Abstract

We provide a comprehensive photographic atlas of the intricate alteration features found in glass in igneous rocks from the ocean basins. The samples come from surface and subsurface rocks from oceanic rises and seamounts of the ocean basins and some marginal seas. These textures have previously been termed “bioalteration textures” by those who consider them as potentially biogenic in origin, or as “etch pits” by those who prefer a non-biogenic interpretation. Here, transmitted-light color photomicrographs are provided to illustrate the range of granular and tubular textures as well as their relation to fractures, minerals, vesicles, and multiple episodes of alteration in the same sample. The tubular forms are described using seven morphological characteristics: (1) length and width; (2) density; (3) curvature; (4) roughness; (5) variations in width; (6) branching; and (7) tunnel contents. The photomicrographs are a starting point for understanding the factors that control the formation of the alteration textures, for evaluating the biogenicity of the various forms, for inferring subsurface conditions during alteration, and for making comparisons to similar textures in ancient ophiolites, some of which have been attributed to the earliest life on Earth

INTRODUCTION AND PREVIOUS WORK

Aims and Scope of This Atlas

The interaction of sub-seafloor volcanic glass with circulating fluids produces secondary minerals as well as alteration textures that penetrate into the glass (e.g., Thorseth et al., 1995; Fisk et al., 1998a; Alt and Mata, 2000; Furnes et al., 2001a; Josef, 2006). These alteration textures are found in basalts from the flanks of ocean rifts, seamounts, back-arc basins, and marginal seas. The alteration textures include micron-sized etch pits and tunnels that are located at the interface of fresh glass and its alteration products. This petrographic atlas aims to bring together and illustrate the full spectrum of alteration textures in marine lavas to show the variety of alteration textures found in volcanic glass and hyaloclastites collected from the ocean crust. In particular we focus on the size, morphology, distribution, and infilling of granular cavities and tubular tunnels.

A selection of annotated petrographic images from a collection of 119 samples spanning the world’s ocean basins is provided to systematically illustrate the key textural characteristics of glass alteration. A guide and glossary to the principal features is provided and an accompanying classification scheme is given to identify the key morphotypes of glass alteration. This expands on earlier classification schemes (Furnes and Staudigel, 1999; Josef, 2006; Staudigel et al., 2006, 2008; McLoughlin et al., 2009) and identifies several previously unrecognized morphotypes.

The atlas is intended as an illustrated guide for geologists, microbiologists, and astrobiologists studying glass alteration. We realize that as researchers further explore their collections and as more deep-sea environments are sampled, new forms of glass alteration will be found and documented; thus, this guide represents the current state of knowledge. Some alteration textures have previously been argued to represent biological alteration products and trace fossils (e.g., Fisk et al., 1998a; Torsvik et al., 1998; Furnes et al., 2001a, 2001b, 2002, 2008; Furnes and Muehlenbachs, 2003; Banerjee and Muehlenbachs, 2003; Thorseth et al., 2003; McLoughlin et al., 2009; Staudigel et al., 2008); however, this study is not designed to support or refute claims of biogenicity of the alteration of basaltic glass. Also, this work does not investigate the secondary mineralogy of altered glass, referred to as palagonite, a mixture of iron oxyhydroxides and phyllosilicates (Stronick and Schmincke, 2002), and we have not characterized the secondary minerals, such as carbonates, zeolites, and phyllosilicates, that occur in voids and fractures in the glass. These minerals are indicative of conditions in the seafloor and may be useful for correlating conditions of alteration with glass alteration features; however, this is the subject of an ongoing study. If the alteration textures are biotic and if specific textures can be correlated with subsurface conditions, then they could help researchers understand the evolution of the marine subsurface environment from the Archean to the present.

Previous Work

Granular and tubular alteration textures of oceanic volcanic glass have been illustrated in transmitted-light photomicrographs since the 1960s (Morgenstein, 1969). In that first study, glass/palagonite alteration boundaries and linear features in black-and-white photographs were described as “micro-channels” and “hair channels.” More recently, transmitted-light photomicrographs of alteration features in seafloor and sub-seafloor basalt glass have been published by a number of authors (e.g., Giovannoni et al., 1996; Fisk et al., 1998a, 2006; Furnes and Staudigel, 1999; Fisk and Giovannoni, 1999; Christie et al., 2001; Furnes et al., 2001a, 2002; Banerjee and Muehlenbachs, 2003; Storrie-Lombardi and Fisk, 2004; Ivarsson et al., 2008; Staudigel et al., 2008; Cockell and Herrera, 2008; McLoughlin et al., 2009, 2010; Heberling et al., 2010). These studies have, in general, included a limited number of images to illustrate the granular or tubular structures, and they have not documented the full range of alteration textures now known from oceanic igneous glass. An extensive unpublished collection of photomicrographs also exists (Josef, 2006).

Over this more recent period (1996 to the present), alteration features in oceanic basalt glass have also been illustrated in backscattered electron images, transmission electron images, and energy-dispersive X-ray spectroscopy (EDS) maps (e.g., Furnes et al., 1996, 1999; Torsvik et al., 1998; Alt and Mata, 2000; Thorseth et al., 2003; Kruber et al., 2008; Cockell et al., 2009). Also, similar features have been documented with transmitted-light photographs of metamorphosed pillow-lava rims from Archean to Phanerozoic ophiolites (Furnes et al., 2001b, 2004, 2008; Furnes and Muehlenbachs, 2003; Staudigel et al., 2006, 2008) and an Archean mafic tuff (Lepot et al., 2011). Photographs of granular and tubular alteration in basalts from the marine/land transition have also been published (Fisk et al., 2003; Walton and Schiffman, 2003; Walton, 2008; Cousins et al., 2009; Montague et al., 2010). Interestingly, similar transmitted-light photomicrographs of alteration features in pillow lavas erupted into fresh water are not evident in the literature.

Common alteration textures, such as tunnels in volcanic glass, were until recently informally classified by several authors, so synonyms for these textures exist in the literature. A more formal ichnotaxonomic classification was suggested by McLoughlin et al. (2009), which considered potential bioalteration textures as trace fossils and recognized two ichnogenera and five ichnotaxa based on a selection of samples from the in situ oceanic crust and Phanerozoic ophiolites. This atlas expands on these five ichnotaxa or morphotypes, and outlines seven morphological criteria and provides names for features that can help unify discussion of the morphotypes.

Abundance and Distribution of the Alteration Textures

The percentage of glass alteration in sub-seafloor basalts can be estimated visually, and the percent of that total alteration that is attributed to biotic versus abiotic processes has been derived by point counting of thin sections from the Mid-Atlantic Ridge, the Costa Rica Rift, and Lau Basin (Furnes et al., 2001a). From 2% to 60% of the glass was altered, with about half of this alteration being granular and tubular and the remainder being “abiotic” secondary minerals. The amount of granular and tubular alteration has also been visually estimated in basalt glass at the marine/land transition (Cousins et al., 2009; Montague et al., 2010). One of these studies (Cousins et al., 2009) from the glacial/marine transition of James Ross Island, Antarctica, found that the samples exposed to seawater tended to have more granular and tubular alteration than samples exposed to fresh water. Alteration of a Hawaiian subsurface hyaloclastite was indexed from 1 to 6, with 1 being no glass alteration to 6 being complete alteration (Montague et al., 2010). Indices were mostly 2–3. From these three studies, it appears that granular and tubular alteration is ubiquitous and more abundant in marine water than fresh water.

Although most photographic documentation of tunnels has come from basalts, there are examples of tunnels from other silicates. There are two examples from felsic rocks—one of these is from a rhyolite tuff from central Oregon (United States) (Fisk et al., 1998b) and the other is from a submarine clastic tuff from the western Pacific (Banerjee and Muehlenbachs, 2003). Also, tunnels have been documented in olivine from an olivine basalt collected from the marine/land transition in Hawaii and in dunites from central Oregon and northern California (Fisk et al., 2006).

Origin of Alteration Textures in Volcanic Glass

It has been hypothesized based on several lines of evidence that some of the tunnel and granular alteration features are produced biotically. In support of this, biological staining has revealed that nucleic acids can be found at the interface of fresh and altered glass near tubular and granular textures and in some tubular forms (e.g., Furnes et al., 1996; Giovannoni et al., 1996; Torsvik et al., 1998; Banerjee and Muehlenbachs, 2003). It has been shown theoretically that basaltic glass can yield sufficient energy to support chemolithoautotrophic growth (Bach and Edwards, 2003), and culture-independent sequencing studies have shown that the microbial population inhabiting the sub-seafloor is distinct from that found in both overlying seawater and seafloor sediments and is up to 4 times larger (Mason et al., 2009; Santelli et al., 2008). Controlled laboratory experiments have found that enhanced, localized dissolution occurs in volcanic glass inoculated with microorganisms, relative to abiotic controls (Thorseth et al., 1995; Staudigel et al., 1995). Comparative analysis of pillow-basalt rims and interiors suggests that biological activity has lowered the δ13C of the rim relative to the basalt interior (e.g., Furnes et al., 2001c). Partially fossilized, mineral-encrusted microbial cells have been observed in or near etch pits on altered glass surfaces, and these pits have forms and sizes resembling the associated microbes suggesting that the microbes are involved in pit formation (Thorseth et al., 1992, 2001, 2003). Although these studies support the hypothesis of biologically mediated tunnels, it has not yet been possible to cultivate microorganisms that create tunnel shapes, and abiotic mechanisms of tunnel production have been proposed such as for the Archean mafic tuffs, which experienced conditions very different from basalts in our collection (e.g., Lepot et al., 2011). So although the weight of evidence is in favor of the biological formation of complex tunnels, the question has not been answered.

