entombed in sediment, such as volcanic ash, which
becomes saturated with water, may petrify or permineralize
the right pH and temperature conditions. Traditionally,
petrification or petrifaction refers to animal or
plant tissue that has turned to stone. Petrified
wood and dinosaur
bone are familiar examples; however, these fossils
actually form through permineralization and often
organic material. In this article we will use petrifaction
and permineralization synonymously.
Permineralized fossils form when solutions rich in
minerals permeate porous tissue, such as bone or
wood. Minerals precipitate out of solution and fill
the pores and empty spaces. In the case of wood, petrifaction occurs when
hemicellulose, and lignin within the cell walls of the woody tissue act
as a framework to preserve cell structure. Silicates,
iron oxides, metal sulfides,
native elements, carbonates, and sulfates can be involved in permineralization.
Silicified wood is the most common and provides the most detailed preservation
of cell structure.
The specimen pictured at the top of this page is a cross-section of a
limb permineralized with silica. Volcanic material often serves as a
source of silica
Volcanic activity resulting in pyroclastic flows, lahars, and ash falls
can bury portions of forests that later become permineralized. Many permineralized
specimens retain patterns of cell structure. Both cell structure and insect
damage, in the form of galleries, have been preserved in the above specimen.
Fossil Wood Composition
When one holds a specimen of silicified wood it certainly appears to be made
entirely of mineral matter with no original cellular material remaining. However,
when examined under magnification many specimens reveal microscopic cellular
leaving one to wonder if some of the original organic matter is still present.
It is informative to make some basic comparisons between fresh wood and silicified
hemicellulose and lignin account for over 95% of the dry weight of wood
(Leo & Barghoorn, 1976, p. 2). The average density of 43 species
of softwoods and 96 species of hardwoods examined by Hoadley is 0.53 g/cm3
(Hoadley, 1990, pp. 49-51). The average density of the softwoods alone was
0.43 g/cm3, while for the hardwoods it was 0.57 g/cm3. Silicified wood
contains more than 90%, by weight, of silica (Leo & Barghoorn, 1976,
pp. 8-9; Sigleo, 1978, p. 1401; Furuno et al., 1986 II, p. 577; Mustoe, 2008, p. 132). Woods mineralized
with opal have densities
of 2.04 g/cm3 or less. Woods permineralized with quartz have densities of
2.34 g/cm3 or greater (Mustoe, 2008, p. 132). Leo and Barghoorn (1976) note that many mineralized woods preferentially fracture toward a radially longitudinal plane as do non-mineralized woods. They hypothesized that this is due to retention of wood in the permineralized specimen or to discontinuities in silica deposition predetermined by the orgininal wood structure at the time of petrifaction (p. 20).
much of the original wood is present? The first well documented attempt
to answer this question was carried out by St. John (1927). St. John examined
25 prepared sections of various silicified wood specimens for cell structure
under a light microscope. The sections were treated with a solution
of one third
hydrofluoric acid and two thirds alcohol to remove silica and then reexamined
under the microscope. Some specimens retained most or some of the structure
indicating the presence of organic matter. Other specimens lost all of their
structure with no trace of organic matter (pp. 733-739).
Mustoe (2008 and
written personal communication, 2011) employed a more quantitative method
to determine the presence of organic matter utilizing heat to destroy residual
organic matter and measuring loss in mass. Mustoe concluded that
most of the plant tissue is destroyed during silicification. Sigleo
Ma Araucarioxylon arizonicum specimens deomonstrating that small
traces of relic organic matter can persist after many millions of years.
evidence suggests that very little of the original organic matter remains
in silicified wood.
How do we account for the visual appearance of cellular detail in silicified
specimens that have little to no organic material? Leo and Barghoorn (1976)
outline five ways in which cellular detail may be retained in silicified
1. The actual wood may remain intact after permineralization.
2. Products from the breakdown of cell walls may be immobilized in silica
close to their site of origin.
3. Variations in the mineralogy of successive silica generations, including
color, texture, and impurities.
4. Infiltration of foreign tar-like organic matter into the specimen.
5. Patterns of entrapped air, which darken silica (pp. 20 & 21).
from the same wood deposit can vary in how much structure is retained.
Even single specimens may exhibit
variation in the retention of wood structure.
The idea that variations in mineralogy lead to differences in texture accords
with my own experience. I have specimens from Sweet Home Oregon that exhibit
beautiful annual rings. Upon closer inspection with a 10x loupe, variations
in cellular detail are immediately apparent. In some areas that have a grainy
texture, described by collectors as “sugary”, no cellular detail
is revealed. In other areas, on the same specimen, the grain size of silica
is so fine that wood histology can be studied with much satisfaction. Do
these differences in how cell structure is preserved represent different
taphonomic pathways or different stages within the same pathway? What are
the conditions and processes that lead to the formation of siliceous petrifactions?
Geochemical Conditions for Silicification
Silicified wood forms in principally two geologic environments.
