A new book has recently been published: Hannu Ahokas: Previously unidentified meteorite impacts in South Finland. In Finnish with English abstract – Click HERE for more information.
A short appreciation: Dr. Andrew Glikson – a stroke of luck for meteorite impact research Continue reading “A stroke of luck for meteorite impact research”
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Meteorite impact-induced tsunami in Lake Chiemsee, Bavaria (southeast Germany)
A new geological outcrop exposing an impressive cross-bedded diamictite substantiates the emergence of a giant tsunami in the Chiemgau Holocene impact event. Click the article!
“The Steinheim impact crater (SW Germany) – where are the ejecta?” – title of an extended paper by Buchner and Schmieder to be published 2015 in Icarus.]
At the this year’s 77th annual meeting of the Meteoritical Society Buchner & Schmieder (2014) have presented an abstract article about the apparently missing impact ejecta of the Steinheim impact crater (Steinheim Basin). Starting point is the statement that beyond of the impact basin not any ejecta are known in obvious contrast to the distinct ejecta curtain of the same-aged, however much larger Ries impact crater.
On the one hand, a primary effect – practically no ejecta were produced upon impact – is discussed, and on the other hand the possibility of a complete erosion of originally existing ejecta is considered. Because of the today’s distribution of the post-impact Miocene sediments around the Steinheim Basin the second possibility is thought to be little likely, and instead a primary effect is favored.
The postulated primary absence of excavation and ejection upon the Steinheim Basin formation is related by the authors with a paper written by Housen & Holsapple (2012; similar papers of these authors also earlier). In this article ejection mechanisms for craters on strongly porous bodies in the Solar System are discussed with the result that on those bodies big craters do not feature impact ejecta in contrast to less porous bodies. The idea is substantiated by laboratory experiments and scaling laws which are obviously compatible with observations of e.g., the Mathilde asteroid (≈ 50% porosity) and the Saturn moon Hyperion (≈ 40% porosity) where the big craters don’t possess significant impact ejecta, but smaller craters however. According to that (Fig. 6 in Housen & Holsapple 2012), a very rough threshold is given by craters with diameters 20 – 50 km and with target body porosities of > 40% assuming that gravity on the highly porous body is not an issue. In the end and a bit simplifying, the reason for a prevention of ejection is the extremely porous material that in the excavation stage and with the development of the transient crater (see here: … understanding the impact cratering process – a simple approach) is preferentially compressed downwards and towards the sidewalls. Hence, percentally much less rock material can find its way outwards in large craters in contrast to smaller ones.
This model is applied by Buchner & Schmieder (2014) to explain the seemingly missing impact ejecta around the Steinheim Basin.
1 The crater size of the Steinheim Basin
Commonly, a diameter of 3.8 km (also 3.7 km) is ascribed to the Steinheim Basin. A gravity survey and a detailed morphological analysis reveals however that this impact structure probably is much larger. Thus, a diameter of 6-7 km seems to be realistic as is shown in the paper by Ernstson (1984: A gravity-derived model for the Steinheim impact structure. International J. Earth Sci. , 73/2, 483-498) and is evident in Figs. 1, 4 and Fig. 5.
Fig. 1. Profile of Steinheim Basin averaged topography (from Ernstson 1984). Upper profile: topography from 32 averaged radial profiles. Bottom profile: topography from 16 averaged southern profiles (to the left) and 16 averaged northern profiles (to the right). Dashed line: left profile (south) mirrored at the zero axis and 20 m shifted. The 3.7 km bar (red) represents the mean diameter of the crater as it is kept used in the literature obviously not corresponding to reality.
Although this article has been printed in an internationally renowned journal, even in more recent papers on impact modeling of the Steinheim Basin (Stöffler et al. 2002, Ivanov & Stöffler 2005) the small diameter is further on used making the results of these crater models rather suspect (see a respective discussion HERE). Such is the case with the Buchner & Schmieder (2014) article who use a 3.8 km diameter but withhold and do not refer to the alternative of the significantly larger crater. Like with Stöffler and Ivanov this must be called bad scientific style (omitting quotation) and dubious scientific working using wrong preconditions as potential starting point.
2 Possible erosion of the ejecta
— Because of the extended forests (Fig. 2) a reliable mapping in the surroundings of the Steinheim Basin is problematic. Buchner & Schmieder don’t write what kind of mapping, to what extent and on what a scale was performed.