In attempts to understand the origin of the alteration textures, several geochemical tools have been used to examine the contents of tunnels and the chemistry of the surrounding glass and alteration products. These studies have included: electron probe microanalysis (Furnes et al., 1996; Torsvik, et al., 1998; Storrie-Lombardi and Fisk, 2004); scanning and transmission electron microscopy (Alt and Mata, 2000; Thorseth et al., 2003; Benzerara et al., 2007; McLoughlin et al., 2011; Knowles et al., 2012); Raman and/or infrared spectroscopy (Preston et al., 2011); and synchrotron-based X-ray microprobe techniques (Benzerara et al., 2007; Staudigel et al., 2008; Knowles et al., 2011, 2012; Fliegel et al., 2012). It has been hypothesized that Fe(II) is an energy source for microbial metabolism, and electron microprobe analyses of palagonite near “biotic” alteration has higher Fe than palagonite near “abiotic” alteration (Storrie-Lombardi and Fisk, 2004). Analysis of the 100–300-nm-wide rim of a tunnel in glass shows that the glass lost Fe (Alt and Mata, 2000) and this loss of Fe is consistent with a gain in Fe in the alteration material near “biotic” alteration (Storrie-Lombardi and Fisk, 2004). Transmission electron microscopy and synchrotron-based X-ray microprobe analysis show the presence of partially oxidized Fe (Benzerara et al., 2007; Knowles et al., 2011; Fliegel et al., 2012) and organic carbon in tunnel-filling smectite (Benzerara et al., 2007). The X-ray microprobe analysis also shows that tunnels are produced by the dissolution of the glass. Nano-Secondary Ion Mass Spectrometry analyses of carbon, nitrogen, and manganese associated with micropores in glass suggest that these are remnants of manganese-oxidizing bacteria (McLoughlin et al., 2011). Raman spectroscopy indicates that tunnels contain complex organic compounds such as amides and esters, which could be left by microbial inhabitants (Preston et al., 2011). These studies show that microbes and microbial processes are associated with some of the alteration features described in this paper.

The biogeochemical controls on the abundance, distribution, and diversity of alteration textures in volcanic glass, however, are yet to be identified, and we hope that the framework presented herein will aid future investigations of the these controls on (bio)alteration. In addition, this collection of alteration textures may be an informative companion for those studying the alteration of (meta)volcanic glass in ophiolites and/or Precambrian greenstone belts and provide a context for interpreting proposed trace fossils that are hypothesized to represent some of the earliest evidence for life on Earth (Furnes et al., 2004). Likewise, for astrobiologists who may one day study alteration in igneous rocks from other planetary bodies (cf. Fisk et al., 2006), this will provide a terrestrial reference frame for the range of currently known textures.

SAMPLES

Samples for this study are from existing collections and are primarily cored sub-seafloor igneous rocks that were collected and archived by the Deep Sea Drilling Project (DSDP) and the Ocean Drilling Program (ODP). The location of volcanic glass within the archived cores was determined by first reviewing Initial Reports volumes of the Deep Sea Drilling Project and the Initial Results volumes of the Ocean Drilling Program. Then, during visits to the sample repositories at Scripps Institution of Oceanography, Texas A&M University, and Lamont-Doherty Earth Observatory, the presence of glass was verified visually and samples were collected from the working halves of the cores. This collection of DSDP and ODP samples was supplemented with a small number of samples from an Integrated Ocean Drilling Program (IODP) expedition as well as from seafloor outcrops that were collected by submersibles. In total, the samples come from 21 DSDP expeditions, 15 ODP and IODP expeditions, and 5 manned and unmanned submersible expeditions. Samples are from the Pacific, Indian, and Atlantic Oceans, the Mediterranean Sea, and some adjacent seas. Basalts from ocean rifts, seamounts, and back-arc spreading ridges are included in the study. The cored samples come from a range of depths into the volcanic basement, ranging from the sediment/basalt contact (<0.5 m into basement, mib) to 320 mib. Samples collected by submersible are from outcrops on the seafloor. The samples are primarily the rims of pillow basalts, sheet-flow margins, and interflow breccias. The youngest cored basalt examined was <0.4 Ma and the oldest was 167 Ma. At some cored sites, samples from multiple depths were examined. Standard 26 mm × 46 mm polished petrographic thin sections were examined. These are listed in Table 1, and Figure 1 shows the global distribution of samples. All samples, except 482D 11R2 32, which appears to have been at ≤150 °C at the time of collection (Duennebier and Blackinton, 1980), were from the seafloor or shallow subsurface where ambient temperatures were compatible with life (<100 °C).

TABLE 1.

SAMPLES EXAMINED FOR THIS STUDY

Figure 1.

Locations of all samples examined as part of this study. Larger (white) circles indicate the locations of samples that are documented with photographs in this article; other samples examined are indicated by smaller (blue) circles. The map was generated with GeoMapApp, http://www.geomapapp.org (Ryan et al., 2009).

Figure 1.

Locations of all samples examined as part of this study. Larger (white) circles indicate the locations of samples that are documented with photographs in this article; other samples examined are indicated by smaller (blue) circles. The map was generated with GeoMapApp, http://www.geomapapp.org (Ryan et al., 2009).

METHODS

The petrographic thin sections listed in Table 1 were examined with a petrographic microscope fitted with objective lenses with 4×, 10×, 20×, and 40× magnification. Thin sections are nominally 30 μm thick, which is 3–30 times the diameter of most tunnels and thus permits viewing tunnels in three dimensions by changing the elevation of the microscope stage. The observation strategy was to survey the whole thin section with the 4× objective lens to locate areas of glass. These glasses were then viewed at 10× and/or 20× to locate regions that contained altered glass and glass-alteration textures. Glass commonly was limited to less than 25% of the thin section area and most regions of altered glass were examined at one of these two higher magnifications. The alteration was photographed at 40× and sometimes at 10× for larger features or to show the context of the feature being illustrated. All of the morphotypes of alteration found in our selection of thin sections are illustrated in the figures.

The optical images shown here were obtained using a Nikon LV100Pol polarizing microscope at the Centre for Geobiology in Bergen, Norway, and photographed using an DS-Fi1 color camera with 5.24-megapixel resolution coupled to NIS-Elements BR 2.30 software. The images were saved in Joint Photographic Experts Group (.jpg) format (2560 × 1920 pixels).

RESULTS

Guide to Illustrations

The alteration features are summarized in line drawings in Figure 2, and each line drawing references a photograph that illustrates the feature (Figs. 3–31). The diversity of alteration features can be illustrated with a subset of 26 thin sections (identified by bold italics font in Table 1). Each photograph is labeled with the sample identification, a scale bar, and descriptive terms. Also the glass and major features such as fractures, vesicles, and minerals are annotated.

Figure 2.

Schematic diagram summarizing the morphological characteristics used to describe alteration textures. The box (top left) shows the main alteration morphotypes: tubular, granular, and the less common sub-types of buds and bubbles. In the rest of the figure, seven characteristics are illustrated with line diagrams: (1) length and width; (2) density; (3) curvature; (4) roughness; (5) variations in width; (6) branching; and (7) tunnel contents. Each of the morphological forms is given a simple descriptive term, and a typical example from our photographic atlas is given. Descriptive terms are defined in Table 2. This diagram expands on the ichnotaxonomic classification scheme shown in McLoughlin et al. (2009, their figure 1).

Figure 2.

Schematic diagram summarizing the morphological characteristics used to describe alteration textures. The box (top left) shows the main alteration morphotypes: tubular, granular, and the less common sub-types of buds and bubbles. In the rest of the figure, seven characteristics are illustrated with line diagrams: (1) length and width; (2) density; (3) curvature; (4) roughness; (5) variations in width; (6) branching; and (7) tunnel contents. Each of the morphological forms is given a simple descriptive term, and a typical example from our photographic atlas is given. Descriptive terms are defined in Table 2. This diagram expands on the ichnotaxonomic classification scheme shown in McLoughlin et al. (2009, their figure 1).

Figure 3.

(A) Tan glass (upper and lower areas of photo) with a fracture filled with banded, yellow to tan palagonite. The border of the glass with the palagonite (arrows) has a granular texture. The lower border is darker than the upper border. (B) Light-tan glass in the lower part of the photo, palagonite in the upper part of the photo with a granular boundary at the palagonite/glass interface. A crystalline quench feature (variole) is on the right side; a microphenocryst is below the focal plane in the center of the palagonite.

Figure 3.

(A) Tan glass (upper and lower areas of photo) with a fracture filled with banded, yellow to tan palagonite. The border of the glass with the palagonite (arrows) has a granular texture. The lower border is darker than the upper border. (B) Light-tan glass in the lower part of the photo, palagonite in the upper part of the photo with a granular boundary at the palagonite/glass interface. A crystalline quench feature (variole) is on the right side; a microphenocryst is below the focal plane in the center of the palagonite.

Figure 4.

(A) Circular alteration features along a fracture. The center of the fracture is palagonite, which is surrounded by a band of dark granular texture at the palagonite/glass border. A mossy texture extends from the granular band into the glass. (B) Short, dark, rough tunnels <5 μm wide and <20 μm long at the glass/granular-alteration boundary. Mossy tunnels appear to be random as opposed to directed tunnels.

Figure 4.

(A) Circular alteration features along a fracture. The center of the fracture is palagonite, which is surrounded by a band of dark granular texture at the palagonite/glass border. A mossy texture extends from the granular band into the glass. (B) Short, dark, rough tunnels <5 μm wide and <20 μm long at the glass/granular-alteration boundary. Mossy tunnels appear to be random as opposed to directed tunnels.

Figure 5.

(A) Five styles of alteration are illustrated: (i) granular, (ii) mossy, (iii) simple directed tunnel with constant width, (iv) kinked directed tunnel, and (v) random tunnels. (B) Simple 50-μm-long, 3–5-μm-wide tunnels radiate from a central point on the edge of a fracture at high angles.

Figure 5.