Trees transported by streams and rivers can become buried in the
fluvial sediments of deltas and floodplains or volcanic ash can
bury trees while still upright (Mustoe, 2003, p. 34). Fresh wood
in soft mud beneath water carrying large amounts of sediment may
set up conditions necessary for fossilization. Rapid burial in
ash is the initial stage for many fossil woods preserved with silica
(Leo & Barghoorn, 1976, p. 5). Volcanic ash acts as an abundant
source of silica for groundwater. The presence of water is important
for several reasons: it reduces oxygen thereby inhibiting tissue
deterioration from aerobic fungi, acts as an agent for the alteration
of ash, maintains
wood shape for maximum permeability, and creates a medium for the
transport and deposition of silica.
The conditions of temperature
during fossil wood formation are equivalent to those found in sedimentary
environments of shallow depth. Excessive pressures would deform
wood shape and tissues. Excessive temperatures (above 100 degrees
break down wood substances. The pH of the sediment-laden water
is probably neutral to slightly acidic. Wood chemically breaks
down at pH values below 4.5 and above 7. Silica is highly soluble
at a pH
of above 9 making precipitation less likely. The weathering of
volcanic ash may produce a pH that is quite high (alkaline), which
silica into solution making it available for emplacement in wood
as the pH is lowered (Leo & Barghoorn, 1976, p. 27 & 29).
These physical and chemical parameters help to define the environmental
conditions in which wood can act as a
template for silica deposition.
A study of silicified wood from the Triassic-aged Chinle Formation of Arizona supports the parameters above. Sigleo (1979) compared the geochemistry of silicified wood and its associated sediments (sandstone with some siltstone and clay) to determine the environmental conditions for the process of wood mineralization. Fossil wood that has stayed in place since deposition and mineralization was carefully chosen for the study. The abundance of minerals and trace elements were measured from the core of the fossil wood to its periphery. Abundance of the same minerals and trace elements were measured in associated sediments and clays from the periphery of the spcimen up to 3 meters away. The clay consisted of 80-90% montmorillonite, which formed from volcanic ash. Identical aluminum concentrations in the clay at the boundary of the fossil and within the periphery of the fossil wood suggest that montmorillonite co-precipitated with silica. The abundance of most trace elements increased from the core of the fossil to its periphery with some notable exceptions.
Antimony (Sb) was found to be much more abundant within the fossil wood than in surrounding sediments with its highest concentrations at the core where carbon was also the most abundant. The abundance of uranium decreased from the carbonaceous core to the periphery of the fossil wood. Uranium and antimony are more mobile when in an oxidized state, but precipitate when reduced. In contrast, the abundance of manganese was low within the fossil specimen and had its highest concentration with in the sediments adhering to the branch. Manganese is more soluble in a reduced state. Clays in the associated sediments were depleted of rare earth elements (REE) relative to the total sediments. REE can be leached from clays in soils with a pH of 4-5.
Sigleo (1979) concluded that the geochemistry of the fossil wood and associated sediments supports a fossil-forming environment that was anoxic and slightly acidic. The silicification process occurred at surface temperatures and pressures associated with typical surface and groundwater conditions. There was no evidence of alkaline conditions or exceptionally high silica concentrations in solution. A continuous supply of silica in solution was provided by the hydrolysis of volcanic ash. Later we will see evidence for secondary stages of silicification associated with hydrothermal events in Chemnitz fossil wood.
The Process of Wood Silicification
Leo and Barghoorn (1976) developed a hypothetical model for wood silicification based upon wood anatomy, a low temperature laboratory process for incipient silicification, and inferred geochemical parameters found in natural settings. Leo and Barghoorn hypothesized that there is a chemical affinity between
wood and silica through hydrogen bonding. Several observations support the
idea that relative unaltered wood may actually serve as a silica sink through
hydrogen bonding. Coalified wood does not silicify well as it has lost functional
groups capable of hydrogen bonding. Carbonate, sulfide, and fluoride petrifactions are
less common and of lower quality possibly because these ions do not establish
hydrogen bonds as well as silica. Silicified woods are often encased within
a matrix that is not cemented with silica, suggesting a differential affinity
for silica between the wood and the surrounding sediment.
Leo and Barghoorn’s
experiments with artificial silicification of wood, described later, also support
the idea that wood has an affinity for silica. According to their hypothesis,
when wood is permeated by silica solution, hydrogen bonding links silicic acid
to hydroxyl groups on cellulose making up the inner cell walls. As water is
lost silicic acid is polymerized into opal. Layers of silica are deposited
with the wood acting as a template (pp. 22-25). Initially, silica is fixed
to the inner cell walls and along the perimeter of the tracheid lumen and infill pits connecting adjacent tracheids. During initial stages of permineralization silica deposition fills voids, especially the lumina.