Fig. 2. The Steinheim Basin within large forested areas. Red: conventional diameter (3.7 km, resp. 3.8 km); green: diameter according to Ernstson (1984). Google Earth.
— Paleogene and Miocene deposits that are quoted by Buchner & Schmieder to show that ejecta would probably have survived are not found in the geological maps (Kranz 1923, Gediga 1984, Reiff 2004).
— Loamy layers with silifications widespread to be mapped on the Alb plateau and also bordering the Steinheim Basin (see geologic map) may well be relics of weathered Malmian ejected limestones.
— The today’s morphology in the surroundings of the Steinheim Basin featuring deeply cut dry valleys (Fig. 3) prove significant erosion.
Fig. 3. Relief map of the Steinheim Basin. Scale bar 3 km. (Source: TOP25 Baden Württemberg).
— The erosion of an originally existing rim wall is explicitly mentioned in Reiff (2002, Fig. 84). In the image sequence 1 – 8 of the basin development phase 2 shows the crater immediately after the impact having a distinct rim wall which by erosion becomes smaller and smaller. For phase 7 – Pliocene – we read: “The rim wall is leveled”. This has been written by W. Reiff, probably the best expert for the more recent geologic research in the Steinheim Basin. I.e., independently of the true, larger or smaller crater size Reiff assumes a significant post-impact erosion (phase 6: tectonic uplift of the Alb mountains) that let the rim wall with the biggest ejecta thickness disappear completely. Also the more distant ejecta with strongly decreasing thickness should not have escaped this erosion. This is not circular reasoning: Reiff does not postulate erosion because of the lacking rim wall (according to Buchner & Schmieder a primary feature) but instead he refers to the post-impact Earth history in the region implying significant erosion also in the Ries impact structure and its surroundings.
— Independently of the post-impact erosion history and the disappearance of the ejecta postulated by Reiff, the morphological analysis addressed above under 1 (Ernstson 1984) shows that a circular rampart of the significantly larger crater seems to exist still today.
Fig. 4. Profiles of averaged topography taken from the Steinheim impact basin (from Ernstson 1984). Explanation see Fig. 1)
Conclusions on 2: The assumption that from the beginning a ejecta curtain did not exist has not any convincing base; Buchner & Schmieder don’t supply the reader with scientific proof. Ejecta and/or their weathering relics may exist still today or/and underwent erosion.
3 The Housen & Holsapple (2012) hypothesis
— The hypothesis differentiates between small and big craters on bodies in the Solar System, where according to a high porosity ejecta curtains do develop or not, respectively. In this sense Steinheim is a small crater (be it the old 3.8 km, be it the 6-7 km postulated by Ernstson (1984)); the threshold is 20 – 50 km after Housen & Holsapple.
— The porosity: Housen & Holsapple postulate a porosity of more than ≈40% in order the process of ejecta formation is suppressed. Buchner & Schmieder quote porosities between ≈21% and ≈44% for the target rocks of the Steinheim Basin and reason these figures with an intense karstification of the Malmian limestones and dolomites. For the whole target they even prefer the larger value of ≈44% porosity. It’s a mystery where these unbelievably high porosity values with a yet certain precision (21, 44) for the sedimentary sequence of the Swabian Alb during the Upper Miocene some 15 Mill years ago originate from. A reference does not exist.
— Investigations especially in more recent deep geothermal boreholes revealed intergranular porosities of Malmian limestones and dolomites near 3.5 %, partly < 3%. Assuming a bulk porosity, karst cavities included, of up to ≈44 % this means that one third or more of the rock volume must be cavernous (open joints, karst cavities). With regard to the innumerable large quarries cut into the Malmian of the Alb it remains enigmatic how Buchner & Schmieder arrived at these porosities.
— It is possibly to convert porosities into densities using, e.g., plausible 2.6 g/cm³ as matrix density for the Malmian limestones. Then, a porosity of 44% is related with a Malmian bulk density of about 1.9 g/cm³ if the whole pore volume is filled with water. Applied to about 150 m dry rocks above the on-site preflooder the density reduces to only c. 1.45 g/cm³. The latter is a little more than the density of the 50 km-diameter Mathilde asteroid (1.3 g/cm³) which is considered a rubble pile body. And exactly for that reason Mathilde was used by Housen & Holsapple to test their models and scaling laws (see above).