(A) Five styles of alteration are illustrated: (i) granular, (ii) mossy, (iii) simple directed tunnel with constant width, (iv) kinked directed tunnel, and (v) random tunnels. (B) Simple 50-μm-long, 3–5-μm-wide tunnels radiate from a central point on the edge of a fracture at high angles.

Figure 6.

(A) Long, directed tunnels extend more than 500 μm from the granular and mossy texture at the right edge of the glass. Tunnels are ∼3 μm wide. (B) Simple, short, close tunnels extending from clay along the margin of an olivine grain and from an area of bubble texture. These tunnels are 1–2 μm wide and 10 μm long and 1 or 2 μm apart. Nearby bubble texture has no tunnels emerging from it.

Figure 6.

(A) Long, directed tunnels extend more than 500 μm from the granular and mossy texture at the right edge of the glass. Tunnels are ∼3 μm wide. (B) Simple, short, close tunnels extending from clay along the margin of an olivine grain and from an area of bubble texture. These tunnels are 1–2 μm wide and 10 μm long and 1 or 2 μm apart. Nearby bubble texture has no tunnels emerging from it.

Figure 7.

(A) Close, smooth tunnels are 5–7 μm wide and 30–40 μm apart along the fracture. (B) Separated tunnels (the spacing along the fracture is more than 10 times the tunnel width). In this case, the tunnel width is 5–7 μm and the distance between them is 100 μm. These channels are ornamented with 3–5 μm extensions and contain septa.

Figure 7.

(A) Close, smooth tunnels are 5–7 μm wide and 30–40 μm apart along the fracture. (B) Separated tunnels (the spacing along the fracture is more than 10 times the tunnel width). In this case, the tunnel width is 5–7 μm and the distance between them is 100 μm. These channels are ornamented with 3–5 μm extensions and contain septa.

Figure 8.

(A) Thin, <3-μm-wide, directed, hair tunnels originating from the edge of the fracture. The fracture contains a 10-μm-wide layer of brown material adjacent to the glass. The image also contains tunnels that randomly change direction within a segment of the tunnel. A tunnel may have more than one of these tangled regions. (B) Alternating dark and light concentric rings in yellow palagonite are centered along the fracture. Granular texture extends from the fracture or from the concentric rings to a dark granular zone. Short, wide, granular incursions emerge from the dark, granular texture. The fracture is filled with an undetermined white transparent mineral.

Figure 8.

(A) Thin, <3-μm-wide, directed, hair tunnels originating from the edge of the fracture. The fracture contains a 10-μm-wide layer of brown material adjacent to the glass. The image also contains tunnels that randomly change direction within a segment of the tunnel. A tunnel may have more than one of these tangled regions. (B) Alternating dark and light concentric rings in yellow palagonite are centered along the fracture. Granular texture extends from the fracture or from the concentric rings to a dark granular zone. Short, wide, granular incursions emerge from the dark, granular texture. The fracture is filled with an undetermined white transparent mineral.

Figure 9.

(A) Directed, simple, empty tunnels with a constant width of 5 μm emerge from granular material. The granular alteration is separated from an original fracture by a crack that was produced possibly during the manufacture of the thin section. Yellow granular material has replaced glass along the original fracture. (B) Kinked, directed, opaque tunnels ∼3 μm wide emerge from the dark granular material. A fracture just visible in the upper right of the photo is surrounded by palagonite that grades from yellow to brown to black.

Figure 9.

(A) Directed, simple, empty tunnels with a constant width of 5 μm emerge from granular material. The granular alteration is separated from an original fracture by a crack that was produced possibly during the manufacture of the thin section. Yellow granular material has replaced glass along the original fracture. (B) Kinked, directed, opaque tunnels ∼3 μm wide emerge from the dark granular material. A fracture just visible in the upper right of the photo is surrounded by palagonite that grades from yellow to brown to black.

Figure 10.

(A) Smooth, simple, 5–10-μm-wide tunnels emerge from yellow granular alteration. Two tunnels are indicated with arrows. (B) Simple tunnels with rough surfaces emerge from brown alteration at the edge of a fracture. Tunnels are 5–10 μm wide.

Figure 10.

(A) Smooth, simple, 5–10-μm-wide tunnels emerge from yellow granular alteration. Two tunnels are indicated with arrows. (B) Simple tunnels with rough surfaces emerge from brown alteration at the edge of a fracture. Tunnels are 5–10 μm wide.

Figure 11.

(A) 15-μm-wide tunnel with rough exterior expands at the end to ∼35 μm wide. The tunnel also has an enlargement in the midsection. Short tunnels, 5–10 μm long, also emerge from the fracture in lower part of the photo. (B) Fracture in the lower left contains brown fill and is surrounded by altered glass. From this comes wide (10–15 μm), rough tunnels that taper to 10 μm or less at their ends and have an intermediate enlargement (15–20 μm wide) with a single ovoid body with dark edges.

Figure 11.

(A) 15-μm-wide tunnel with rough exterior expands at the end to ∼35 μm wide. The tunnel also has an enlargement in the midsection. Short tunnels, 5–10 μm long, also emerge from the fracture in lower part of the photo. (B) Fracture in the lower left contains brown fill and is surrounded by altered glass. From this comes wide (10–15 μm), rough tunnels that taper to 10 μm or less at their ends and have an intermediate enlargement (15–20 μm wide) with a single ovoid body with dark edges.

Figure 12.

(A) Fractures with several styles of alteration. Yellow granular alteration occurs at the margins of the fractures. Mossy alteration and 3-μm-wide tunnels with variable width emerge from the fracture on the left. Annulated tunnels and tunnels with club-shaped ends emerge from the fracture with yellow fill. (B) Fracture surrounded by several styles of alteration, one of these (arrow) being a smooth tunnel, 5 μm wide, that has a 25-μm-wide, dark disk 100 μm from the fracture and 60 μm from the tunnel terminus.

Figure 12.

(A) Fractures with several styles of alteration. Yellow granular alteration occurs at the margins of the fractures. Mossy alteration and 3-μm-wide tunnels with variable width emerge from the fracture on the left. Annulated tunnels and tunnels with club-shaped ends emerge from the fracture with yellow fill. (B) Fracture surrounded by several styles of alteration, one of these (arrow) being a smooth tunnel, 5 μm wide, that has a 25-μm-wide, dark disk 100 μm from the fracture and 60 μm from the tunnel terminus.

Figure 13.

(A) Smooth, 10-μm-wide tunnel with spiral filament has repeated rings (annulations) every 3–5 μm near its end. The photo also contains smooth, thin, simple tunnels on both sides of a fracture that runs vertically through the image, and thin, kinked, dark tunnels on the left side of the image. (B) Fracture with little alteration has three smooth fingers or tunnels of variable width that taper from 10 μm at their bases to points ∼30 μm from the fracture. Brown patches are areas of quench crystals and varioles.

Figure 13.

(A) Smooth, 10-μm-wide tunnel with spiral filament has repeated rings (annulations) every 3–5 μm near its end. The photo also contains smooth, thin, simple tunnels on both sides of a fracture that runs vertically through the image, and thin, kinked, dark tunnels on the left side of the image. (B) Fracture with little alteration has three smooth fingers or tunnels of variable width that taper from 10 μm at their bases to points ∼30 μm from the fracture. Brown patches are areas of quench crystals and varioles.

Figure 14.

(A) There is a fracture in the lower left from which a tunnel that is 20 μm wide expands to 40 μm just below a mushroom-shaped cap that is 70 μm wide. (B) Fracture runs diagonally from the upper left corner and has smooth tunnels, three of which are broad and flattened, petal shapes. One (i) has a honeycomb constructed of 5–10-μm-wide cellular pattern. Another (ii) has dark lineaments spaced 5 μm apart. Boxed areas are shown in Figure 15. Spotted texture is an artifact of thin section production.

Figure 14.

(A) There is a fracture in the lower left from which a tunnel that is 20 μm wide expands to 40 μm just below a mushroom-shaped cap that is 70 μm wide. (B) Fracture runs diagonally from the upper left corner and has smooth tunnels, three of which are broad and flattened, petal shapes. One (i) has a honeycomb constructed of 5–10-μm-wide cellular pattern. Another (ii) has dark lineaments spaced 5 μm apart. Boxed areas are shown in Figure 15. Spotted texture is an artifact of thin section production.

Figure 15.

(A) Flattened petal-shaped tunnels have a 10-μm-wide cell-like pattern of dark partitions. (B) Flattened petal-shaped tunnel with ribs separated by 5 μm. Smooth tunnel with spiral filament is on the left side of the photograph.

Figure 15.

(A) Flattened petal-shaped tunnels have a 10-μm-wide cell-like pattern of dark partitions. (B) Flattened petal-shaped tunnel with ribs separated by 5 μm. Smooth tunnel with spiral filament is on the left side of the photograph.

Figure 16.

(A) Two short, wide (15–20 μm), smooth, round, yellow-brown buds extend from the granular area next to the fracture. Also present is a row of tunnels that are truncated at the upper and lower surfaces of the thin section. (B) Coalesced 5–8-μm-diameter spheres produce a bubble texture. The bubbles grade from transparent yellow spheres on the left to brown spheres with dark rims.

Figure 16.

(A) Two short, wide (15–20 μm), smooth, round, yellow-brown buds extend from the granular area next to the fracture. Also present is a row of tunnels that are truncated at the upper and lower surfaces of the thin section. (B) Coalesced 5–8-μm-diameter spheres produce a bubble texture. The bubbles grade from transparent yellow spheres on the left to brown spheres with dark rims.

Figure 17.

(A) A 10-μm-wide fracture has 5–10-μm-diameter spherical buds along its edge. The buds lack any internal structure and are not granular. (B) Simple branching; a single tunnel can have more than one node. Branches have the same diameter as the trunk. Tunnel width varies in a sawtooth or thorny pattern.