Cell walls may be replaced with silica in later stages of silicification. To replicate cell structure with high
fidelity a balance between wood degradation and mineral
deposition must be achieved. The amorphous silica that initially permeates wood is highly hygroscopic
water) and highly permeable to fluid flow (Leo & Barghoorn,
1976, p. 20). The rate at which this silica crystallizes to more impervious forms is extremely slow in geologic terms. Thus, long after silicification begins the influx of silica and the migration of degraded organic matter can continue.
As silicification proceeds
to more advanced stages cellulose degrades leaving
more room for the emplacement of silica between cells
and within cell wall layers. Lignin, under anaerobic
conditions, is the most decay resistant compound in
wood and continues to act
a template for structural detail. In fact, fossil woods
show an increase in the ratio of lignin to holocellulose
(cellulose & hemicellulose)
when compared with contemporary counterparts. Specimens
aged Eocene or older are devoid of holocellulose (Leo & Barghoorn,
1976, p. 5). Thus, lignin is the last organic matter
replaced. The balance between removing organic matter and the deposition of minerals is often not complete so, some organic matter remains in many petrifactions. As the process continues silica deposits in intercellular
spaces and voids created by shrinkage and wood degradation.
Silica that initially fixes to the wood structure is
amorphous. This amorphous silica is unstable and slowly
crystallizes to more stable forms. The transition to
more stable forms of silica involves continued polymerization
and water loss. Higher ordered forms of opal are created
through this process and eventually lead to the thermodynamically
more stable silica quartz (Stein, 1982, p. 1277). Multiple
studies have examined natural wood petrifactions representing different fossil deposits providing insights into the physical and chemical processes involved
in wood silicification. Many of these studies lend evidence in support of Leo and Barghoorn's model of silicification.
Buurman (1972, pp. 1-43) examined fossil wood
specimens preserved with a variety
and scanning electron microscopy. We will summarize his
findings relating to silicification. In one group of
silicified woods Buurman found evidence suggesting that
wood preservation is best when disordered tridymite (opal-CT)
replaces cell walls or when this opal is subsequently
transformed to chalcedony through recrystallization.
In both instances, Buurman suggests the fossil wood has
formed by replacement rather than filling. A second group
of silicified woods preserved with chalcedony and quartz
retained some woody tissue. Buurman suggested that these
specimens had formed through permineralization (filling).
Buurman concluded that replacement and permineralization
are distinct processes.
a more detailed study, Scurfield and Segnit (1984, pp.
165-167) examined 75 fossil wood specimens from Australia
using X-ray diffraction, differential thermal analysis,
electron probe techniques, optical and scanning electron
microscopy. Their study found that replacement of the
cell walls of tracheids and vessels occurred in addition
to permineralization. They conclude that petrifaction
of wood occurs in five stages, summarized as follows:
1. Wood is permeated by silica solution or colloid.
2. The pores of cell walls are penetrated.
3. Progressive dissolution of cell walls occurs as a mineral framework builds
to maintain wood structure.
4. Silica deposits in voids, intercellular spaces, and finally cell lumina.
5. Lithification occurs, as water is lost. Silica may transform from one form
to another by pseudomorphic replacement and/or repeated solution and recrystallization.
Scurfield and Segnit found evidence, in the specimens they studied, for transformation
from opal-CT to chalcedony and chalcedony to quartz. Evidence for the conversion
of opal-A to opal-CT was not strong. They also hypothesized that the rate of
cell wall breakdown may determine whether opal-CT or chalcedony is the initial
Furuno et al. (1986 I & II) used light microscopy, SEM, electron probe X-ray microanalysis (EPMA), polarizing microscopy, and X-ray diffraction to study the anatomy and mineralization of Pliocene and Miocene silicified woods collected in Japan. Chemical and physical parameters such as color, reaction to hydrofluoric acid on fractured surfaces, and loss on ignition were also examined. Three samples representing the Pliocene were collected from the Mukaiyama Foramation. Three samples representing the Miocene were collected from the Hata, Fujina, and Kori Formations.
Two Sequoia petrifactions of Pliocene age are black in color. When fractured radially and treated with hydrofluoric acid these specimens produced silica casts of tracheid lumens. The cell walls of these specimens are not silicified and retain substantial organic matter. Cell lumens and pit chambers are permineralized with opal-CT and some quartz, with one specimen showing more quartz than the other. By weight one specimen is 22.89% organic matter and 77.11% silica, while the other is 20.56% organic matter and 79.44% silica. A third Tsuga petrifaction of Pliocene age is white to light brown in color. When fractured radially and treated with hydrofluoric acid isolated silicified tracheids were produced. The cell walls of this specimen are preserved in silica. The lumens and cell walls are preserved in opal-CT and some quartz. By weight the specimen is 2.42% organic matter and 97.68% silica.