But the Steinheim Basin underground? Every geophysicist’s hair would stand on end when, conducting a gravity survey in the Alb mountains, he/she should do his/her mass correction using a reduction density of 1.45 g/cm³ with the consequence that his/her gravity map would practically be the mirror image of topography.
Moreover, given the Housen & Holsapple model is applicable to the Steinheim crater, then after the impact the basin underground density should have increased compared with the surroundings, due to the strong shock compression downwards and sidewards squeezing the karst fissures and cavities. Hence, a gravity survey today should measure a positive gravity anomaly over the crater. This is evidently not the case as a reasonable density model proves (Fig. 5).
Fig. 5. Results of gravity modeling for the Steinheim impact basin. Densities are g/cm³. (from Ernstson 1984).
Conclusions on 3: The starting point of Buchner & Schmieder to apply the Housen & Holsapple model to the Steinheim impact crater is far from any geologic and geophysical reality und thus in the end leads to nothing.
In principle it is reasonable and in science the appropriate line to make observations, carry out experiments and analyses before (!) calculations and computer modeling are considered and performed to support explanatory models or to disprove them. However, more recently it can be stated more and more frequently that the cart is put before the horse, which means the computer models are put at the very beginning and the observation (in geology the field work) has to be kindly adapted.
Seemingly Buchner & Schmieder chose the correct way: In the first place the observation of the apparently non-existing ejecta at the Steinheim Basin and then the theoretical model that should explain the observation. However, in the end they were thinking nothing else but the model in order to make the observations fit the model: disregarding the literature of most experienced geologists (e.g., Reiff 2002), ignoring important articles about the Steinheim impact crater (Ernstson 1984), not involving specifications of the theoretical model (contrasting big and small craters with distinct differences), disregarding existing geophysical data (the negative gravity anomaly), and finally – scientifically especially inexcusable – to present parameters (absolutely unrealistic porosities for the Steinheim underground rocks) without any source.
Once again, Buchner & Schmieder demonstrate that by hook or by crook they want to give the Steinheim Basin a particular importance that does not exist, and we mention their paper on the Steinheim “suevite” that can be shown is a pure fiction. (see a comment on that article)
Buchner, E. & Schmieder, M. (2010): Steinheim suevite – A first report of melt-bearing impactites from the Steinheim Basin (SW Germany). -Meteoritics & Planetary Science, 45, 1093-1107. (comment on the article)
Buchner, E. & Schmieder, M. 2014): The Steinheim impact crater (Germany) – where is the ejecta blanket? – 77th Annual Meteoritical Society Meeting, 5168.pdf.
Ernstson, K., Mayer, W., Neumair, A., Rappenglück, B., Rappenglück, M.A., Sudhaus, D. and Zeller, K.W. (2010): The Chiemgau crater strewn field: evidence of a Holocene large impact in southeast Bavaria, Germany. – Journal of Siberian Federal University, Engineering & Technology, 1 (2010 3) 72-103.
Gediga, P. (1984): Geologische Karte von Steinheim 1 : 10 000, Diploma thesis Universität Essen.
Housen, K.R. & Holsapple, K.A. (2012): Craters without ejecta. – Icarus, 219, 297-306.
Ivanov, B.A. & Stöffler, D. (2005): The Steinheim impact crater, Germany: Modeling of a complex crater with central uplift. -Lunar and Planetary Science XXXVI (2005), 1443.pdf.
Reiff, W. (2002): Das Steinheimer Becken, Darstellung der geologischen Zusammenhänge (Teil I), in: Heizmann, E.P.J. & Reiff, W.: Der Steinheimer Meteorkrater (Gemeinde Steinheim, Hg.), Pfeil-Verlag, München, 160 S.
Stöffler, D., Artemieva, N.A. and Pierazzo, E. (2002): Modeling the Ries-Steinheim impact event and the formation of the moldavite strewn field. -Lunar and Planetary Science XXXIII (2002) 1871.pdf.