Figure 17.

(A) A 10-μm-wide fracture has 5–10-μm-diameter spherical buds along its edge. The buds lack any internal structure and are not granular. (B) Simple branching; a single tunnel can have more than one node. Branches have the same diameter as the trunk. Tunnel width varies in a sawtooth or thorny pattern.

Figure 18.

(A) Dark, 1-μm-wide, separated, branched tunnels form random networks that extend 50–60 μm from the fracture. (B) Semicircular palagonite area is centered on a fracture (top of photo) and surrounded by a black mass of kinked tunnels. Branched, straight, dark tunnels are 3–5 μm wide. 30-μm-long tunnels with undulating, smooth outlines emerge from the black mess. The branches fork at ∼60° angles from each other. Most appear to have only one branch per tunnel. Boxed area enlarged in Figure 19A.

Figure 18.

(A) Dark, 1-μm-wide, separated, branched tunnels form random networks that extend 50–60 μm from the fracture. (B) Semicircular palagonite area is centered on a fracture (top of photo) and surrounded by a black mass of kinked tunnels. Branched, straight, dark tunnels are 3–5 μm wide. 30-μm-long tunnels with undulating, smooth outlines emerge from the black mess. The branches fork at ∼60° angles from each other. Most appear to have only one branch per tunnel. Boxed area enlarged in Figure 19A.

Figure 19.

(A) Annulated tunnels branch at 60° angle. Mossy, kinked tunnels also branch. (B) Fracture at the bottom of the photo has granular alteration along one side that grades into a dark zone. Emerging from the dark zone are kinked, dark, branched, random tunnels that are ∼3 μm wide and 30–50 μm long. This is the type specimen of Tubulohyalichnus stipes isp., first described in McLoughlin et al. (2009).

Figure 19.

(A) Annulated tunnels branch at 60° angle. Mossy, kinked tunnels also branch. (B) Fracture at the bottom of the photo has granular alteration along one side that grades into a dark zone. Emerging from the dark zone are kinked, dark, branched, random tunnels that are ∼3 μm wide and 30–50 μm long. This is the type specimen of Tubulohyalichnus stipes isp., first described in McLoughlin et al. (2009).

Figure 20.

(A) Fracture at the bottom of the photo has tunnels up to 300 μm long emerging from it. One tunnel branches at nodes into a palmate arrangement of tunnels that terminate in 2 μm bulbs. Some tunnels are annulated; one has a petal shape. Some branches emerge from an expanded node; some tunnels are partitioned with a filigree of dark material. (B) Fracture (out of view below the bottom of the photo) is surrounded by reddish palagonite (granular texture), which grades into a dark zone. Emerging from the dark zone are dark, simple tunnels that are 5–10 μm wide. Some have blunt terminations as close as 10 μm to the dark zone. Others penetrate 100–120 μm into the glass and expand to 20 μm wide or produce crowns of 3–5-μm-wide tunnels that end in bulbs.

Figure 20.

(A) Fracture at the bottom of the photo has tunnels up to 300 μm long emerging from it. One tunnel branches at nodes into a palmate arrangement of tunnels that terminate in 2 μm bulbs. Some tunnels are annulated; one has a petal shape. Some branches emerge from an expanded node; some tunnels are partitioned with a filigree of dark material. (B) Fracture (out of view below the bottom of the photo) is surrounded by reddish palagonite (granular texture), which grades into a dark zone. Emerging from the dark zone are dark, simple tunnels that are 5–10 μm wide. Some have blunt terminations as close as 10 μm to the dark zone. Others penetrate 100–120 μm into the glass and expand to 20 μm wide or produce crowns of 3–5-μm-wide tunnels that end in bulbs.

Figure 21.

(A) Separated, smooth tunnels, 3–4 μm wide and 20 μm long, with crowns composed of multiple, dark helixes that are 1 μm wide. (B) Three forms of tunnel filling of simple, directed, smooth tunnels: granular, intermittent dark material, and continuous dark material.

Figure 21.

(A) Separated, smooth tunnels, 3–4 μm wide and 20 μm long, with crowns composed of multiple, dark helixes that are 1 μm wide. (B) Three forms of tunnel filling of simple, directed, smooth tunnels: granular, intermittent dark material, and continuous dark material.

Figure 22.

(A) Smooth, simple, 2-μm-wide tunnels contain 2 μm ovoid bodies spaced 10–20 μm apart and septae that divide the tunnel at 2 μm intervals. (B) Tapering tunnels with intermediate enlargements that are divided by dark partitions.

Figure 22.

(A) Smooth, simple, 2-μm-wide tunnels contain 2 μm ovoid bodies spaced 10–20 μm apart and septae that divide the tunnel at 2 μm intervals. (B) Tapering tunnels with intermediate enlargements that are divided by dark partitions.

Figure 23.

(A) Dark alteration at the right of the figure has a single, rough, variable-width tunnel that is 100 μm long and expands from 12 μm at its base to 20 μm just below the 30-μm-wide, rough crown. The tunnel has prominent septae and an enlarged segment below the crown. (B) Smooth, simple, 5-μm-wide tunnels contain spiral filaments. One tunnel may also have a filament and septae.

Figure 23.

(A) Dark alteration at the right of the figure has a single, rough, variable-width tunnel that is 100 μm long and expands from 12 μm at its base to 20 μm just below the 30-μm-wide, rough crown. The tunnel has prominent septae and an enlarged segment below the crown. (B) Smooth, simple, 5-μm-wide tunnels contain spiral filaments. One tunnel may also have a filament and septae.

Figure 24.

(A) Fracture at the left has separated patches of dark, granular material. From one of these patches emerges a 1–2-μm-wide, simple, directed, convoluted tunnel with dark contents. (B) Annulated tunnel contains a 10-μm-wide and 20-μm-long, brown oval.

Figure 24.

(A) Fracture at the left has separated patches of dark, granular material. From one of these patches emerges a 1–2-μm-wide, simple, directed, convoluted tunnel with dark contents. (B) Annulated tunnel contains a 10-μm-wide and 20-μm-long, brown oval.

Figure 25.

(A) A group of tunnels radiate from a center on a fracture at the right of the photo. One smooth, 8-μm-wide tunnel in the group contains numerous 8 μm × 5 μm ovals that are 5–10 μm apart. A second tunnel also contains ovals. (B) A 3–5-μm-wide fracture with granular alteration along its edges and rough, simple tunnels (5–10 μm wide and up to 40 μm long) with rough crowns, 10–20 μm wide. Tunnels vary in width and several have three bulges plus the crown.

Figure 25.

(A) A group of tunnels radiate from a center on a fracture at the right of the photo. One smooth, 8-μm-wide tunnel in the group contains numerous 8 μm × 5 μm ovals that are 5–10 μm apart. A second tunnel also contains ovals. (B) A 3–5-μm-wide fracture with granular alteration along its edges and rough, simple tunnels (5–10 μm wide and up to 40 μm long) with rough crowns, 10–20 μm wide. Tunnels vary in width and several have three bulges plus the crown.

Figure 26.

(A) A fracture cuts across the center of the photo. Two spherical vesicles, one 70 μm in diameter and the other 30 μm in diameter, are above the fracture. Empty, rough tunnels with broadened crowns extend from the rims of the vesicles. (B) Smooth, simple, 1–3-μm-wide tunnels emerge from the rim of a vesicle. The vesicle contains tan clay and an opaque sulfide. The tunnels extend from the vesicle in opposite directions. Some tunnels contain ovoid bodies. The photo also shows two smooth tunnels with ovoid bodies that are not connected to the vesicle and which wrap around an olivine microphenocryst.

Figure 26.

(A) A fracture cuts across the center of the photo. Two spherical vesicles, one 70 μm in diameter and the other 30 μm in diameter, are above the fracture. Empty, rough tunnels with broadened crowns extend from the rims of the vesicles. (B) Smooth, simple, 1–3-μm-wide tunnels emerge from the rim of a vesicle. The vesicle contains tan clay and an opaque sulfide. The tunnels extend from the vesicle in opposite directions. Some tunnels contain ovoid bodies. The photo also shows two smooth tunnels with ovoid bodies that are not connected to the vesicle and which wrap around an olivine microphenocryst.

Figure 27.

(A) A vesicle lined with light-tan clay. The glass rim of the vesicle has been altered to granular palagonite. Granular incursions into the glass are 5–20 μm wide at their contact with the granular/glass boundary and have rough crowns that are 20 μm wide. (B) A dark brown, 150-μm-long and 70-μm-wide variole has numerous empty, smooth tunnels that are 1–3 μm wide and up to 80 μm long that emerge from the contact of the spherule with glass. The tunnels only emerge from the side of the variole that faces the fracture. At the top of the photo, there is a fracture surrounded with light-colored alteration with a dark border and associated, dark, kinked tunnels.

Figure 27.

(A) A vesicle lined with light-tan clay. The glass rim of the vesicle has been altered to granular palagonite. Granular incursions into the glass are 5–20 μm wide at their contact with the granular/glass boundary and have rough crowns that are 20 μm wide. (B) A dark brown, 150-μm-long and 70-μm-wide variole has numerous empty, smooth tunnels that are 1–3 μm wide and up to 80 μm long that emerge from the contact of the spherule with glass. The tunnels only emerge from the side of the variole that faces the fracture. At the top of the photo, there is a fracture surrounded with light-colored alteration with a dark border and associated, dark, kinked tunnels.

Figure 28.

(A) A fracture on the left and a dark quench feature (variole) on the right are connected by clear, smooth tunnels that are 1–3 μm wide and 150–200 μm long. (B) A thin, directed network of branched tunnels between the fracture on the left and olivine microphenocryst on the right. In some locations, the network appears to initiate from the olivine and in others, it emerges from the fracture.

Figure 28.