One Podocarpus petrifaction of Miocene age is black in color. Cell lumens and cell walls are preserved in mostly quartz. The Podocarpus specimen contains some carbon in the cell walls and in resin cells. The authors hypothesize that resin within the resin cells may have fossilized into amber. By weight the Podocarpus specimen is 5.93% organic matter and 94.08% silica. A second Miocene aged Tsuga specimen is light grey in color. The Miocene-aged Tsuga has cell lumens and walls preserved in quartz. By weight this specimen is 0.09% organic matter and 99.91% silica. One Celtis petrifaction of Miocene age is the only angiosperm dicot in the study and is light grey to brown in color. The Celtis specimen has cell lumens and cell walls preserved in quartz. By weight the Celtis specimen is 0.90% organic matter and 99.10% silica. Hydrofluoric acid applied to radially fractured surfaces on Miocene samples did not produce lithomorphs as easily as the Pliocene samples.
The samples in this study show a correlation between specimen color and carbon content. The study also shows a correlation between the extent of silicification and time. Specimens in this study exhibit a pattern of increasing quartz content over time. Furuno et al. (1986 I & II) proposed the following phases for the silica mineralization of wood.
1. Deposition of silica filling voids like cell lumens and pit chambers, but no penetration of silica into the walls, which remain.
2. Formation of casts of lumens by deposition of silica followed by loss of wall substance.
3. Deposition of silica in the voids and penetration of silica into the wall, some of which are replaced by silica.
4. Deposition of silica in the voids and penetration of silica into the walls, most or all of which are completely replaced, and in some cases loss of intercellular substance.
The authors note that phase 2 was not observed in the specimens of their study. Furuno et al. (1986 II) present the following senario for wood silicification. First opal-A dissolved in an alkaline solution that permeated the wood. Silica precipitated within the acidic wood. Opal-CT was formed. The mineral was kept in a solid state and over tens of millions of years the opal-CT was crystallized to quartz. In the course of time all of the silica minerals were transformed to quartz.
progressive transformation of opal-A to opal-CT
to chalcedony and finally quartz is an important
aspect of the accepted model for wood silicification.
Recent work by Mustoe (2008) reveals that the silica
transformation aspect of this model is inconsistent
with the mineralogy of fossil wood in the Florissant
Formation (pp. 127-140). Mustoe examined 15 specimens
representing six silicified stumps. The samples
were analyzed using X-ray diffraction, X-ray fluorescence,
scanning electron microscopy/energy-dispersive
X-ray spectrometry (SEM/EDX), and optical microscopy.
Basic physical properties including density, color,
and loss on ignition were also determined.
Some of the specimens were permineralized with only
opal-CT, others were a combination of opal-CT and chalcedony,
and still others were quartz. In specimens permineralized
with both opal-CT and chalcedony the two silica phases
appeared to coexist as primary minerals. Thus, evidence
for the transformation of opal-CT to chalcedony was
missing. Evidence gathered by this study suggests that
the Florissant specimens were directly mineralized
with chalcedony. The precipitation of opal, chalcedony,
and quartz are influenced by concentrations of dissolved
silica. Opal is precipitated with high concentrations
of dissolved silica while chalcedony is precipitated
with low concentrations and quartz still lower. Mustoe
speculates that these geochemical characteristics may
explain the patterns of mineralization found at Florissant.
concluded that petrification at Florissant occurred
First, amorphous silica
precipitated on cell wall surfaces.
and chalcedony filled cell lumina.
filled fractures that crosscut permineralized tissues
in some specimens.
Spaces between adjacent tracheids
were often unmineralized, making the fossil wood permeable
to water and susceptible to cleaving radially, tangentially
and transversely from freeze-thaw weathering. This
finding has important implications to the preservation
of specimens at Florissant Fossil Beds National Monument.
Mustoe’s findings are important because they
suggest that petrifaction may occur through multiple
processes or pathways.
Witke et al. (2001) used Raman and cathodoluminescence spectroscopy to study the chemical composition and structural order of silicified plants from the 290 million year old Chemnitz Petrified Forest. Samples of the seed fern Medullosa, gymnosperm Dadoxylon, sphenopsid Calamodendron striatum, and tree fern Psaronius were used in the study. Tracheid and sclerenchyma cells making up vascular tissues are preferentially preserved in Chemnitz fossil plants. Cell walls are preserved primarily in microcystalline alpha quartz. In areas where tissue is not preserved as as in the pith of Medullosa one finds banded agate structures composed of phanerocystalline and microcrystalline alpha quartz along with moganite. A very low percentage of original organic material remains in the Chemnitz silicified plants.Raman spectra of carbonized material dispersed within Chemnitz petrifcations reveals a rank equal to bituminous and anthracite coals.
Witke et al. (2001) proposed the following steps for the mineralizations of Chemnitz petrifcations.
First, plants were mineralized with quartz and fluorite.
Second, a hydrothermal alteration transformed the silica. Iron oxides were associated with this process.
The third step consisted of secondary mineralizations with calcite and barite in cracks of the former wood.
The minor residues of carbonaceous material of anthracite rank found in Chemnitz specimens seem to be consistent with the hydrothermal event.
Dietrich et al. (2013) used backscatter electron imaging (BSE) and electron backscatter diffraction (EBSD) in a scanning electron microscope to study the ordering of silica preserving xylem tissue in three different fossil tree forms found in Chemnitz Petrified Forest.