From a communication with the “OBSERVATOIRE de L’ASTROBLÈME de Charlevoix” (Prof. Jean-Michel Gastonguay, academic advisor) the idea arose to present here on our website the Charlevoix impact structure and some of its prominent geologic inventory as well as a hint to the observatory with its museum and geologic route. Continue reading “Focusing on the Charlevoix (Quebec, Canada) impact structure”
Dear visitor of our website,
in the last years we have observed a permanently increasing number of page views, and statistics counted more than 9,000 (nine thousand) just for the last four weeks and solely for the English version. And statistics also said that a very high percentage of the views have accounted for the page on “Understanding the Impact Cratering Process: a Simple Approach“. This was the initial spark to introduce a new category “Impact educational” that may be clicked in the top menu from now on. Moreover, we got clear about the fact that many of our scientific contributions – to say it geologically – have sedimented and buried to deeper and deeper layers, and many an article may have become subject even to subduction and oblivion – despite all search engines. Hence, our new “Impact educational” category especially intends to excavate older impact literature of particular importance and interest, and specific subject areas earlier discussed on our homepage will step by step be brought into a new context also integrating new research aspects and publications. Make a test and read about meteorite impact spallation, including a chapter on dynamic spallation vs. tectonic stress – fractured pebbles as a stress indicator!
Meteorite Impact spallation: from mega- to micro-scale
Content. – 1 Introduction 2 Meteorite impact spallation – geological implications 2.1 Spallation and spall plates – Spall plates in experimental hypervelocity impact cratering 2.2 Spallation and structural features 2.3 Spallation on a geologic mesoscopic scale 2.4 Tectonic stress vs. dynamic spallation – fractured pebbles as a stress indicator 3 Meteorite impact spallation – mineralogical implications – Literature
The process of spallation in solids (not to be confused with nuclear spallation) is well understood in fracture mechanics. Spallation takes place when a compressive pulse impinges on a free surface or boundary of material with reduced impedance (= the product of density and sound velocity) where it is reflected as a rarefaction pulse. The reflected tensile stress may exceed the tensile strength of the material leading to tensile fractures and to detachment of a spall or series of spalls (Fig. 1).
Fig. 1. Sketch of spallation in solids by dynamic deformation.
Since the tensile strength of a matter is in general much lower than the compressive strength, spallation frequently causes the main mechanical damage and, hence, is of some practical importance. In the early years of nuclear plant construction, e.g., when catastrophic damage in an air crash was for the first time discussed, model calculations from fracture mechanics showed that tensile stresses from spallation were much more dangerous than the immediate impact. In a recent experimental technique Laser spallation uses a high energy pulsed laser to detach thin films from the substrate by the reflected tensile wave. More generally, the term spallation is also used, e.g., in quarry blasting and drilling of very hard rocks in boreholes (thermal spallation drilling) where spall detachment is induced by various superposition of internal compressive and tensile stresses, which is not of further interest here.
The dramatic effect of spallation can be shown by relatively simple experiments in combination with a high-speed camera, which is demonstrated here (Figs. 2, 3, and the video) with regard to impact shock spallation to be treated below. In these experiments 3 cm-diameter glass cylinders, 10 cm und 20 cm long, were impacted by a 6 mm-diameter aluminum sphere at an impact velocity of ≈ 1250 m/s. For details of the experimental setting see http://www.impact-structures.com/understanding-the-impact-cratering-process-a-simple-approach/making-impacts-experimental-hypervelocity-crater-generation/
Fig. 2. Spallation experiment, shot 3, on a glass cylinder. Sequence of freeze images from a video taken with a high-speed camera, milliseconds (ms) after impact. Note the heavy damage in view of the tiny projectile of only 0.3 g mass. – Click on the image for a full-size pdf. Click the full video!
Fig. 3. Spallation experiment, shot 4, on a glass cylinder. Sequence of freeze images from a video (to be clicked here) taken with a high-speed camera, milliseconds (ms) after impact. Note the heavy spallation damage by the tiny 0.3 g projectile, but also the broad segment in between that remained completely untouched. The light flash regularly emitted in the very first moment from the point of impact (also see Fig. 2) has remained unsettled. – Click on the image for a full-size pdf.
The spallation experiments have been performed in cooperation with Werner Mehl who is a top expert of professional short-term measuring technique, high-speed photography and triggering systems.
Different from the subparallel spallation fractures in the glass cylindrical bars resulting from the reflection at the plane end, spallation in more complex bodies and – with regard to spallation in geologic objects to be discussed below – may feature quite specific tensile fractures. For geometrical reasons the reflected tensile wave front roughly mirrors the geometry of the free surface which is especially striking in spherically shaped objects (Fig. 4) and will further on become evident in images of spallation fractures in rocks and minerals.
Fig. 4. Open spallation fracture in a quartzite cobble a s a mirror of the shock-reflecting surface (left), and an experimentally produced lens-shaped spall in a quartz sphere.