(A) A fracture on the left and a dark quench feature (variole) on the right are connected by clear, smooth tunnels that are 1–3 μm wide and 150–200 μm long. (B) A thin, directed network of branched tunnels between the fracture on the left and olivine microphenocryst on the right. In some locations, the network appears to initiate from the olivine and in others, it emerges from the fracture.

Figure 29.

(A) Glass that once surrounded a vesicle has been replaced with palagonite. The outlines of smooth, tapered tunnels with dark tips that surround the vesicle are preserved. (B) Fracture in the lower part of the photo has dark networks of tunnels that were overprinted with secondary alteration that left parallel dark laminations outlining the groups of tunnels. A second episode of similar tunnels formed along the dark upper margin of the alteration.

Figure 29.

(A) Glass that once surrounded a vesicle has been replaced with palagonite. The outlines of smooth, tapered tunnels with dark tips that surround the vesicle are preserved. (B) Fracture in the lower part of the photo has dark networks of tunnels that were overprinted with secondary alteration that left parallel dark laminations outlining the groups of tunnels. A second episode of similar tunnels formed along the dark upper margin of the alteration.

Figure 30.

(A) A fracture across the lower part of the photo is bordered by an early stage of dark, granular alteration (1). This is followed by hemispherical alteration centered on what is assumed to be the edge of an advancing alteration front (2). A second dark zone (3) is associated with dark, mossy alteration. The final glass/alteration boundary is dark and rough (4). The white crack occurred during or after sample collection. (B) Granular texture surrounded by 5–8-μm-wide, tapered channels. Similar but slightly larger tunnels are present to the right of the granular texture and are overprinted with palagonite.

Figure 30.

(A) A fracture across the lower part of the photo is bordered by an early stage of dark, granular alteration (1). This is followed by hemispherical alteration centered on what is assumed to be the edge of an advancing alteration front (2). A second dark zone (3) is associated with dark, mossy alteration. The final glass/alteration boundary is dark and rough (4). The white crack occurred during or after sample collection. (B) Granular texture surrounded by 5–8-μm-wide, tapered channels. Similar but slightly larger tunnels are present to the right of the granular texture and are overprinted with palagonite.

Figure 31.

Simple, smooth, empty tunnels start at the granular boundary of the fracture and extend parallel to the fracture. Tunnels are 5 μm wide and 40 μm long or longer. Granular texture extends 5–20 μm from the edge of the fracture.

Figure 31.

Simple, smooth, empty tunnels start at the granular boundary of the fracture and extend parallel to the fracture. Tunnels are 5 μm wide and 40 μm long or longer. Granular texture extends 5–20 μm from the edge of the fracture.

Features are first separated into major categories of granular and tubular forms (Fig. 2, upper left panel) as previously described (Furnes et al., 2001a). In addition to the granular form, a bud-shaped form is recognized here that is an intermediate form between granular and tubular. The photographs are grouped by the primary feature that is being illustrated such as granular forms, simple tubes, branching, distribution, and overprinting. In many photographs, more than one textural feature is present but typically only the feature being demonstrated is described. A glossary of terms is provided in Table 2 to aid in the description of the alteration features. In the text below, terms that are from the glossary are italicized.

TABLE 2.

GLOSSARY OF TERMS, DESCRIPTIONS, AND ILLUSTRATIVE FIGURES SPECIFIC TO THIN SECTIONS IN THIS STUDY

Tubular Alteration

The tunnel forms are more complex and varied than granular textures and are therefore further characterized by their shape, density, contents, and their relationship to other features in the thin sections such as fractures and vesicles. Seven major characteristics are used to describe the variety of tunnel morphologies. These are: (1) size (length and width); (2) spacing between similar tunnels; (3) curvature; (4) roughness; (5) changing width along the length of the tunnel; (6) branching; and (7) tunnel contents. In addition we recognize differences in how tunnels are distributed relative to fractures, minerals, and vesicles, and we note that some thin sections have a single type of alteration but others exhibit multiple forms.

The term thin is applied to tunnel widths (diameters) less than 3 µm from edge to edge (Fig. 8A) and long tunnels are more than 50 times longer than they are wide (Fig. 6A). The length of short tunnels is less than 10 times their width (Fig. 6B). The density term (Fig. 2) is based on how closely packed the tunnels are along the fracture or other surface from which they originate: close tunnels have a center-to-center distance that is less than 10 times the tunnel width (Fig. 7A), whereas the center-to-center distance of separated tunnels are apart by more than 10 times their diameters (Fig. 7B). Tunnels are usually curved and directed, such as away from a fracture (e.g., Figs. 5A, 6A). These directed tunnels can be nearly linear (curvilinear), kinked with sharp changes in direction (Figs. 5A, 9B), or appear have a tangled knotted appearance along their length (Fig. 8A). Convoluted tunnels turn back toward their point of origin (e.g., Fig. 24A) and do not appear to be directed away from their point of origin. Some tunnels have nearly constant width ±20% over their entire lengths (Figs. 5A, 7A), but others are variable (e.g., Figs. 14, 15, 20). Some taper from their origin at a free surface to a point in the glass (Fig. 13B). Others have repeated variations in their width resulting in a rhythmic annulated tunnel (Fig. 13A), or have a single bump between the tunnel origin and end termed engorged tunnels (Figs. 11B, 22B), or multiple irregular bumps (Fig. 12A). Rarely, a tunnel will broaden into a mushroom shape (Fig. 14A) or central disk (Fig. 12B). In addition to tunnels of variable width, there are round bud and bubble textures that are present at the margins of fractures (Figs. 16, 17A).

The surfaces of some tunnels are smooth, having irregularities that are less than 0.5 μm (Fig. 10A). Rough tunnel walls (Figs. 7B, 10B, 11) are embellished with fine (>1 μm) extensions into the glass uniformly or periodically distributed along the tunnel. The widths of individual extensions from the walls of tunnels are much thinner than the width of the tunnel. In contrast to this, branches (Fig. 2) are commonly the same width as the main tunnel. Branching may be simple with the nodes widely spaced along a tunnel, (Fig. 17B), or mossy (Fig. 4A), or networks (Figs. 18A, 19), where branches are crowded together and branch repeatedly. In the case of simple, mossy, or network branching, daughter branches are the same diameter as the parent branch. In other cases branches are narrower than their parent tunnels (Figs. 20, 21A). Some tunnels have crowns, composed of multiple radiating tunnels that have a different form than the tunnel from which they originate (Figs. 21A, 23A, 25B).

Content of Alteration Textures

The contents of tunnels can vary as well. Some tunnels appear to be empty (Fig. 9A), but others are partially or completely filled (Fig. 21B) with opaque material. Tunnel contents can be segregated into oval or ovoid bodies typically 1–2 μm in diameter that are commonly evenly distributed along the interior of the tunnel (e.g., Figs. 22A, 25A). However, a single, large, 20 μm ovoid body is present in some tunnels and the tunnel walls swell around the body (Fig. 11). In one example the large ovoid body is divided by dark septae into five separate bodies (Fig. 22B). Septae can also divide a tunnel into multiple chambers that are 5–10 μm long (e.g., Figs. 22A, 23). Broad flat tunnels are divided by a honeycomb or patterned with a filigree of dark material (Figs 14B, 15). Tunnels may also have spiral filaments (e.g., Figs. 13A, 23B).

Distribution and Directionality of Alteration

The distribution of alteration textures within glass has also been documented in this study. Tunnels are usually found distributed along fractures (e.g., Figs. 5A, 6A) but sometimes they are distributed around vesicles (Figs. 26, 27A, 29A), varioles (Figs. 27B, 28A), or phenocrysts and microphenocrysts (Figs. 6B, 28B). Tunnels are commonly directed away from fractures, but sometimes they are parallel to fractures (Fig. 31). Tunnels may also radiate from a point at the edge of a fracture (Fig. 5B). Some tunnels turn sharply from their initial direction perpendicular to the surface where they originate to a direction parallel to the alignment of other tunnels in the glass (Fig. 26B). In one example, the alignment of tunnels is parallel to the major axis of elongation of vesicles in the glass (not shown).

Timing of Alteration

The photographs also illustrate the temporal relationship of alteration in some samples. For example, Figure 29A shows tapered tunnels radiating from a vesicle. Originally the tunnels extended into glass, but the vesicle, tunnels, and surrounding glass have now been replaced with phyllosilicate. Overprinting of a network is obvious in Figure 29B. Here a granular border evolves into a dark network in glass in the upper half of Figure 29B. In the lower half of the figure, glass containing a previous dark network has been transformed into a yellow phyllosilicate. In Figure 30A a semicircular alteration pattern, which is similar to that in Figure 8B, has been replaced by a subsequent phase of alteration, which suggests conditions changed during the formation of this alteration boundary.

STATE OF KNOWLEDGE ON ALTERATION TEXTURES IN VOLCANIC GLASS

This Atlas Compared to Earlier Studies

Morgenstein (1969) illustrated granular and tubular textures in three dredged basalts from the Mid-Atlantic Ridge and one from a fracture zone along the Pacific-Antarctic Ridge. His transmitted-light images showed granular alteration forming a semicircle around a fracture (similar to Fig. 4A) and 20-µm-wide zones between glass and palagonite along fractures (similar to Fig. 4B). His photographs also include what he called “hair tunnels” (see Table 2) extending 50 μm from a granular texture into glass (similar to Fig. 6A) and from fractures into glass (similar to Fig. 9A). He also described a “solid solution” border that is similar to the dark zone between glass and palagonite (Fig. 4).

