Ignimbrite Deposits - Textures and Microscopic Features

1. Ignimbrite Deposits - Texturesand Microscopic Features Source for most of the material presented here: http://www.geology.sdsu.edu/how_volcanoes_work /Thumblinks/ignimbrite_page.html

2. Ignimbrite Deposits Ignimbrites are pumice-dominated pyroclastic flow deposits with subordinate ash. There are many historic examples, most of which are restricted to valleys emanating from summit craters. One such deposit from the 1980 eruption of Mt. St. Helens (below left) contains abundant pumice blocks at its terminus. However, there are no historic examples of the voluminous ignimbrite sheetflows associated with caldera formation. These extensive deposits can cover many thousands of square kilometers. They often appear as coherent, well-compacted, often partially welded, layers that in some cases resemble lava flows, as demonstrated by the Miocene Rio Loa sheetflows of northern Chile (below right). Small ignimbrite deposit terminus MSH, 1980 Miocene Rio Loa sheetflow, Northen Chile

3. Ignimbrite Rock Textures Ignimbrites are typically characterized by fist-sized pumice fragments floating in a finer grained matrix (below left). Many ignimbrites, however, are still hot when they are emplaced so that the pumice and ash fragments are still plastic and malleable. Thick, hot ignimbrites will often collapse under their own weight, thus fusing the fragments together to generate a welded flow. In such cases (below right) the pumice fragments are compacted into dark, glassy pancake shapes, called fiamme. A welded ignimbrite containing fiamme is said to have a eutaxitic texture. Unwelded ignimbrite with pumice fragments Welded ignimbrite with collapsed pumice (fiamme)

4. Non-welded Microscopic Features Nonwelded ignimbrites are distinct from their welded counterparts in both outcrop appearance and microscopic texture. Glass shards, derived from the fragmentation of the vitric bubble walls of pumice vesicles, are well-preserved. They occur as slender branches having platy to cuspate forms, many of which display triple junctions marking the site of the coalesced bubble walls. In many cases, entire vesicles are well-preserved. Although nonwelded, the glass shards commonly display some degree of compaction, marked by the a slight aligned and/or flattening of the vitric forms. Rattlesnake tuff from central Oregon, displaying slightly flattened shards with unbroken glass bubbles, now in oval outline. Nonwelded tuff from Sumatra with very slight compaction of glass shards. Note the unusually massive shard center right.

5. Welded Microscopic Textures Compaction and welding is evident in the deformation of glass shards and pumice fragments, as demonstrated by: the collapse of Y-shaped shards and bubble walls, the alignment of elongate crystal and lithic fragments, the folding of shards around lithic and crystal fragments, and the collapse of pumice fragments into glassy lenticular masses called fiamme. The degree of welding can be highly variable, often marked by distinctive color changes reflecting variable oxidation states of iron. Under extreme welding, the welded mass has an obsidian-like appearance, often associated with ghost-like impressions of the flattened shards surrounding the crystal and lithic fragments. Welded tuff from Valles, NM displaying well-developed parallel alignment of shards and elongate crystal fragments. Fine-grained, glassy welded tuff showing extreme compaction and molding against crystal fragments. Welded tuff from SE Idaho. Note marked compression of the shards, but good retension of the shard structures.

6. Lithic and Crystal-rich Tuffs Pumice fragments are much more common in ignimbrites than are lithic and crystal fragments. Lithic clasts are generally cognate or accidental fragments; i.e., not derived from the erupting magma, but rather from wall-rock within, or below, the edifice of the volcano. Magma-derived crystal fragments are common, particularly in the main body of the pyroclastic flow where they become concentrated by the winnowing out of vitric ash from the flow proper, and into the overlying ash cloud. This process, known as elutriation, effectively concentrates the denser crystal fragments into the main body of the flow, relative to the glass shards. Although crystal fragmentation can be partly attributed to percussive interactions during the eruption, recent data suggests that a more likely scenario involves the internal bursting of individual crystals as they ascend through the magma column. Crystals commonly contain small fluid inclusions, the decompression of which will result in rapid gas expansion, and explosion of the crystals accordingly. Crystal-rich welded tuff from the 74,000 year-old Tobaeruption in Sumatra, displaying compressed glass shards molded around the crystal fragments of quartz, feldspar, and biotite. A lithic fragment of older welded tuff, displaying marked compaction and distortion of shards, residing in a younger ignimbrite that is poorly welded.

7. Devitrification and Axiolitic Textures Devitrification is a post-depositional process resulting in the crystallization of microlites along the boundaries of the glass shards or within glassy masses. The mineral compositions produced are mainly cristobalite and alkali feldspar. This process is more common in densely welded ignimbrites, where individual glass shards can often be identified by devitrified crystals radiating from the shard walls toward the inner part of the shard to produce axiolitic texture. This term is derived from the axis of the shard, which is typically outlined by the inward-growing microlites. If welding occurs before devitrification begins, the devitrification process may extend across individual shards boundaries, often obliterating shard structures Highly magnified view (note scale) shows axiolitic texture of feldspar and cristobalite along the walls of a large shard representing the walls of several bubbles. The narrow, white margins on these glass shards mark incipient devitrification. The interior of the shards remain glassy.

8. Spherulites Devitrification may occur around scattered nuclei to form spherulites, which are delineated by radiating crystals of acicular cristobalite and feldpar. These spherical aggregates are common features in both rhyolitic lavas and felsic ignimbrites. In the latter, their sub-solidus growth typically results in severe destruction of original tuff structures The radial aggregates of cristobalite and feldspar are well displayed in this very large spherulite. Note also the growth of secondary minerals generating a plumose structure along the spherulite's outer margin. Spherulites from a welded tuff at Valles, NM. The concentric banding in the spherulites is due to variations in grain size of the aggregates of cristobalite and feldspar.