2 Meteorite impact spallation – geological implications
2.1 Spallation and spall plates
In impact research, spallation as a highly important geologic process has been considered only very hesitantly, right up to not at all. In the book “Traces of Catastrophe – A handbook of Shock-Metamorphic Effects in Terrestrial Meteorite Impact structures” (French 1998) the term “spallation” does not exist, and in the much more recent article “The convincing identification of terrestrial meteorite impact structures: What works, what doesn’t, and why” (French & Koeberl 2010) a search for “spallation” is futile. [A comment paper on this French & Koeberl article may be clicked HERE.]
On a megascale, spallation in impact cratering was, obviously for the first time, introduced by Melosh (1989) with the concept of spall plates. Spall plates form in the early phase of impact excavation in the superficial interference zone where the expanding compressive shock front superimposes with the tensile rarefaction waves starting from reflection at the free surface of the impacted target. From this, large rock bodies, the spall plates, are expelled with enormous velocities at the same time carrying only slight shock intensities.
For a long time spallation and spall plates remained a more theoretical idea and concept, in particular among geologists because of the not so simple mathematical background, but initiated also a few experimental approaches (e.g., Polanskey 1989, Polanskey & Ahrens 1990).
Only in recent years, but rarely, spall plates have entered impact literature being considered in connection with impact excavation and impact ejecta (e.g., Buchner et al. 2007, Osinski et al. 2013), although much earlier the spall plate theory could have explained many a geologic observation. In the famous Ries impact structure (Nördlinger Ries crater), e.g., the Bunte breccia sedimentary ejecta from the upper part of the mixed target are standing out due to their very low shock metamorphism. This holds true also for shatter cone development. Even up to now not any shatter cones that are formed at shock pressure exceeding roughly 2 GPa have been observed to occur in the sedimentary rocks, although the thick fine-grained Malmian limestones from the uppermost target would have made an excellent material for shatter cones. Together with the in part enormous range of excavated big megablocks (see HERE) the spall plate concept seems well applicable to the Ries crater. As for the big ejected megablocks displaced over 15 km or more from the Ries crater a nice counterpart has been found to exist in connection with the ≈ 40 km-diameter Mid-Tertiary Azuara impact structure in Spain where the spall plate concept can be applied as well (Claudin & Ernstson 2012).
Spall plates in experimental hypervelocity impact cratering
Interestingly, the formation and expulsion of spall plates can nicely be observed also in experimental hypervelocity impact cratering. A respective report can be found by clicking HERE, and a foretaste is seen on clicking on the image (Fig. 5).
The effect of spall plate highest-velocity ejection to be observed in an experiment as a matter of fact was in particular crucial to understand a geologic observation of enigmatic “erratic” large blocks in the field of the Chiemgau impact meteorite crater strewn field (Ernstson et al. 2010) – more HERE and by clicking on the label.
Click on the label and copy the impact experiment video as a file to a folder on your disk.
2.2 Spallation and structural features
On a somewhat smaller scale impact spallation must be considered a significant geologic process in impact cratering considering rock deformation and structural features in and around impact structures. Originally, compressive deformation by the propagating shock waves were considered the main acting forces, but the idea that spallation and related strong tension by rarefaction waves are the dominant component of damage and deformation is little by little gaining acceptance in impact research. This is insofar important as geologists are often rather puzzled being confronted with complex tensile features not listed in their textbooks. As early as some 20 years ago the authors of this website have repeatedly pointed to such a tectonic style in the Azuara impact structure enigmatic for “normal” geologists frequently, and more than ever, raising opposition against impact as such.
2.3 Spallation on a geologic mesoscopic scale
Spallation works best if the compressive (shock) pulse impinges on a rock boundary of strong impedance change (see chapter 1) or in particular on a free surface. Hence, spallation is a prominent feature to be observed in shocked conglomerates when competent cobbles are embedded in a soft matrix. Exemplarily this process is exposed and can nicely be observed in the widespread Buntsandstein quartzitic conglomerates that were in part strongly shocked in the big Azuara/Rubielos de la Cérida impact event in Spain.
Fig. 7. On clicking on the image with the shocked cobble and open spallation fractures a lengthy report on the many aspects of the deformations of the Spanish shocked conglomerates with a special focus on spallation can be read.