The study of Chemnitz petrifactions included the root mantle of the tree fern Psaronius, vascular segments in the pith of the seed fern Medullosa stellata, and the secondary xylem of the gymnosperm Dadoxylon. Former open spaces and specific tissue structures were found to be correlated with different silica ordering.
Tracheid cell walls inthe aerial roots of Psaronius are largely preserved by well-ordered microcrystalline quartz grains. The thickened cell walls of the sclerenchyma fibers, making up the outer boundary of the aerial root, are preserved with extremely fine-grained but well-ordered quartz. Cell lumina are filled with cryptogrystalline quartz. Tracheid cell walls in M. stellata exhibited multiple microcrystalline layers outlining the former cell wall layers. In fact, crystal growth directions within these layers seem to mirror former cellulose fibril orientations. As in Psaonius, cell lumina were largely filled with cryptocrystalline quartz. Tracheid cell walls in the secondary xylem of Dadoxylon are preserved with microcrystalline quartz. Cell lumina are filled mostly with cryptocrystalline quartz or more infrequently with microcrystalline quartz or large fluorspar crystals.
In general the cell lumina of all three specimens are filled with cryptocrystalline quartz, while the cell walls were preserved with microcrystalline quartz. Microcrystalline quartz grain size decreased with tracheid cell diameter. Psaronius tracheid cell walls are preserved with the largest grain size, while the cell walls of Psaronius sclerenchyma, M. stellata tracheids, and Dadoxylon tracheids are preserved with a finer grain size. The tissues of these plants vary in their proportions of cellulose, hemicellulose, and lignin. The results of this study suggest that tissue composition affects silicification ordering in petrifactions.
Dietrich et al. (2013) proposed the following stages of petrifaction to explain the patterns of silica ordering observed in the tissues of Chemnitz specimens.
1. Silica solution permeates the porous xylem tissue and forms a silica gel inside the tracheid limina starting at the inner cell walls.
2. Thus, cell lumina are quickly preserved in silica, which may be transformed later to cryptocrystalline silica or to alpha quartz.
3. The gel cast of the lumina is initially porous and allows a continued influx of silica solution (presumably in a hydrothermal process), which over longer periods of time permeates into the ligno-cellulose making up the former cell walls and intercalates the cellulose fibrils.
4. Cellulose fibrils act as templates for microcrystalline growth of silica. Thus, the preserved cell walls can be distinguished from the cell lumina by different crystal growth.
5. In a third stage, agate and/or larger grains of microcrystalline quartz form in areas with fewer precipitation sites such as cell corners, central piths and fissures resulting from cracking, drying, and tissue degradation.
Is there a place we can go to examine the silicification of wood occurring in more recent times? Karowe and Jefferson (1987) investigated the initial stages of silicification by examining trees buried by Mount St. Helens lahars or mudflows dated at 1980, 1885, A.D. 1450-1550, and 36,000 years B.P. Wood samples were examined using scanning electron microscopy and energy dispersive X-ray analyses. Wood buried in 1980 showed no siginificant mineral deposition. Wood buried in 1880 and A.D. 1450-1550 exhibited traces of silica on cell walls as well as cell wall decay.Wood buried 36,000 years B.P. showed silica impregnation of cell walls. Decay in these older specimens affecgted the secondary wall and removed the middle lamella (pp. 198-200). Karowe and Jefferson concluded that the increase in silica deposition as well as decay associated with the age of these trees supported the model of silicification proposed by Leo and Barghoorn in 1976.
The apprent increase in silica deposition was an exciting find. However, researchers at the University of Bonn were unable to reproduce the results of Karowe and Jefferson even when using specimens prepared from the same trees (Hellawell et al., 2011). Perhaps Karowe and Jefferson were looking at an instrumental artifact. Scientists at the University of Bonn are currently working on a paper that will explore the results of their study in more depth. It is clear that many petrified wood deposits, such as those found at Yellowstone, are associated with volcanic mudflows. George Mustoe has examined many Holocene wood specimens from mudflows and has found no evidence of silicification (Mustoe, written personal communication, 2012).
Time and Silicified Wood
Fossil plant deposits including petrified forests
from around the world allow paleontologists
to trace the evolutionary history of vascular
Ma ago (Silurian) to the present (Kerp, 2002, p. 23). Petrified forests
throughout the world capture the public’s
imagination (Ransom, 1955; Dernbach, 1996; Dernbach
and Tidwell, 2002; Daniels and Dayvault, 2006).
to know how long
it takes to form natural petrified wood. Some Pleistocene deposits
contain peat and wood fragments that can be carbon dated. Ice Age gravels
deposited 12,000 years ago contain fresh looking
wood pieces. Wood dated at 15 million
years weathering out of the Wilkes Formation in Washington can be carved
with a pocketknife and ignited with a match (Mustoe,
2001, p. 18). It is clear that
wood can be preserved for long periods of time under the right conditions.