It was not until 1996 that tubular and granular features were again emphasized and documented with transmitted-light photomicrographs (Giovannoni et al., 1996). Also at this time and from the same Costa Rica Rift site, granular and tubular features were illustrated in backscattered electron images (Furnes et al., 1996). More detailed close-up photomicrographs (Fisk et al., 1998a) illustrated that the tubular phenomenon was more varied than the tunnels seen in Costa Rica Rift basalts. In these new photographs, mossy and branching tunnels, granular alteration, as well as tunnels with pronounced septae and cell-sized inclusions were illustrated from separate seamounts in the Pacific Ocean (one dredged and one cored basalt), from the Mid-Atlantic Ridge (two cored basalts), and from the Indian Ocean (one cored basalt) (Fisk et al., 1998a).

In the 2000s the growing literature of oceanic glass alteration reported additional morphologies including: budding along a tunnel (Furnes et al., 2000a), similar to what we have called tangled texture (Fig. 8A), and bifurcating tunnels (Furnes et al., 2001a, 2002). Annulated and convoluted tunnels were described by Banerjee and Muehlenbachs (2003) in basalts from the Ontong Java Plateau, which we have also illustrated with samples from Chagos Ridge (Fig. 13A) and from the Philippine Sea (Fig. 24A), respectively. Josef (2006) identified a number of textures not previously described, such as mushroom (Fig. 14A) and engorged (Fig. 11B). Networks of branched tunnels were first described by McLoughlin et al. (2009), and the type example is illustrated in Figure 19B. Here we also report networks made of thinner branched tunnels (Figs. 18A, 28B).

Comparison to an Ichnotaxonomic Classification

An ichnotaxonomic framework was advanced for glass alteration by McLoughlin et al. (2009) that considers the textures as trace fossils, and two new ichnogenera were proposed, corresponding to the two broad granular and tubular morphotypes discussed here and in earlier reports. Five ichnospecies were also defined on the basis of morphological characteristics and these are compared to the range of textures illustrated here, which includes new morphological variants:

  1. Granulohyalichnus vulgaris isp. has a granular form (McLoughlin et al., 2009, their figure 2), and is very common and comparable to the examples illustrated here (e.g., Figs. 3 and 4).

  2. Tubulohyalichnus simplus isp. has an unornamented tubular form (McLoughlin et al., 2009, their figure 3). This alteration morphology is also illustrated here (Figs. 5–31) and with further descriptors including short or long, thick or thin, closely spaced or separated, curvilinear, smooth, or constant width, possibly with tunnel contents (Fig. 2).

  3. Tubulohyalichnus annularis isp. has an annulated tubular form (McLoughlin et al., 2009, their figure 4). This morphotype is also illustrated here (Fig. 13A); however, we have subdivided the annulated type further into those with regularly sized and spaced annulations (Fig. 13A), and those with irregularly sized and spaced annulations termed engorged and bumpy (Figs. 11B and 12A, respectively). The latter can be compared to the “string-of-beads” form previously described by Fisk et al. (1998a).

  4. Tubulohyalichnus spiralis isp. has a helicoidal tubular form with a coiled or helical axis (McLoughlin et al., 2009, their figure 5), with up to 12 rotations reported, and can be either sinistrally or dextrally coiled. This ichnospecies may show a linear or curved growth axis with the spacing and diameter of the whorls changing along its length. This morphotype was not identified in the selection of sub-seafloor samples described here, although we did find spiral-shaped filaments within some of the tunnels (Fig. 23B) and extending from the crown in another example (Fig. 21A).

  5. Tubulohyalichnus stipes isp. has a branched tubular form (McLoughlin et al., 2009, their figure 6) with dichotomously branching tubes, in which the diameters of the daughter branches are equal to that of the parent branches, and occur in dense intergrowths that may be hemispherical-shaped clusters or more irregular bands. The type material is illustrated in this atlas (Fig. 19B); however, many additional variations of branching are also illustrated here, for example, with more widely spaced branches (Fig. 17B) or palmate crowns (Fig. 20A).

Tunnel Contents

The contents of tunnels have been noted in previous photomicrographs (Fisk et al., 1998a; Josef, 2006), and here tunnel contents are used as a distinguishing characteristic of the alteration. Tunnels are often transparent and apparently empty; however, others have dark contents (Fig. 21B) that we interpret to be either foreign material introduced during drilling, sampling, or thin-section preparation, or alternatively as primary organic residue (cf. Preston et al., 2011). The single or multiple ovoid bodies spaced along the tunnel (Fig. 22A) are intriguing, and further investigation, for example with fluorescent microscopy techniques, could test the hypothesis that they are cellular bodies. The origin of septae (Fig. 23), spiral filaments, ornaments inside tunnels (Fig. 23B), and petaloid or flattened tubes with ribbing and/or honeycomb ornament (Fig. 14B, 15) may be revealed with microanalytical techniques (Alt and Mata, 2000; Knowles et al., 2011a, 2011b).

Environmental Controls on Alteration

We expect that certain styles of alteration of basalt glass will be correlated with environmental variables at the time of alteration. Factors such as temperature, aqueous chemistry, and oxygen abundance are known to affect the secondary mineral chemistry and therefore assumedly the textural styles of alteration. In one attempt to relate alteration styles to environmental conditions, Josef (2006) studied 140 thin sections from 63 DSDP and IODP boreholes and found no correlation. This may be because in the sub-seafloor the temperature and composition of the formation water are usually not measured and must be inferred, and the conditions at the time of sample collection may not represent the conditions when the alteration occurred.

In another study at DSDP Site 504B and ODP Site 896A of the 5.9 Ma Costa Rica Rift, Furnes and Staudigel (1999) and Staudigel et al. (2006) compared the abundance of granular and tubular alteration, which was determined by point counting, with measured and inferred subsurface conditions in the ocean crust. At these sites, measured temperatures increase with depth, and porosity is highest at ∼75 m below the sediment/basalt interface and decreases below this depth. Permeability also decreases with depth, and it is inferred that the oxygen content of formation fluids decreases with depth. They found that granular alteration was present from the basalt/sediment interface to a depth where the current temperature was ∼115 °C (500 m). Tubular alteration had a more restricted range, being rare near the basalt/sediment interface and at depths where the temperature was greater than 90 °C. The tubular style had a peak abundance of ∼10% at ∼120–130 m depth. This depth corresponds to a temperature of ∼70 °C where formation permeability is high and the presence of celadonite indicates that alteration occurred in a relatively oxidizing environment (Furnes and Staudigel, 1999; Furnes et al., 2001a). Their work shows that granular alteration is limited to temperatures less than 115 °C (500 m) and that tubular alteration is limited to shallower regions of the crust where temperatures are lower and fluid flow is likely to be higher than in deeper parts of the crust.

Boreholes on the flanks of Juan de Fuca and Mid-Atlantic Ridges that are fitted with devices (CORKs) that monitor physical and chemical conditions in the holes (Fisher et al., 2005, 2011; Expedition 336 Scientists, 2012) can also provide basalt samples in which alteration features can be documented. Although alteration textures may form at conditions different from the current conditions at the site, CORKed holes may enable studies where sub-seafloor environmental conditions are compared to the distribution, abundance, and variability in alteration features like those described in this atlas.

History of Alteration

The period over which the alteration textures in basalt glass forms is not known. The textures may form any time between eruption into the cold, oxygenated seawater to when the basalt is deeply buried and surrounded by warm anoxic fluids. In the shallow ocean crust at both the 5.9 Ma Costa Rica Rift and the 110 Ma Western Atlantic oceanic crust, there are similar maxima in the amount of granular and tubular alteration as a percentage of the total alteration (see Furnes et al., 2001a, their figure 11). This suggests that a substantial portion of this alteration is established early in the crustal history, i.e., within ∼6 m.y. Images presented here indicate that there can be at least two episodes of texture formation at some locations (Figs. 29, 30). These episodes probably reflect changing conditions in the seafloor; however, the time between these episodes of texture formation is not known.

SUMMARY

Alteration textures in oceanic basalt glass have been documented in a comprehensive sample set from the ocean basins (Fig. 1). The alteration textures originate at the glass/water interface both on the seafloor and along the fractures and surfaces of glass that is buried in the crust. The alteration transforms the glass to palagonite and creates cavities in the glass that exhibit a wide range of simple, intricate, or ornate forms, which are summarized in graphical form (Fig. 2) and documented in photomicrographs (Figs. 3–31). The photographs illustrate prevalent as well as rare forms. The granular form is common and it is often abundant along most of the altered fractures in some samples. Also quite common is a mossy texture. Tubular or tunnel forms are less common. Often cohorts of tunnels have a common orientation away from their region of origin and although within a few microns of each other they do not intersect. Some tunnels have random tracks and do not appear to be directed away from their point of origin. Tunnel diameters are often constant, not varying more than 20% over a 100 µm length of tunnel. In some basalts only a single type of alteration, such as the granular form, is present. However, some rocks contain multiple forms of alteration within a few tens of micrometers of each other. The superposition of alteration types in single thin sections probably reflects changing conditions in the sub-seafloor. The wide range of alteration features in some individual basalts suggests variations in chemical or physical conditions over time or on micrometer scales at a given time. The images presented here are a starting point for correlating alteration features with physical and chemical conditions in the seafloor. We consider the photographic atlas to be the current state of knowledge, which will likely be expanded as new features are discovered. Biogenicity has been proposed for alteration features that are similar to some of those illustrated here; however, if future work with microbial cultures and environmental samples documents the biogenic production of some features, we would not extend this interpretation to the broad range of features illustrated here.

Thanks to the U.S. Fulbright Program, the U.S.–Norway Fulbright Foundation, and the Centre for Geobiology at the University of Bergen for their financial support. The Centre for Geobiology was a gracious host during this study. Jeff Karson provided a scanned version of Maury Morgenstein’s Master’s thesis from the Syracuse University library. Samples were acquired from the Deep Sea Drilling Project and the Ocean Drilling Program sample repositories and funds for that travel to visit the repositories was provided by the National Science Foundation. J. Josef described many of the samples in this study in her Master’s thesis at Oregon State University (2006). Many of those samples were reexamined and re-photographed for this atlas and some of her descriptive terms were adopted.

