Accretionary lapilli from the Azuara and Rubielos de la Cérida impact structures (Spain)

Accretionary lapilli is a term originally solely related with volcanism. Accretionary lapilli are pellets that form by the accretion of fine ash around condensing water droplets or solid particles, particularly in steam-rich eruptive columns. Commonly, they exhibit a concentric internal structure, and, once formed, they can be transported and deposited by pyroclastic fall, surge, or flow processes (Allaby & Allaby, 1999; A Dictionary of Earth Sciences). Armoured lapilli is the term that is especially used in the case the ash has accumulated around a small rock fragment. The armoured-lapilli variety is frequently found in deposits of basaltic base surges.

Image 1: Accretionary lapillus (diameter 0.5 mm) from the basal
suevite breccia in the Azuara impact structure (Mayer 1990).
Photomicrograph, xx nicols.

Since similar processes are related with the turbulent explosion plume raising above the expanding excavation cavity in an impact cratering event, it is not surprising that accretionary lapilli have been found also in impact deposits. Graup (1981) describes accretionary lapilli to occur in the suevite fall-back breccia of the Ries impact structure. They are also reported for ejecta deposits of the K/T Chicxulub impact structure in Mexico (, and Belize (

Concentrations of lapilli formed lapillistone that occurs as discontinuous, reworked clasts within the megabreccia related with the Late Devonian Alamo impact (

For the Azuara impact structure, accretionary lapilli was first reported by Mayer (1990). Image 1 shows a typical lapillus from the matrix of the basal suevite breccia near Muniesa. The interior is composed of very badly sorted material (calcite, quartz, ore). The rim zone is formed by concentric layers of finer material (mostly micritic calcite). Similar accretionary lapilli are observed also in the matrix of Azuara breccia dikes.

Accretionary lapilli also contribute to the matrix material of the basal suevite breccia and breccia dikes in the Rubielos de la Cérida elongated impact basin (as part of the Azuara/Rubielos de la Cérida impact crater chain, see Highlights ).

 2 3

 4 5

Images 2 – 5: Accretionary lapilli from the basal suevite breccia in the Rubielos de la Cérida impact basin. Photomicrographs, xx nicols; the fields are 3.5, 5, 6.5 and 3 mm wide.

Images 2 – 5 show accretionary lapilli from the basal suevite breccia near Corbatón in the Rubielos de la Cérida impact basin. The lapilli are basically carbonate with some accessory silicate material (e.g., quartz fragments, Image 3) and regularly exhibit the typical “onion skin” internal structure. The angular core of the lapillus in Image 5 probably is a fragment of a former lapillus thus reflecting some kind of reworking in the lapilli formation and deposition process.

Near the village of Olalla in the northern rim zone of the Rubielos de la Cérida impact basin, a prominent breccia dike is exposed (Images 6, 7). In the early seventies, in the course of his geologic mapping activities, W. Monninger called this dike “Teufelsmauer” (Devils Wall) because of its peculiar structure and composition. At that time, impact processes and impact rocks were not well known among geologists.

 6 7

Images 6, 7: The Devils Wall breccia dike near Olalla.

 8 9

Images 8, 9: The matrix of the Devils Wall breccia dike composed of accretionary lapilli. The whitish crusts of some breccia fragments are suggested to result from high-temperature decarbonization of limestone. Polished sections, the fields are 13 and 15 mm wide.

In polished sections (Images 8, 9), the matrix of the carbonate dike breccia for the most part proves to be completely composed of accretionary lapilli (lapillistone). Limestone fragments from the disintegrated host rock of the dike abundantly make up the core of larger lapilli. In doing so, the fragments my be broken but still remain coherent within the lapillus, as can be seen in Image 10. This shows that the accretion process continued upon injection of the vapor plume material into the host rock.

Image 10: Fragments of the breccia dike host rock make up the core of larger accretionary lapilli.

