three active trachytic
remarkably insoluble species such as iron(III) and
central volcanoes on the island of São Miguel, Azores. It is
manganese(IV) oxides. The pathway of electron flow from the
regarded as one of the most active and dangerous volcanoes in
cytoplasmic membrane to the outer membrane remains elusive
the Azores archipelago owing to a population of several
after years of research with different Shewanella species. We
thousand people living within the caldera and in the immediate
are pursuing a novel approach to identify the essential
vicinity of the volcanic complex. Throughout its history,
components of the electron transport chain by reconstituting
volcanic activity at Furnas has been essentially explosive but
the pathway for iron(III) reduction by S. oneidensis in
eruptive styles have varied from mild effusive activity to at
Escherichia coli. We generated a suitable E. coli strain as a
least two caldera-forming eruptions ~30,000 and 12,000-
platform for this work and integrated the central electron
transfer protein, CymA into the genome. CymA allows for
During the past 5,000 years, ten explosive eruptions
electron transfer from the cytoplasmic membrane to the
occurred at Furnas, which produced a total of ~0.9 km3 (DRE)
periplasmic space in Shewanella species. We showed (i) that
of fairly homogeneous trachytic magma. The deposits of these
the expressed CymA activity is growth supporting for E. coli,
eruptions are collectively referred to as Furnas A-J members
(ii) that CymA couples directly to the soluble fumarate
of the Upper Furnas Group [1,2]. The latest eruption (Furnas
reductase of S. oneidensis, and (iii) that CymA in vitro
J) occurred after the settlement of the Azores archipelago in
facilitates reduction of ferric citrate and the soluble quinone
1630 AD. Eruptions of the Upper Furnas Group were mainly
analog AQDS. Our generated E. coli strain is a dissimilatory
characterised by alternating episodes of magmatic and
iron reducer in that it can use ferric-NTA as a terminal
phreatomagmatic activity producing deposits of interbedded
electron acceptor during growth with glycerol as the sole
ash and lapilli that overlie the widespread Fogo A deposit
carbon and electron source. We could furthermore show
from adjacent Fogo volcano [3]. At least three of these
through in vitro assays that a direct interaction between CymA
eruptions, namely Furnas E, Furnas I and the 1630 AD event
and the periplasmic decaheme cytochrome MtrA from S.
(Furnas J), were accompanied by trachyte dome extrusion in
To develop a fuller understanding of the underlying
dynamics of the magma system of Furnas, we have investigated the whole-rock major and trace element geochemistry of the products of the Upper Furnas Group and the older caldera-forming events. These data are discussed together with U-Th-Ra isotopic disequilibria obtained on trachyte pumice clasts and lavas to place constraints on the dynamics and longevity of the magma system of Furnas. References [1] Guest et al. (1999), J. Volcanol. Geotherm. Res.92, 1-29 [2] Booth et al. (1978), Phil. Trans. Royal Soc. London 288,
[3] Cole et al. (1999), J. Volcanol. Geotherm. Res.92, 39-53.
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