Geologists have never understood these deformations, and since decades and without a closer look at them they have always interpreted the clear spallation features as having originated from tectonic load and pressure dissolution. Even impact researchers not exactly unknown like Bevan M. French and Christian Koeberl when mentioning the cobble deformations of the Spanish Buntsandstein conglomerates (French and Koeberl 2010) in connection with the publication of Ernstson et al. (2001) in the GEOLOGY journal show that they have obviously not understood spallation and the complex physical process related with shock propagation in spherically shaped cobbles.
More evidence of impact spallation in the Spanish impact regions is found with cobbles and boulders from the prominent impact ejecta (Pelarda Fm.) (Fig. 8).
Fig. 8. On clicking on the image showing a prominent spallation fracture plane the concave surface of which is mirroring the original boulder convex shape, more can be read about spallation in the Spanish impact ejecta.
Also in the Ries impact crater clear spallation features are abundant but have never been recognized by geologists as such. For a more detailed discussion in a bit longer paper click on the image in Fig. 9 showing spallation fractures in Ries and Azuara crater shocked cobbles and in the famous Ries shocked belemnites.
Fig. 9. To the left: very similar spallation fractures in cobbles from the Ries and Azuara impact structures. To the right: The Ries belemnites have always been considered to have been deformed by shock without however specifying the mode of deformation. Spallation to have produced the abundant open, tensile fractures is a reasonable explanation. Click on the image to read the article.
Moreover, impressive spallation fractures in shocked cobbles have been described and published for the Holocene Chiemgau impact event in southeastern Germany (Ernstson et al. 2010), and a special article has been addressed to their occurrence and formation: Click the image in Fig. 10 to read and see!
Fig. 10. Prominent open spallation (tensile) fracture in a limestone cobble from the Chiemgau impact region.The process is nicely documented by the observation that the running fractures have come to standstill midway through the cobble. In case they had continued running, the cobble would have been fractionized to pieces, and nothing of note would have remained. For a better understanding we add that fractures always begin at a definite point within the material propagating from there with a certain fracture velocity which may change during propagation and may even become zero. Then the fracture stops unless it is again fed with energy and continues running.
In the Chiemgau impact region spallation of Quaternary cobbles is often accompanied by distinct open (tensile) fractures that are completely filled with glass quenched from impact melt (Fig. 11).
Fig. 11. A shocked cobble from the Chiemgau impact region with prominent open spallation fractures filled with glass. The perfect fitting of the zig-zag fracture planes proves the tensile character of deformation without any shearing.
Comparable to the Chiemgau finds, strongly shocked quartzite cobbles exhibiting glass-filled tensile fractures as the obvious result of spallation (Fig. 12) have been described only recently also for the newly established Nalbach impact event in the Saarland region of western Germany (Müller 2011, Müller 2012, Berger 2014).
Fig. 12. Nalbach impact: glass-filled tensile fractures in quartzitic cobbles; sawed surfaces. Note the fissures often narrowing from the surface which document the direction of fracture propagation and the injection of the melt or the rock vapor.
2.4 Tectonic stress vs. dynamic spallation – fractured pebbles as a stress indicator
Geologists are commonly accustomed to gradual processes and very slow deformation of rocks which among other things is the reason behind their frequently articulated reluctance to meteorite impact phenomena manifoldly addressed here on our website. This in particular may explain that they tend to interpret unusual deformation features they have observed in nature by intricate models of slow tectonic movements and/or complex stress – strain relations. Exemplarily, much opposition has been roused to the impressive spallation features exhibited by the Buntsandstein quartzite conglomerates affected by the impact shock of the Spanish Azuara and Rubielos de la Cérida impact structures. Not only geologists having worked in the region of the large Spanish impact event like Spanish regional geologist or the geologists from Amsterdam around Jan Smit, who evidently overlooked the exceptional situation or did not understand the peculiar deformations, but also remote geologists like Shapman, Evans & McHone (2004) never having put their foot on the Spanish terrain prefer to discredit the dynamic mode of impact spallation (A comment on their paper of rather bad science can be clicked HERE) in favor of a tectonic explanation. And we mention (and discuss HERE) also French & Koeberl (2010) who have evidently not understood the spallation features in the Spanish shocked conglomerates.
In contrast, good science is an earlier article on fractured pebbles (Eidelman & Reches 1992) that is a fine clue for discussing quasi-static and dynamic fracturing of rocks. In that article Eidelman & Reches report on two outcrops in Israel and the USA where they observed unusual fracturing of competent cobbles in a soft matrix forming thick conglomerates. The main features of this subparallel tensile fracturing can be seen in Fig. 13, and the authors were surprised to find these systematic tensile joints since such poorly cemented conglomerates tend to deform by shear and displacement.
