Skolithos

The structure of the trace fossil is cylindrical and elongated in shape, usually at a perpendicular angle to the surface where it has been deposited. They can reach lengths of up to about 35 cm (14 in)[6] and diameters of up to about 5 cm (2.0 in).[6] The vertical burrows are composed of the same mineralogy as its surrounding matrix which allow it to deform homogenously with the parent rock. Variations in observed Skolithos structures include burrow curvature, angle to the plane of deposition, and size of the fossil’s aperture.[11] Funnel-shaped apertures of Skolithos reflect the filter- and suspension-feeding habits of burrowing genera. The high intensity of bioturbation of these organisms indicate the shallow water paleoenvironment in which the Skolithos burrows formed shortly after the deposition of the bed.[11]

Unstrained Skolithos structures are normal to the plane of the bed.[11] In zones where tectonic deformation is intense, such as thrust zones, the deformed Skolithos burrow can be used to evaluate the local strain on the region.[11] This technique is performed by comparing the angle between the specimen and the bedding surface, with the original 90^o geometric relationship. Since the trace fossil shares similar material properties to the surrounding matrix, they are inferred to deform by the same mechanism.[11] This technique can be applied in areas where other strain markers may have been destroyed by tectonic activity or cataclastic flow.[11]

Unit strain ɛ can also be defined using the elongation of the structure:

${\displaystyle \varepsilon =(\ell -\ell \circ )\div \ell \circ }$

where

•     ɛ is the unit strain due to elongation

•      l  is the deformed length of the structure

•     l_o is the initial length of the structure

The structure length and orientation may be influenced by the directional behaviour of the burrowing organism, therefore observing the widths of the burrow may provide a more precise strain estimation.[12]

The famous "Pipe Rock" of northwest Scotland is a well-known example of Skolithos. The 'pipes' that give the rock its name are closely packed straight Skolithos tubes that were presumably made by a worm-like organism.[13] The Pipe Rock can be found in the Stack of Glencoul region beneath the Moine Thrust Belt, Scotland.[14]  This area which has a history of thrust faulting activity is a highly deformed mylonite zone with a quartzite protolith where many structural geologists have used microstructures such as the Skolithos borings in conjunction with other strain markers, such as quartz vein recrystallization, in order to approximate strain in the region.[14] Using three-dimensional analysis of the strain markers, geologists inferred flattening of the region parallel to the thrust direction, stretching along the vertical strain direction and shortening perpendicular to the foliation of the lithology.[14] The deformation history of the mylonite belt which is characterized by large translation of thrust faults, can be deduced from the apparent clockwise rotation of these structures. Assuming simple shear, the westward displacement of the 800 m thick Moine Thurst mylonites at Loch Eriboll where the average shear strain determined using the trace fossils is approximately 10, was calculated to be about 8 km.[11]

Assumptions regarding the undeformed burrow and its geometric relationship cannot directly be determined, and only estimated.[15] While it is common for Skolithos burrows to form normal to the deposition plane, this is not always true, in which case, the ideal, undeformed state can no longer be used as a reference orientation.[15] Shallow depositional sediments are also susceptible to damage by erosion and tectonic stress forces, which can influence average measurements and geometric orientations.[7] Since the rheological properties between the structure and the host rock are usually very similar, observations of the fossils are conducted with the assumption that they have deformed homogeneously, where the deformation forces are distributed evenly along the entire deformation zone.[12] This is directly contradicted by the presence of folding and varying elongation measurements of the fossil at different locations in the same deformation zone. Deformation mechanisms are difficult to distinguish using this strain marker, as the thinning and flattening of the highly deformed rocks where they are found, cannot necessarily be attributed to pure shear since the planes may have simply rotated near parallel to the shear plane.[15] It is therefore only possible to make accurate strain determinations of the host rock provided the correct assumption of the deformation mechanism and original measurements.