is equally clear that wood can be quickly mineralized
under the right conditions. Timbers in copper mines
and Arizona have been found that contain
copper (Daniels & Dayvault, 2006, p. 173). It would be interesting
to study the amount of original wood, extent of permineralization and
lithification in these specimens and compare them with silicified woods.
produced from the 1886 eruption of Mt. Tarawera in New Zealand is mineralized
with silica. Wood specimens recently exposed to hot springs in Yellowstone
exhibit the beginning stages of silicification; however, geologic evidence
suggests siliceous thermal springs have not been major sites of wood
petrifaction (Leo & Barghoorn, 1976, pp. 26 & 27). Silicified
wood from Wyoming contained enough organic material to be carbon dated
at less than 3,000 B.P. X-ray diffraction
these recently silicified woods are impregnated with amorphous opal
(Leo & Barghoorn,
1976, p. 15; Stein, 1982, p. 1279).
The question of how long it takes to form petrified wood also depends on the physical qualities of the fossil wood we have in mind. Are we looking at wood that is mostly intact and has cell lumina and intercellular spaces impregnated with minerals or fossil wood that has little to no wood remaining and has cellular detail replicated in opal-CT, chalcedony, and microgranular quartz? If we have in mind the latter then these recent petrifactions are
not what collectors think of as gem quality petrified wood, which can be cut and polished at the lapidary.
initial emplacement of silica as a film may occur rapidly.
Artificial silicification of wood in the lab and studies
of natural silicified wood demonstrate that the physical
state of silica in newly formed petrifactions is amorphous
(Leo & Barghoorn, 1976, p. 28). Conversion of this
silica to increasingly stable forms of opal-A (amorphous),
to opal-CT (cristobaite & tridymite), to chalcedony
(cryptocrystalline quartz), and finally to microgranular
quartz requires millions of years (Leo & Barghoorn,
1976, p. 29; Stein, 1982, p. 1281; Kuczumow et al.,
1999, p. 436). Under normal conditions conversion of
opal to quartz requires tens of millions of years; however,
under geothermal conditions the same process may occur
in 50,000 years or less (Mustoe, 2003, p. 34).
X-ray diffraction patterns for different aged silicified specimens examined
by Stein support the well established transformational sequence of opal-A to
opal-CT, to quartz. A Yellowstone Wyoming sample carbon dated at 2,430 years
was composed of opal-A. A Pliocene-aged sample from the Sante Fe Formation
of New Mexico was composed of opal-CT. A Miocene-aged sample from the Bozeman
Lake Beds was composed of opal-CT and some quartz. A Late Eocene sample from
Florissant, Colorado was composed of quartz. However, Mustoe (2008) has determined
that some Florissant wood is also permineralized with opal-CT and chalcedony.
Still, chalcedony and microgranular quartz are the most common forms of silica
that are Eocene
or older. X-ray diffraction studies, specific gravity measurements and indices
of refraction all support an increase in silica ordering with increase in age
(Stein, 1982, pp. 1277-1280).
Instant Petrified Wood?
Fascination with natural permineralized specimens has spurred interest in creating methods for artificial petrifaction. Artificial petrifaction reflects both scientific and commerical interests. Methods for artificial petrifaction have been devised as ways to study wood structure and model the initial stages of natural silicification. Artificial petrifaction is also used to develop wood composites and ceramics. Leo and Barghoorn (1976) document early attempts at creating artificial silicified wood in the 1500's by Basil Valentine and Johannes Kentmann.Experimental replication of these early recipes has not been successful (p. 10). More recent attempts have produced some positive results.
Ryan W. Drum from the University of Massachusetts, Amherst, describes his attempt at the laboraty silicification of twigs in a 1968 article that appeared in the journal Science. Twigs were soaked in solutions of sodium metasilicate, washed, and then treated with chromic acid to remove organic remains. Entire twigs did not remain intact; however, single cells and small aggregates of cells were replicated in silica. Drum described these replicas as very fragile and included electron micrographs of his results. Drum goes on to say that his in vitro silicification process might provide a method to study cellular spaces in 3-D, intercellular connections, and the morphology of woody cells.
Leo and Barghoorn (1976) improved upon Drum's experiments. Their procedure included boiling wood to degas and waterlog specimens. The wood was alternately soaked in solutions of water and ethyl silicate at neutral pH and 70 degrees Celsius. Ethyl silicate decomposes to monomolecular silicic acid, which is thought to be the silicifying agent in natural processes. Nitric acid and potassium chlorate were used to remove organic matter. The silica lithomorphs that remained replicated cell structure and were more substantial than those produced from Drum's procedure. The silica lithomorphs were fragile and composed of amorphous silica. These silica lithomorphs resemble the first stages of permineralization observed in recent silicified specimens (p. 12-15).
