GEOPHYSICAL RESEARCH LETTERS, VOL. 32, L23205, doi:10.1029/2005GL023403, 2005
Search for past life on Mars: Physical and chemical characterization of
minerals of biotic and abiotic origin: part 1 - Calcite
Fabien Stalport,1 Patrice Coll,1 Michel Cabane,2 Alain Person,3
Rafael Navarro González,1,4 Francois Raulin,1 Marie Jo Vaulay,5 Patrick Ausset,1
Chris P. McKay,6 Cyril Szopa,2 and John Zarnecki7
Received 16 August 2005; revised 25 October 2005; accepted 8 November 2005; published 15 December 2005.
[1] Several lines of evidence suggest that early Mars once
had liquid water on its surface, a denser atmosphere and a
mild climate. Similar environmental conditions led to the
origin of life on the Earth more than 3.5 billion years ago;
consequently, life might also have originated on Mars. The
Viking landers searched for evidence of organic molecules
on the surface of Mars, and found that the Martian soil is
depleted in organics at ppb levels at the landing sites. We
contend that inorganic compounds could give us interesting
clues as to the existence of possible biological activity in
future astrobiological missions to Mars. Consequently, we
have investigated the physical and chemical properties of
calcite, which could be expected on Mars because liquid
water was certainly present on the surface of early Mars and
carbon dioxide was abundant in its atmosphere. Calcite is
interesting because on Earth this mineral is produced by
abiotic processes as well as by biological activity. One may
suppose that crystalline defects and trace element in the
crystal lattice and the growth speed of biotic calcites must
indicate a difference between them and pure abiotic calcites.
We investigated twelve different terrestrial calcite samples
from various origins: biotic, diagenetic and abiotic. The
minerals were studied by X-ray diffraction and electron
scanning microscopy to determine their mineralogical and
chemical composition, and differential thermal analysis
coupled to thermogravimetric analysis (DTA-TG) to
determine their thermal behavior. Our results show that
the thermal degradation of abiotic calcite starts at a
temperature at least 40C higher than the degradation
temperature of any biotic calcite investigated. Consequently,
in the case of a Martian in-situ study or in a sample return
mission, the analysis of Martian minerals by DTA-TG
represents a promising approach to detect evidence of past
1
Laboratoire Interuniversitaire des Systèmes Atmosphériques (LISA),
Université Paris XII, Créteil, France.
2
Service d’Aéronomie du CNRS, SA/IPSL, Université Paris VI, Paris,
France.
3
Laboratoire de Géologie Sédimentaire, Université Paris VI, Paris,
France.
4
Formerly at Laboratorio de Quimica de Plasmas y Estudios
Planetarios, Universidad Nacional Autónoma de México, Mexico City,
Mexico.
5
Interfaces, Traitements, Organisation et Dynamique des Systèmes
(ITODYS), Université Paris VII, Paris, France.
6
Space Science Division, NASA Ames Research Center, Moffett Field,
California, USA.
7
Planetary and Space Sciences Research Institute, Open University,
Milton Keynes, UK.
Copyright 2005 by the American Geophysical Union.
0094-8276/05/2005GL023403$05.00
biological activity on Mars. Citation: Stalport, F., et al.
(2005), Search for past life on Mars: Physical and chemical
characterization of minerals of biotic and abiotic origin: part 1 Calcite, Geophys. Res. Lett., 32, L23205, doi:10.1029/
2005GL023403.
1. Introduction
[2] Environmental conditions favorable for the emergence of life similar to that on Earth must have been
present on Mars during the first hundred million years
after its formation, or even more recently [Ori, 1999].
These conditions included a dense atmosphere [Pollack et
al., 1987], liquid water on the surface and mild temperatures [Carr, 1986; Paige, 2005]. The first microorganisms may have been present on Earth under similar
environmental conditions as early as 3.8 billion years
ago [Schopf, 1993; Mojzsis et al., 1996]. Consequently, it
is possible that life originated on Mars just as it originated on primitive Earth.
[3] The principal objective of the two landers of the
Viking Mission was to search for evidence of biological
activity in the top layers of the Martian soil. Different
experiments for detecting present life were carried out, in
particular in terms of organic molecule detection (For
complete information, see Biemann et al. [1977], Oyama
and Berdahl [1977], Levin and Straat [1977], and Klein
[1979]). No organic molecule was detected at the landing
site; this put serious questions on the possibility of extent or
extinct life on Mars. Moreover the results of the exobiological experiments of the two Viking landers suggested the
presence of oxidants in the Martian soil (detected in the
atmosphere [Encrenaz et al., 2004] and assumed to exist in
the soil).