REFERENCES CITED

1.
Alt
J.C.
Mata
P.
,
2000
,
On the role of microbes in the alteration of submarine basaltic glass
:
A TEM study: Earth and Planetary Science Letters
 , v.
181
, p.
301
313
,
doi:10.1016/S0012-821X(00)00204-1
.
2.
Bach
W.
Edwards
K.J.
,
2003
,
Iron and sulfide oxidation within the basaltic ocean crust: Implication for chemolithoautotrophic microbial biomass production
:
Geochimica et Cosmochimica Acta
 , v.
67
, p.
3871
3887
.
3.
Banerjee
N.R.
Muehlenbachs
K.
,
2003
,
Tuff life: Bioalteration in volcaniclastic rocks from the Ontong Java Plateau
:
Geochemistry Geophysics Geosystems
 , v.
4
,
1037
,
doi:10.1029/2002GC000470
.
4.
Benzerara
K.
Menguy
N.
Banerjee
N.R.
Tyliszczak
T.
Brown
G.E.
Jr
Guyot
F.
,
2007
,
Alteration of submarine basaltic glass from the Ontong Java Plateau: A STXM and TEM study
:
Earth and Planetary Science Letters
 , v.
260
, p.
187
200
,
doi:10.1016/j.epsl.2007.05.029
.
5.
Cockell
C.S.
Herrera
A.
,
2008
,
Why are some microorganisms boring?
:
Trends in Microbiology
 , v.
16
, p.
101
106
,
doi:10.1016/j.tim.2007.12.007
.
6.
Cockell
C.S.
Olsson
K.
Herrera
A.
Meunier
A.
,
2009
,
Alteration textures in terrestrial volcanic glass and the associated bacterial community
:
Geobiology
 , v.
7
, p.
50
65
,
doi:10.1111/j.1472-4669.2008.00184.x
.
7.
Cousins
C.R.
Smellie
J.L.
Jones
A.P.
Crawford
I.A.
,
2009
,
A comparative study of endolithic microborings in basaltic lavas from a transitional subglacial-marine environment
:
International Journal of Astrobiology
 , v.
8
, p.
37
49
,
doi:10.1017/S1473550408004369
.
8.
Christie
D.M.
et al
,
2001
,
Proceedings of the Ocean Drilling Program, Initial Reports, volume 187
:
College Station
,
Texas
, .
9.
Duennebier
R.
Blackinton
G.
,
1980
,
A man-made hot spring on the ocean floor
:
Nature
 , v.
284
, p.
338
340
,
doi:10.1038/284338a0
.
10.
Expedition 336 Scientists
,
2012
,
Mid-Atlantic Ridge microbiology: Initiation of long-term coupled microbiological, geochemical, and hydrological experimentation within the seafloor at North Pond, western flank of the Mid-Atlantic Ridge
:
Integrated Ocean Drilling Program Preliminary Report
 , v.
336
,
71
p.,
doi:10.2204/iodp.pr.336.2012
.
11.
Fisher
A.T.
et al
,
2005
,
Scientific and technical design and deployment of long-term subseafloor observatories for hydrogeologic and related experiments, IODP Expedition 301, eastern flank of Juan de Fuca Ridge
, in
Fisher
A.T.
Urabe
T.
Klaus
A.
,
and the Expedition 301 Scientists
,
Proceedings of the Integrated Ocean Drilling Program, volume 301
 :
College Station
,
Texas, Integrated Ocean Drilling Program Management International, Inc.
,
doi:10.2204/iodp.proc.301.103.2005
.
12.
Fisher
A.T.
et al
,
2011
,
Design, deployment, and status of borehole observatory systems used for single-hole and cross-hole experiments, IODP Expedition 327, eastern flank of Juan de Fuca Ridge
, in
Fisher
A.T.
Tsuji
T.
Petronotis
K.
,
and the Expedition 327 Scientists
,
Proceedings of the Integrated Ocean Drilling Program, volume 327
 :
Tokyo
,
Integrated Ocean Drilling Program Management International, Inc.
,
doi:10.2204/iodp.proc.327.107.2011
.
13.
Fisk
M.R.
Giovannoni
S.J.
,
1999
,
Sources of nutrients and energy for a deep biosphere on Mars
:
Journal of Geophysical Research
 , v.
104
, p.
11,805
11,815
,
doi:10.1029/1999JE900010
.
14.
Fisk
M.R.
Giovannoni
S.J.
Thorseth
I.H.
,
1998a
,
The extent of microbial life in the volcanic crust of the ocean basins
:
Science
 , v.
281
, p.
978
980
,
doi:10.1126/science.281.5379.978
.
15.
Fisk
M.R.
Thorseth
I.H.
Giovannoni
S.J.
Urbach
E.
Streck
M.
,
1998b
,
Endolithic microbes from the Rattlesnake Tuff, Oregon Blue Mountain region
:
Eos (Transactions, American Geophysical Union), Abstract U32A-12: Fall Meeting Supplement
 , v.
79
, p.
F58
.
16.
Fisk
M.R.
Storrie-Lombardi
M.C.
Douglas
S.
Popa
R.
McDonald
G.
Di Meo-Savoie
C.
,
2003
,
Evidence of biological activity in Hawaiian subsurface basalts
:
Geochemistry Geophysics Geosystems
 , v.
4
,
1103
,
doi:10.1029/2002GC000387
.
17.
Fisk
M.R.
Popa
R.
Mason
U.O.
Storrie-Lombardi
M.C.
Vicenzi
E.P.
,
2006
,
Iron-magnesium silicate bioweathering on Earth (and Mars?)
:
Astrobiology
 , v.
6
, p.
48
68
,
doi:10.1089/ast.2006.6.48
.
18.
Fliegel
D.
Knowles
E.
Wirth
R.
Templeton
A.
Staudigel
H.
Muehlenbachs
K.
Furnes
H.
,
2012
,
Characterization of alternation textures in Cretaceous oceanic crust (pillow lava) from the N-Atlantic (DSDP Hole 418A) by spatially resolved spectroscopy
:
Geochemica et Cosmochimica Acta
 , v.
96
, p.
80
93
,
doi:10.1016/j.gca.2012.08.026
.
19.
Furnes
H.
Muehlenbachs
K.
,
2003
,
Bioalteration recorded in ophiolitic pillow lavas
, in
Dilek
Y.
Robinson
P.T.
, eds.,
Ophiolites and Earth History
 :
Geological Society of London Special Publication 218
, p.
415
426
.
20.
Furnes
H.
Staudigel
H.
,
1999
,
Biological mediation in ocean crust alteration: How deep is the deep biosphere?
:
Earth and Planetary Science Letters
 , v.
166
, p.
97
103
,
doi:10.1016/S0012-821X(99)00005-9
.
21.
Furnes
H.
Thorseth
I.H.
Tumyr
O.
Torsvik
T.
Fisk
M.R.
,
1996
,
Microbial activity in the alteration of glass from pillow basalts from Hole 896A
, in
Alt
J.J.
Kinoshita
H.
Stokking
L.B.
Michael
P.J.
, eds.,
Proceedings of the Ocean Drilling Program, Scientific Results, volume 148
 :
College Station
,
Texas, Ocean Drilling Program
, p.
191
206
,
doi:10.2973/odp.proc.sr.148.119.1996
.
22.
Furnes
H.
Muehlenbachs
K.
Tumyr
O.
Torsvik
T.
Thorseth
I.H.
,
1999
,
Depth of active bio-alteration in the ocean crust: Costa Rica Rift (Hole 504B)
:
Terra Nova
 , v.
11
, p.
228
233
,
doi:10.1046/j.1365-3121.1999.00251.x
.
23.
Furnes
H.
Staudigel
H.
Thorseth
I.H.
Torsvik
T.
Muehlenbachs
K.
Tumyr
O.
,
2001a
,
Bioalteration of basaltic glass in the oceanic crust
:
Geochemistry Geophysics Geosystems
 , v.
2
,
1049
,
doi:10.1029/2000GC000150
.
24.
Furnes
H.
Muehlenbachs
K.
Tumyr
O.
Torsvik
T.
Xenophontos
C.
,
2001b
,
Biogenic alteration of volcanic glass from the Troodos ophiolite, Cyprus
:
Journal of the Geological Society
 , v.
158
, p.
75
84
,
doi:10.1144/jgs.158.1.75
.
25.
Furnes
H.
Muehlenbachs
K.
Torsvik
T.
Thorseth
I.H.
Tumyr
O.
,
2001c
,
Microbial fractionation of carbon isotopes in altered basaltic glass from the Atlantic Ocean, Lau Basin and Costa Rica Rift
:
Chemical Geology
 , v.
173
, p.
313
330
.
26.
Furnes
H.
Thorseth
I.H.
Torsvik
T.
Muehlenbachs
K.
Staudigel
H.
Tumyr
O.
,
2002
,
Identifying bio-interaction with basaltic glass in oceanic crust and implications for estimating the depth of the oceanic biosphere: A review
, in
Smellie
J.L.
Chapman
M.G.
, eds.,
Volcano-Ice Interaction on Earth and Mars
 :
Geological Society of London Special Publication 202
, p.
407
421
.
27.
Furnes
H.
Banerjee
N.R.
Muehlenbachs
K.
Staudigel
H.
de Wit
M.
,
2004
,
Early life recorded in Archean pillow lavas
:
Science
 , v.
304
, p.
578
581
,
doi:10.1126/science.1095858
.
28.
Furnes
H.
McLoughlin
N.
Muehlenbachs
K.
Banerjee
N.
Staudigel
H.
Dilek
Y.
de Wit
M.
Van Kranendonk
M.
Schiffman
P.
,
2008
,