Persson et al. (2004) evaluated the use of sol-gel mineralization to study the wood morphology of spruce and birtch xylem. Wood chips of birch, Betula verrucosa, and spruce, Picea abies, along with the pulp of spruce were used in the study. Spruce pulp was prepared using the Kraft process. The Kraft process uses a mixture of sodium hydroxide and sodium sulfide along with cooking at high tempertures (170 degrees Celsius) to degrade lignin and hemicellulose, converting the wood to a pulp consisting of almost pure cellulose fibers.
Wood chip samples and the pulp were soaked in ethanol and vacuum dried two times to facilitate impregnation. The prepared wood and pulp samples were immersed in a sol-gel mixture (polysilicic acid) for three days at 60 degrees Celsius. Silica casts of the wood and pulp were recovered by removing all organic material by heating to 575 degrees Celsius for 6 hours. The brittle silica casts replicas were studied using environmental scanning electron microscopy (ESEM) and transmission electron microscopy (TEM). Persson et al. (2004) found that their sol-gel casting medium penetrated and condensed on the ultrastructure of cell walls. The high-resolution silica casts were used to observe the three dimensional structure of xylem and pit structures connecting wood cells.
Experiments in artificial silicification described above have been used as methods to replicate the process of natural incipient silicification and to study the ultrastructure of wood. These experiments suggest that the organic cell structure of wood acts as a template for initial silica deposition. The fact that wood is removed in making silica-cast replicas limits the use of these procedures for studying advanced stages of natural silicification.
recently, Ballhaus et al. (2012) designed closed-system experiments
at 100 degrees Celsius to simulate the silicification of trees
buried by volcanic pyroclastics. Silica rich solutions
by reacting powdered obsidian with water at 100 degrees Celsius
for several days. Under these conditions it was found that
silica and alkali
oxides readily go into solution while aluminum oxide remains
in the residue. The pH of the solution increases to values
of 9.4-10.5. Wooden cubes made of Douglas-fir (Pseudotsuga
menziesii) were reacted with the silica solution in an
autoclave for up to 300 hours. In the presence of the wood
the pH and
silica concentrations decreased, while alkalis remained in
rich solutions were again prepared by reacting powdered
obsidian with water at 100 degrees Celsius for several days.
The solution was doped with NaOH to increase the pH values
to 12.5 and 13.2
in order to increase the solutions silica concentration. Douglas-fir
wood cubes were reacted with the solutions in autoclaves for
112 days. Periodically, slices of wood were prepared and analyzed
for precipitates. After several days many of the cell lumina
were infilled with silica. Most precipitates were found on
wood that exhibited final pH values near neutral. Under SEM
the silica precipitates appeared as microspheres of opal.
experiments simulate and provide evidence in support of
to be involved in the incipient permineralization
of wood. Volcanic material rich in siliceous glass can be quite
alkaline. When these solutions come into contact with wood
the pH is lowered and silica becomes less soluble, precipitating
onto wood surfaces. This pH gradient between the silica rich
alkaline water and the acidic environment of the wood tissue
acts as force to precipitate opal onto wood surfaces. A second
force driving permineralization is the ability of wood tissue
to extract silica out of solution. The decrease in the silica
concentration in the presence of Douglas-fir wood cubes is
indirect evidence that is consistent with Leo and Barghoorn’s
(1976) hypothesis that silica species chemically bond with
hydroxyl groups on wood surfaces.
et al., (2012) used simple diffusion and advection models
how long it would take to permineralize
a tree with opal. Using Frick’s Law a theoretical conifer
tree trunk with a diameter of 100 cm and a length of 100 cm
buried horizontally in a pyroclastic deposit would be permineralized
through diffusion within an estimated time of 47,000 years.
Using an advection model the same tree buried upright (in
would require approximately 3,600 years for cell lumina and
intercellular spaces to become impregnated with opal. This
estimate assumes wood structure remains intact. The results
of this study are consistent with other findings and indicate
that the incipient permineralization of large trees with opal
is on a time scale of thousands of years.
process of natural permineralization has also inspired
the pursuit of artificial wood composites. These wood
composites use fresh wood as a framework for creating
either a wood composite or a ceramic. An
October 1992 Popular Science news article read ‘Instant
petrified wood?’ In reality researchers at the
Advanced Ceramic Materials Lab at the University of Washington
in Seattle were making wood ceramic composites. Wood
is soaked in solutions of silica and aluminum and then
oven-cured to create the composites. The solution penetrates
the wood to a depth of up to 0.2 inches. The wood is
abrasive, but can be worked with carbide tools. The authors
speculate that these composites could be made with the
same rock-hardness of petrified wood. The composite is
wood impregnated with silica and aluminum up to a depth
of 0.2 inches.