[4] Since Mars continues to be a relevant object of
astrobiological interest, there are several space missions
planned for the search of present and/or past life in the
subsurface [Cabane et al., 2004]. Following the difficulty of
detection of organic compounds on the surface of Mars, we
propose to evaluate the potential of inorganic compounds as
tracers of biological activity. In this paper we first focus on
carbonates, the presence of which are suggested because of
the past presence of liquid water and its atmosphere of CO2
[Owen, 1992]. Even if no large carbonate deposit has been
detected yet, carbonates were found to be part of the
Martian dust material [Bandfield et al., 2003], and the
analyses of several Martian meteorites pointed to their
presence which could be of Martian origin [McKay et al.,
1996]. The carbonates are interesting to study because on
Earth they are produced by abiotic processes but also by
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Table 1. Presentation of the Different Calcite Samples Studied and Their Originsa
Codes
Name
Origin
FBC1
MBC1
MBC4
MBC5
MBC6
DC1
DC2
DC4
DC6
DC8
AC3
AC5
sea urchin fossilized
oyster
tunicates
crab
alga
carbonate, Valley of the Moon
carbonate, Arecibo
carbonate, New Zealand
carbonate, Shakespeare Cliff
carbonate, Ardeche
calcite crystal
Iceland spar (calcite crystal)
Chile
France
France
France
France
Chile
Puerto Rico
New Zealand
England
France
France
France
X-Rays Diffraction Results
calcite
calcite
calcite, a few
calcite
calcite, a few
calcite, a few quartz
calcite
calcite, a few
calcite
calcite, a few
calcite
calcite
quartz
quartz
and feldspars
quartz
quartz
MEB Results
high magnesium
no
high magnesium
high magnesium
high magnesium
low magnesium
low magnesium
no data
no data
no
no
no
a
They present a large wide at the surface of the Earth. The FBC samples are fossil biotic calcites, the MBC samples are current biotic calcites (shells and
bacterial deposits). The DC samples are diagenetic calcites (carbonated rocks). The AC are abiotic calcites (crystals). Results of the analyses in X-ray
diffraction confirm the mineralogical composition of the samples: Some samples are very pure, others have low traces of parasitic minerals (quartz and
feldspar). Results of the scanning electron microscopy analysis show that biotic calcites are the only one to incorporate magnesium in their crystalline
structure whereas abiotic calcites are pure.
biologically induced or controlled mineralization [Mann,
2001]. Additionally the most primitive terrestrial organisms
on the Earth are biomineralized carbonates [Schopf, 1993;
Westall et al., 2004]. The hypothesized Martian carbonates
could have also been produced partially by biotic processes
in the case that even a primitive form of life had originated
there. Due to the short period of time during which any
hypothetical Martian life would have been able to appear
and be sustained, we assume that it was certainly only
represented by very primitive forms similar to the terrestrial
primitive forms. Thus a comparison of the signatures of
carbonate of biotic and abiotic origins represents an interesting approach for the detection of biological activity on
the surface of Mars.
2. Sample Description
[5] The present paper is devoted to a study of calcite,
CaCO3, a common mineral on Earth, that could be
present on Mars if one assumes the transformation of
gaseous CO2 into solid carbonates. Calcite can be formed
from three possible processes on Earth: a biotic process, a
diagenetic process and an abiotic process [Tucker and
Wright, 1990]. Many living organisms, eukaryotes and
prokaryotes, are able to biomineralize calcite by biologically induced or controlled mineralization. Carbonate
rocks like limestones are mainly produced on the oceanic
floor by precipitation of carbonates (mainly calcite) of
only biotic origin. Calcite is also produced by purely
chemical precipitation according to different processes
(magmatism, dissolution and precipitation, metamorphism,
hydrothermalism) which are completely independent of
the presence of life. Finally, calcite is also the result of
diagenesis. In this process biotic phases change by
mechanisms of dissolution-recrystallization adapting to
the new thermodynamic conditions of their new abiotic
environment. Thus diagenetic calcite structure will be a
mixing between biotic and abiotic calcite structure.
[6] Several samples were investigated (Table 1). They
were selected among fossil or contemporary specimen,
collected around the world, composed mostly of calcite.
They were grouped in three families, according to their
mode of formation. These are (i) biotic calcites, divided into
two subgroups, modern biotic calcites (MBC) and fossil
biotic calcites (FBC); (ii) diagenetic calcites (DC) and (iii)
abiotic calcites (AC).
3. Sample Preparation
[7] The minerals were ground in an agate mortar (size
grains <50mm). The chemical composition of the mortar
was selected to avoid any contamination of the sample.