Fig. 13. Map of fractured pebbles from the Arava, Israel, outcrop. Modified from Eidelman & Reches (1992).
In a theoretical model of stress – strain relationship they come to the conclusion that intrapebble tension may develop due to the amplification of the stresses inside a competent pebble within a soft matrix, even under compressive tectonic stresses. Hence, the authors suggest that these tensile fracture patterns appear to be an excellent indicator of the tectonic stress in particular because of their regional consistency.
So far, so good. In 1992, Eidelman & Reches were of course not aware of the Spanish spallation features and the paper of Ernstson et al. (2001), by the way printed in the same journal GEOLOGY, otherwise they could perhaps have discussed also a dynamic formation of their tensile fractures by spallation.
We will address this possibility here. With regard to their model and an interpretation of tectonic stress reflecting a single tectonic stage to deform pebbles even at depths of a few hundred meters, it appears rather peculiar that in the studied outcrops fracture-parallel displacements are practically absent (see Fig. 13). Eidelman & Reches mention less than 5% of the fractures showing a slip that is restricted to individual cobbles and is assumed to belong to a later stage. This later stage obviously means that stress distribution within the conglomerates enabled shear deformation, but it is hardly to not at all to understand why more than 95% of the already dissected cobbles escaped this shear forces completely. Moreover, we must not forget that the model of Eidelman & Reches is strongly idealized considering an elastic circular inclusion in a soft matrix under plane strain conditions (their Figure 4). This constellation may approximately function for the first tensile fracture to occur in each cobble, but for the development of the subsequent fractures opening subparallel to the first, second, third, etc. ones, these very idealized conditions are no longer fulfilled. The important observation of lacking slip added by the observation of conspicuously equidistant fractures in many cobbles (see Fig.13) creates some doubt whether the theoretically proper model of Eidelmann & Reches meets the field observations.
Hence we pose the question whether the tensile fracturing as described by Eidelman & Reches could be the result of rather a dynamic deformation having led to open, tensile spallation fractures, and for a first approximation we show photos (Figs. 14, 15) of a subparallel fracturing in quartzite conglomerates with open tensile fractures that has been shown to be the result of dynamic deformation in the Azuara-Rubielos de la Cérida impact event with a high degree of probability (Ernstson et al. 2001, and also HERE). The similarity to the fractured cobbles in the Eidelman & Reches outcrops (Fig. 13) without any displacements and abundant equidistant fractures is unmissable.
Fig. 14. Buntsandstein basal conglomerates near Ródenas, west of the Rubielos de la Cérida impact basin. A strong sub-parallel fracturing with open tensile fractures cutting through the cobbles is observed. No slip along the joints is observed.
Fig. 15. Another outcrop: Typical in situ subparallel fracturing in quartzite cobbles of the Buntsandstein basal conglomerates. The tensile character of most of the joints is obvious. No displacements due to shearing can be observed. Also note the equidistant fractures in many cobbles similar to Fig. 13.
To come straight to the point, we are far from postulating meteorite impacts in Israel and California to have affected the conglomerates under discussion. However, interestingly both locations for the observations of the peculiar fractures are found at prominent active faults, in Indio Hills along the eastern side of the San Andreas fault and in the Arava Valley of the Dead Sea rift in Israel, which are characterized by significant earthquake activities (e.g. the devastating 1068 AD earthquake in the southern Arava valley (Zilbermana et al. 2005), or the Magnitude 7.3 earthquake within 30 miles of Indio Hills (http://www.homefacts.com/earthquakes/California/Riverside-County/Indio-Hills.html).
Could it be that the tensile fracturing reported by Eidelmann & Reches was not produced by tectonic slow deformation but occurred dynamically by spallation induced by a heavy earthquake shock? Spallation as an earthquake damage to buildings is not uncommon. After the August 23, 2011, Mineral, Virginia earthquake the Washington Monument exhibited a number of spalls formed at the exterior surface of the pyramidion, and nice photographs can be seen in a report (WASHINGTON MONUMENT,Post-Earthquake Assessment, National Mall, Washington DC, EXECUTIVE SUMMARY) to be clicked HERE. Remarkably, the spalls as such are shown and described, but the physical process of spallation with the most effective tensile stress at the free surface is not addressed. Likewise, in earthquake engineering the term spalling (not spallation!) is frequently used but considers various mechanisms by which spalls simply break away from affected buildings or constructions.