Shin and colleagues at the Pacific Northwest National
Laboratory (PNNL) developed a method for creating a silica-based
ceramic that mimics wood structure. The process uses
surfactants and silicate solutions to mineralize wood
that has been soaked in an acid solution. After the silicate
solution penetrates cell wall structures it is heated
to high temperatures in air to oxidize the silicate and
remove organic residue. This method creates a ceramic,
which faithfully reproduces cellular structures in great
detail as confirmed by SEM images (Shin et al. 2001, p. 728). Shin et al (2001) points
out that, “Another important phenomenon related
to the current study is natural petrification, which
takes place over a very long period of time. In some
cases the cellular tissue is completely replaced by silicate
and other minerals. Our study not only points to a more
rapid approach to transforming organic tissues into ceramic
materials, it may also shed some light on how natural
petrification takes place (p. 731).”
article on ChemicalProcessing.com entitled ‘Petrified
wood yields super ceramics’ describes a process
developed at PNNL for using wood to form the ceramics
silicon carbide (SiC) and titanium carbide (TiC). The
process involves soaking the wood in acid, infusing it
with titanium or carbon, and baking it in an argon-filled
furnace at 1,400 degrees Celsius. This process is the
same as Shin's 2001 study except for heating in an argon
atmosphere instead of air. The 2001 and 2005 experiments
used small blocks of pine and poplar wood. Both the macro
and microstructure of the wood is preserved in this ceramic.
The material has the strength of steel, and can resist
temperatures of up to 1,400 degrees Celsius. PNNL scientist
Yongsoon Shin is quoted as saying that one-gram of this
material flattened has enough porosity to cover an entire
football field. SEM and TEM images were used to study
the microscopic structure of these ceramics (Shin et al. 2005, pp. 73-76). The SiC ceramics could be used for
making filters, catalysts, cutting tools, abrasives,
and coatings. The purpose of Shin’s research is
to develop methods for using natural biological materials
as templates to construct inorganic materials.
Hicks was issued US patent 4612050 on September 16, 1986
for a mineralized sodium silicate solution used to create
wood with the “non-burning characteristics of petrified
wood” (Patent Storm). In one experiment a horse
stall was set on fire with combustible materials. The
treated wood showed signs of charring, but did not burn.
The patent indicates that the treated wood is non-toxic
and has an inherently bad taste. This bad taste prevents
horses from “chewing or nibbling the wood to shreds”.
The inventor speculates, “petrifaction of the treated
wood is achieved when minerals in his solution “replace
the cells” and the solution hardens the wood. It
would be interesting to compare the amount of wood still
present as well as the nature and extent of silicification
in this product with that found in naturally silicified
Products referred to as "instant petrified wood" may provide insights in the initial stages of permineralization. However, many of the materials and procedures used to make these products are not found in nature. Furthermore, procedures to make silica-cast replicas and ceramics remove wood after the initial permeation with artificial mediums. Products made from the initial emplacement of silica, represented by both artificial and recent natural petrifactions do not resemble what a collector regards as gem quality petrified wood. Multiple lines of evidence suggest that natural fossil wood silicified with opal-CT, chalcedony, and microgranular quartz requires millions of years to form.
Evidence for pathways that lead to the formation of silicified wood comes from studies of fossil wood representing different aged deposits, laboratory simulations of petrifaction, production of organic composites, and examination of trees buried recently by volcanic deposits. The formation of silicified wood includes permineralization, replacement, and recrystallization. A summary of an accepted model for natural silicification is as follows.
When wood is permeated by silica solution, hydrogen bonding links silicic acid to cellulose making up the inner cell walls. Silicic acid is polymerized into opal through water loss. Silica that initially fixes to wood structure is amorphous and can recrystallize to a more stable form. Layers of silica are deposited with the wood acting as a template. Initially, silica is fixed to the inner cell walls and infills the lumina of tracheary elements (vessel elements and or tracheids) and the pits connecting adjacent tracheary elements. Cell walls may be replaced with silica as permineralization continues. To replicate cell structure with high fidelity a balance between the chemical and biological decomposition of wood and the precipitation of silica must be achieved. As silicificaiton proceeds to more advanced stages cellulose degrades leaving more room for the emplacement of silica between cells and within cell wall layers. This replacement is not molecule-by-molecule. Lignin is the most decay resistant compound in wood and continues to act as a template for structural detail. Later, cracks and fractures are preserved with silica. A traditional model of silicification includes a transformation of the initial silica to increasingly more stable forms from opal-A to opal-CT to chalcedony and finally to quartz. However, evidence for silica recrystallization is lacking in some specimens suggesting more than one pathway for silicified wood formation (Mustoe, 2008).
Studies of silicified wood from Florissant and Chemnitz demonstrate that cell walls and lumina can be preserved in different forms of silica. Thus, forms of silica that serve as the initial replicating material for cell walls and open spaces may be different from what initially permineralized the wood. Factors that affect what form of silica serves as the initial replicating material will lead to a better understanding of natural silicification pathways. One of these factors may include the plant tissues themselves. Examination of microstructure in petrifactions of Chemnitz encourages further investigations into how tissue composition affects what form of silica may act as a replicating material (Dietrich et al. 2013).
I would like to thank George Mustoe, Dagmar Dietrich, Yongsoon Shin, and Jim Mills for their expertise and encouragement.