Oceanic pillow lavas and hyaloclastites as habitats for microbial life through time: A review
, in
Dilek
Y.
Furnes
H.
Muehlenbachs
K.
, eds.,
Links between Geological Processes, Microbial Activities and Evolution of Life
 :
Berlin
,
Springer
, p.
1
68
.
29.
Giovannoni
S.J.
Fisk
M.R.
Mullins
T.D.
Furnes
H.
,
1996
,
Genetic evidence for endolithic microbial life colonizing basaltic glass/seawater interfaces
, in
Alt
J.J.
Kinoshita
H.
Stokking
L.B.
Michael
P.J.
, eds.,
Proceedings of the Ocean Drilling Program, Scientific Results, volume 148
 :
College Station
,
Texas, Ocean Drilling Program
, p.
207
214
,
doi:10.2973/odp.proc.sr.148.151.1996
.
30.
Heberling
C.
Lowell
R.P.
Liu
L.
Fisk
M.R.
,
2010
,
Extent of the microbial biosphere in the oceanic crust
:
Geochemistry Geophysics Geosystems
 , v.
11
,
Q08003
,
doi:10.1029/2009GC002968
.
31.
Ivarsson
M.
Lausmaa
J.
Lindblom
S.
Broman
C.
Holm
N.G.
,
2008
,
Fossilized microorganisms from the Emperor Seamounts
:
Implications for the search for a subsurface fossil record on Earth and Mars
:
Astrobiology
 , v.
8
, p.
1139
1157
,
doi:10.1089/ast.2007.0226
.
32.
Josef
J.A.
,
2006
,
Microbial alteration of the seafloor [M.S. thesis]
 :
Corvallis
,
Oregon State University
,
155
p.
33.
Knowles
E.
Staudigel
H.
McLoughlin
N.
Templeton
A.
,
2011
,
Geochemical characterization of biosignatures in sub-seafloor basalts [abstract]
:
Mineralogical Magazine
 , v.
75
, p.
1206
.
34.
Knowles
E.
Wirth
R.
Templeton
A.
,
2012
,
A comparative analysis of potential biosignatures in basalt glass by FIB-TEM
:
Chemical Geology
 , v.
330–331
, p.
165
175
,
doi:10.1016/j.chemgeo.2012.08.028
.
35.
Kruber
C.
Thorseth
I.H.
Pedersen
R.B.
,
2008
,
Seafloor alteration of basaltic glass: Textures, geochemistry, and endolithic microorganisms
:
Geochemistry Geophysics Geosystems
 , v.
9
,
Q12002
,
doi:10.1029/2008GC002119
.
36.
Lepot
K.
Benzerara
K.
Philippot
P.
,
2011
,
Biogenic versus metamorphic origins of diverse microtubes in 2.7 Gyr old volcanic ashes: Multi-scale investigations
:
Earth and Planetary Science Letters
 , v.
312
, p.
37
47
,
doi:10.1016/j.epsl.2011.10.016
.
37.
Mason
O.U.
Di Meo Savoie
C.
Van Nostrand
J.D.
Zhou
J.Z.
Fisk
M.R.
Giovannoni
S.J.
,
2009
,
Prokaryotic diversity, distribution, and insights into their role in biogeochemical cycling in marine basalts
:
ISME Journal
 , v.
3
, p.
231
242
,
doi:10.1038/ismej.2008.92
.
38.
McLoughlin
N.
Brasier
M.D.
Wacey
D.
Green
O.R.
Perry
R.S.
,
2007
,
On biogenicity criteria for endolithic microborings on early Earth and beyond
:
Astrobiology
 , v.
7
, p.
10
26
,
doi:10.1089/ast.2006.0122
.
39.
McLoughlin
N.
Furnes
H.
Banerjee
N.J.
Muehlenbachs
K.
Staudigel
H.
,
2009
,
Ichnotaxonomy of microbial trace fossils in volcanic glass
:
Journal of the Geological Society
 , v.
166
, p.
159
169
,
doi:10.1144/0016-76492008-049
.
40.
McLoughlin
N.
Staudigel
H.
Furnes
H.
Eickmann
B.
Ivarsson
M.
,
2010
,
Mechanisms of microtunneling in rock substrates: Distinguishing endolithic biosignatures from abiotic microtunnels
:
Geobiology
 , v.
8
, p.
245
255
,
doi:10.1111/j.1472-4669.2010.00243.x
.
41.
McLoughlin
N.
Wacey
D.
Kruber
C.
Kilburn
M.R.
Thorseth
I.H.
Pedersen
R.B.
,
2011
,
A combined TEM and NanoSIMS study of endolithic microfossils in altered seafloor basalt
:
Chemical Geology
 , v.
289
, p.
154
162
,
doi:10.1016/j.chemgeo.2011.07.022
.
42.
Montague
K.E.
Walton
A.W.
Hasiotis
S.T.
,
2010
,
Euendolithic microborings in basalt glass fragments in hyaloclastites: Extending the ichnofabric index to microbioerosion
:
Palaios
 , v.
25
, p.
393
399
,
doi:10.2110/palo.2009.p09-025r
.
43.
Morgenstein
M.
,
1969
,
The composition and development of palagonite in deep-sea sediments from the Atlantic and Pacific Oceans [M.S. thesis]
 :
Syracuse, New York
,
Syracuse University
,
137
pp.
44.
Preston
L.J.
Izawa
M.R.M.
Banerjee
N.R.
,
2011
,
Infrared spectroscopic characterization of organic matter associated with microbial bioalteration textures in basaltic glass
:
Astrobiology
 , v.
11
, p.
585
599
,
doi:10.1089/ast.2010.0604
.
45.
Ryan
W.B.F.
et al
,
2009
,
Global Multi-Resolution Topography synthesis
:
Geochemistry Geophysics Geosystems
 , v.
10
,
Q03014
,
doi:10.1029/2008GC002332
.
46.
Santelli
C.M.
Orcult
B.N.
Banning
E.
Bach
W.
Moyer
C.L.
Sogin
M.L.
Staudigel
H.
Edwards
K.J.
,
2008
,
Abundance and diversity of microbial life in ocean crust
:
Nature
 , v.
453
, p.
653
656
,
doi:10.1038/nature06899
.
47.
Staudigel
H.
Chastain
R.A.
Yayanos
A.
Bourcier
R.
,
1995
,
Biologically mediated dissolution of glass
:
Chemical Geology
 , v.
126
, p.
147
154
,
doi:10.1016/0009-2541(95)00115-X
.
48.
Staudigel
H.
Furnes
H.
Banerjee
N.R.
Dilek
Y.
Muehlenbachs
K.
,
2006
,
Microbes and volcanoes, a tale from oceans, ophiolites, and greenstone belts
:
GSA Today
 , v.
16
, p.
4
10
,
doi: 10.1130/GSAT01610A.1
.
49.
Staudigel
H.
Furnes
H.
McLoughlin
N.
Banerjee
N.
Connell
L.
Templeton
A.
,
2008
,
3.5 billion years of glass bioalteration: Volcanic rocks as a basis for microbial life?
:
Earth-Science Reviews
 , v.
89
, p.
156
176
,
doi:10.1016/j.earscirev.2008.04.005
.
50.
Storrie-Lombardi
M.C.
Fisk
M.R.
,
2004
,
Elemental abundance distributions in suboceanic basalt glass: Evidence of biogenic alteration
:
Geochemistry Geophysics Geosystems
 , v.
5
,
Q10005
,
doi:10.1029/2004GC000755
.
51.
Stronick
N.A.
Schmincke
H.U.
,
2002
,
Palagonite: A review
:
International Journal of Earth Sciences
 , v.
91
, p.
680
697
.
52.
Thorseth
I.H.
Furnes
H.
Meldal
M.
,
1992
,
The importance of microbiological activity in the alteration of natural basaltic glass
:
Geochimica et Cosmochimica Acta
 , v.
56
, p.
845
850
.
53.
Thorseth
I.H.
Furnes
H.
Tumyr
O.
,
1995
,
Chemical and textural effects of bacterial activity on basaltic glass: An experimental approach
:
Chemical Geology
 , v.
119
, p.
139
160
,
doi:10.1016/0009-2541(94)00098-S
.
54.
Thorseth
I.H.
Torsvik
T.
Torsvik
V.
Daae
F.L.
Pedersen
R.B
,
and Keldysh-98 Scientific Party
,
2001
,
Diversity of life in ocean floor basalt
:
Earth and Planetary Science Letters
 , v.
194
, p.
31
37
.
55.
Thorseth
I.H.
Pedersen
R.B.
Christie
D.M.
,
2003
,
Microbial alteration of 0–30-Ma seafloor and sub-seafloor basaltic glasses from the Australian Antarctic Discordance
:
Earth and Planetary Science Letters
 , v.
215
, p.
237
247
,
doi:10.1016/S0012-821X(03)00427-8
.
56.
Torsvik
T.
Furnes
H.
Muehlenbachs
K.
Thorseth
I.H.
Tumyr
O.
,
1998
,
Evidence for microbial activity at the glass alteration interface in oceanic basalts
:
Earth and Planetary Science Letters
 , v.
162
, p.
165
176
,
doi:10.1016/S0012-821X(98)00164-2
.
57.
Walton
A.W.
,
2008
,
Microtubules in basalt glass from Hawaii Scientific Drilling Project #2 phase 1 core and Hilina slope, Hawaii: Evidence of the occurrence and behavior of endolithic microorganisms
:
Geobiology
 , v.
6
, p.
351
364
,
doi:10.1111/j.1472-4669.2008.00149.x
.
58.
Walton
A.W.
Schiffman
P.
,
2003
,
Alteration of hyaloclastites in the HSDP 2 phase 1 drillcore—1. Description and paragenesis
:
Geochemistry, Geophysics, Geosystems
 , v.
4
,
doi: 10.1029/2002GC000368
.