Before the crushing of each sample, mortars were cleaned
with nitric acid in distilled water to dissolve possible grains
of previous samples, also to avoid any contamination.
4. Experimentation
[8] Three different analyses were carried out in all
samples:
[9] i- X-ray diffraction to determine the mineralogical
composition of the samples. The measurements were
achieved with a SIEMENS diffractometer (Cu Ka)
[10] ii- Electron scanning microscopy to estimate the
chemical elemental composition of calcite minerals. The
measurements were achieved with a JEOL microscope (type
JSM-6031-F)
[11] iii- Differential thermal analysis coupled with a
thermogravimetric analysis (DTA-TG) to compare thermal
degradations of the samples of biotic origin and abiotic
origin. Samples were heated in a DTA-TG SETARAM
92-10. The samples are deposited in an alumina crucible
(Al2O3) which is thermally inert: no transition phase nor
loss of mass. The inert reference is alumina (alumina
powder (Al2O3). The mass deposited in the crucible is 20
to 40 mg. The conditions of heating are 20C per minute
from ambient (25C) to 1000C under one bar of an inert
atmosphere of N2 circulating at the rate of 1 liter per minute
to evacuate formed gases (e.g. CO2) and to avoid their
accumulation. The sample mass losses are measured with a
microbalance.
5. Results and Discussion
[12] The samples were first analyzed with X-ray diffraction. The results are presented in Table 1. They are mainly
composed of calcite with traces (a few percent) of parasitic
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Figure 1. Mass loss (ML) of the different calcite samples
as a function of the temperature ML = (M/Mi) 1 with M
the sample masse at a given temperature and Mi, the initial
sample mass. Two domains are clearly highlighted according to the origin of the sample. The first one is the biotic
calcite domain in green, and the second one is the abiotic
calcite field in red. The temperature difference obtained
between the two fields is approximately 45C. The
diagenetic calcite mass losses (blue) occupy the space
between these two domains because they are intermediate
between calcites of biotic and abiotic origins.
minerals (quartz, feldspars). These low level ‘‘pollutants’’
have no major influence on the performed thermal analysis.
[13] The results of electron scanning microscopy are
presented in Table 1. It can be seen that the calcites of
abiotic origin are pure, whereas most of the biotic calcites
have magnesium in their crystalline structure. Biotic calcites
have in their crystal lattice a higher number of trace
elements and imperfections compared to abiotic calcites.
These defects are due to the growth speed of the biotic
calcite grains and the imperfections are due to substitutions
of calcium atoms by other chemical elements (magnesium
in this case). These defects and imperfections increase the
calcite crystal entropy and structurally weaken the calcite
[Astilleros et al., 2002].
[14] Differential thermal analysis is based on sample
heating. Thermogravimetry (TG) provides Quantification
of the sample mass loss and comparison of thermal degradations of the biotic samples with their abiotic equivalents.
If a biotic sample mineral has more trace elements and
imperfections in its crystal lattice it is more fragile structurally, and should then be thermally degraded at temperatures lower than an abiotic mineral.
[15] In theory, calcite mass losses begin at temperatures
between 700C and 950C. They are caused by the
decomposition of the calcite which releases CO2 under
its gaseous state and forms calcium oxide CaO. When the
temperature of 1000C is reached at the end of the
analyses, the reaction is total and the theoretical mass
loss by-production of CO2 for a pure calcite is approximately 44%. This endothermic reaction can be described
as following [L’vov et al., 2002].
CaCO3 ðsÞ ! CaOðsÞ þ CO2 ðgÞ
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[16] The data showing the mass loss of the sample
(emission of gaseous CO2) during the temperature increase
is shown in Figure 1, where mass loss (as a percentage) is
plotted as a function of temperature.
[17] Two domains are clearly highlighted according to
the origin of the sample. The first one corresponds to the
biotic calcite domain, both fossil and current, and the
second one to the abiotic calcite domain (respectively
displayed in green and red in Figure 1). These domains
have been bordered by oblique parallel lines (roughly
parallel to the average maximum mass variation). The
two domains defined by these lines are the biotic, lower
temperature, and abiotic, higher temperature. The temperature difference obtained between the two parallel lines is
approximately 45C, indicating a quite clear separation of
the areas. We also observe that the mass losses of the
diagenetic calcites occupies the space between these two
domains, which corresponds exactly to the definition of
diagenetization, namely they are intermediate between
biotic calcites and abiotic calcites. Moreover, it can be
observed that the diagenetic calcites are closer to the
abiotic domain, whereas the diagenetic calcites which
preserved a part of their biotic signature are closer to
the biotic domain border.