We may ask whether the peculiar equidistant tensile fractures seen in the figures 13 – 15 and also observed with the fractured Ries belemnites are an attribute to support a dynamic formation by spallation. The experimentally fractured glass rod (Fig. 3) may underpin this assumption with regard to Fig. 16 where we show a snapshot taken from this figure. A physical model may consider some interference procedure and should be investigated in more detail.
On the whole and to summarize, dynamic deformation and spallation remain the “unknown entity” in geology, but with regard to the highlighting spallation experiments as discussed above (Figs. 2, 3) we have to be aware that even very small spallation energies are able to produce enormous damage. We don’t know whether the tensile-fracturing tectonic model of Eidelman & Reches is the correct explanation for the observations in Israel and the USA, but for replacing it by the more reasonable spallation model more field work under the aspect of an earthquake-related deformation is needed.
3 Meteorite impact spallation – mineralogical implications
Here we focus on a few examples of shock-induced spallation features and especially refer to earlier work published here on our website.Shock spallation on a microscopic scale especially in quartz grains can regularly be observed in shocked rocks from impact structures. Interestingly and rather surprisingly, these effects have never been considered by other impact researchers working on shock metamorphism in geologic materials, although spallation in quartz grains may be considered diagnostic of strong dynamic deformation. On the other hand, in impact engineering shock deformation and spallation damage by laser shock load in various materials and especially also in quartz has been addressed in recent times (Rességuier et al., 2005, 2010) featuring interesting results that, together with the effects shown here, should add to commonly described shock effects in quartz like planar deformation features (PDFs), planar fractures (PFs), diaplectic glass, ballen and feather structures.
Here we focus on a few examples of shock-induced spallation features and especially refer to earlier work published here on our website and elsewhere.
Fig. 17. Shocked sandstone from the Rubielos de la Cérida impact basin (Spain) with multiple spallation (tensile) fractures in quartz grains. Click on the image to read more about shock spallation and shock effects in general. Photomicrograph, crossed polarizers.
Fig. 18. Glass-filled spallation fractures in quartz grains from shocked rocks in the Chiemgau impact meteorite crater strewn field. Note the approximate mirror symmetry of fracture and grain boundary geometries. Photomicrographs, crossed polarizers.
Fig.19. Quartz grains in shocked impact melt rocks from the Nalbach impact event in the Saarland region. Note the glass-filled spallation (tensile) fractures identical to the Chiemgau features in Fig. 18. Blue: Some marked spalls; red: lines of symmetry within spall fragments.Photomicrographs, crossed polarizers. Image taken from the diploma thesis (Berger 2014).
Planar fractures (PFs) in quartz as a shock effect – also produced by spallation?
Commonly quartz is considered to have no cleavage, and in practically all mineralogical literature this statement is textbook knowledge. But this is not correct apart from very scarce hints to rare cleavage after the rhombohedron due to extreme tectonic pressure in strong regional metamorphism. However, cleavage in the form of crystallographically oriented planar fractures is a common shock effect in quartz (Fig. 20) and develops already at moderate shock intensities. Today, multiple sets of PFs in quartz are considered even diagnostic of shock and meteorite impact (French and Koeberl, 2010).
Fig. 20. Multiple sets of planar fractures (together with a few spots of diaplectic glass) in a quartz grain from shocked rock; Nalbach (Saarland) impact event. Photomicrograph, crossed polarizers. Image taken from the diploma thesis (Berger 2014).
But why this strict difference between strongly deformed quartz in tectonics revealing irregular fracturing at most and moderate shock to produce nice cleavage with more or less slightly open fractures (Fig. 20)? A reasonable explanation may be given by the difference in compressive and tensile stress of a material the latter in general being much lower than the former. Hence, cleavage in quartz may occur on tension following crystallographical planes of weakness but not on compression. And since tectonics may compress single quartz grains but is unable to pull a grain open, we need tension for cleavage and PFs, and the simple connection between impact shock and cleavage is given by spallation due to rarefaction from compressive shock reflected at the free surface of the quartz grain as tensile pulse. While this explanation makes some sense, additional conditions must obviously be fulfilled to produce either planar fractures of cleavage, or curved spallation tensile fractures like those in Figs. 18, 19, or subparallel open spallation fractures like those in Fig. 17. These conditions are unsettled so far.
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