[18] For a more precise determination of the temperature difference between the two domains, mass loss data
are represented, as a function of the temperature T, as the
first derivative of the mass (dML/dT) (Figure 2). Hence
the maximum of each derivative curve represents the
inflection point of the original curve, i.e. the temperature
at which the mass loss rate is most significant. We can
then simply use these particular points to delineate the
different domains. The temperature difference between
biotic and abiotic domains is about 40C. Again, most
of the diagenetic calcites are found in the space between
these two domains (Figure 2).
[19] Biotic calcites are structurally more fragile than
abiotic calcites due to trace element (magnesium), crystal
Figure 2. First derivative of the calcite sample mass loss
according to the temperature (dML/dT = f(T)). The
temperature difference between the biotic domain (green)
and the abiotic domain (red) is approximately 40C
(materialized by the black vertical lines). The diagenetic
calcite (blue) occupies the space between these two domains
again.
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defects (sample MBC1 of biotic origin is a pure calcite
consequently its mass loss is due principally to crystal
defect) and speed growth. Finally two diagenetic calcite
samples are old biotic calcite deposits and their respective
mass losses are located at the border of the biotic domain.
This means that these samples preserved their biotic signature in spite of the circulation of fluids specific to terrestrial
conditions, which erase these biotic signatures by diagenesis. This result is encouraging for a possible preservation of
mineral biotic calcite structures at Mars for billion years, as
there are probably no fluid circulations on Mars because of
the low atmospheric pressure and minimal liquid water
activity.
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Wright, 1990]. However, the conservation of this original
mineralogy is often temporary: the fluid circulations (rain,
water) in the rock partially or entirely dissolve biotic
carbonates when they emerge. Vacuums are filled by
secondary precipitation of another mineral (abiotic calcite,
silica . . .). These fluid circulations are common in the
terrestrial subsoil but on Mars there are no fluid circulations
able to dissolve Martian subsoil biotic structures since the
loss of the atmosphere and liquid state water more 3 billion
years ago [Martineau and Pollard, 2003]. Thus hypothetical
biotic structures may be preserved on Mars even now, and
their presence may be deduced using simple techniques
such as DTA-TG, by measuring the temperatures at which
they break down, delivering gaseous CO2 under endothermic reactions.
6. Conclusion
[20] The principal aim of these experiments on carbonates was to propose an effective technique of analysis in
the characterization of samples of abiotic origin and possibly biotic origin on Mars and a simple technique of analysis
for future space missions.
[21] The technique of thermal analysis allows us to
observe a clear difference between carbonate samples of
biotic and abiotic origin. This work shows that the thermal
degradation of abiotic calcite occurs at a temperature at least
40C higher than the degradation of any biotic calcite. The
knowledge of the above biotic and abiotic limits can be used
to define the ‘degree of biomineralization’ of a given
sample, from highly diagenetized to fully biotic minerals.
It is easy to understand that the defects due to the fast
growth of the biotic carbonates, the substitution of calcium
atoms by other elements during this growth, increase their
fragility, hence their sensibility to thermal stresses. Consequently, in the case of a Martian in-situ or sample return
experiments, the techniques of thermal analyses DTA-TG
represent a promising approach to detect evidence of past
biological activity on Mars.
[22] Future studies will focus on carbonates linked to
primitive living organisms. These will include stromatolites
and microbialites, bacterial carbonate deposits that are the
oldest fossils of biological activity traces known on the
Earth. The second point will be the addition of more
carbonate references like aragonite. One extension of this
work will be to study other biomineralisation such as
nitrates, sulphates, phosphate, silica.
[23] A persistent question however concerns the preservation of biotic carbonates on Mars. Could biotic structures
of primitive organisms on Martian subsoil have been
preserved? Carbonates formed by an organism through
biologically induced or controlled mineralization have in
general a good potential of fossilization compared to organic
matter. Organic matter is very quickly degraded by
predation, putrefaction, and/or oxidation, whereas biotic
carbonates precipitate, accumulate and form a sedimentary
layer. Burial and diagenesis then will transform this layer
into a carbonated sedimentary rock [Tucker and Wright,
1990]. The transformation of sediment into sedimentary
rock will produce a rock containing the deposits of fossil
biotic carbonates which keep their original mineralogical
composition. The crystalline structure of biotic carbonate
(macro and microstructure) is very well preserved, thus
there is conservation of this biotic signature [Tucker and
[24]
Acknowledgment. We gratefully acknowledge funding by
CNES.
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