Regional geologists from Spain (M. Aurell, E. Díaz-Martínez, A. L. Cortés, and others) vehemently refusing the impact origin of Azuara and Rubielos de la Cérida, suggest the basal suevite breccia and breccia dikes to be diagenetic, pedogenetic or karstification features. For these geologists, the accretionary lapilli is calcrete (caliche).

Impact spallation in nature and experiment

Spallation is a well-known process in fracture mechanics as well as in impact cratering and has been investigated theoretically and experimentally by many researchers. Unfortunately, it is less well known that spallation can also be observed in nature as an actually existing geologic phenomenon in and around impact structures. The present WEEKLY IMAGE shows already known spallation features in conglomerates around the Azuara/Rubielos de la Cérida impact structures (Spain), now recognized to form a 120 km long impact crater chain (see

–  KLICK here; and Ernstson, K., Schüssler, U., Claudin, F. & Ernstson, T. (2003): An Impact Crater Chain in Northern Spain. – Meteorite, 9/3, 35-39 – KLICK here), and prominent spallation fractures only recently observed in ejecta (Pelarda Fm. ejecta) from this crater chain.Spallation takes place when a compressive shock 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 stresses lead to detachment of a spall or series of spalls.Prominent spallation effects have been reported for shocked Buntsandstein conglomerates exposed around the Azuara/Rubielos de la Cérida impact structures. Details about these geologic spallation features have been described in Ernstson, K., Rampino, M.R., and Hiltl, M. (2001): Cratered cobbles in Triassic Buntsandstein conglomerates in northeastern Spain: An indicator of shock deformation in the vicinity of large impacts. Geology, 29, 11-14., and can be found here.

Image A. Subparallel open spallation
fractures in a shocked quartzite cobble
from Buntsandstein conglomerates.

Image B. Spallation crater in a shocked
quartzite cobble from Buntsandstein

Image C. Shock experiment on artificial conglomerate.

Images D

Images E
Images D, E. Concave spallation fracture surfaces in quartzite boulders from the Pelarda Fm. ejecta.
The Images A and B show typical shock-produced spallation features in these Buntsandstein quartzite cobbles: subparallel open spallation fractures (Image A) and a concave fracture surface forming a crater after the detachment of a lens-shaped spall (Image B). This concave spall fracture near a spherically shaped reflection surface is predicted by theory (and hardly explained by any other geologic process) and can be produced experimentally as shown in Image C.
The shock experiments were performed at the Fraunhofer Institute for High-Speed Dynamics (Ernst-Mach-Institut) in Freiburg, Germany. A single-stage powder gun was used to accelerate steel projectiles. As targets, we used two quartz spheres (rock crystal) in contact, embedded in a synthetic epoxy matrix. The shots were performed with impact velocities in the range of 25 to 115 m/s, corresponding to initial impact pressures between 0.55 and 2.5 GPa (5.5 and 25 kbar). The recovered samples were cut in half (see Image C, shot 3), thin sections were made, and the results of our observations were presented in Ernstson, Rampino, and Hiltl (see above). Here, the recovered sample of shot 3 at lowest impact velocity is shown (Image C) displaying a clear spallation fracture in the right-hand sphere otherwise untouched.
In the Ernstson/Rampino/Hiltl paper published by Geology (see above), the importance of such shock-deformed autochthonous conglomerates for an easy recognition of regional impact signature has been pointed out.
Here, we report on recent observations of prominent spallation fractures in quartzite boulders from the Azuara/Rubielos de la Cérida impact ejecta (Pelarda Fm.). The Image D shows a typically deformed boulder that displays a concave spall fracture surface being a mirror image of the convex surface (sketched as white broken line in Image D) of the detached (and now missing) large spall. A similar concave spallation fracture can be seen in Image E.
The quartzite boulders (mostly Cambrian Bámbola quartzite and Ordovician Armorican quartzite) contributed to the upper part (dominating molasse sediments) of the purely sedimentary target and, upon impact, experienced moderate to strong shock before excavation and ejection. The shock is documented by abundant multiple sets of PDFs in quartzite boulders (see, e.g., the sound PDF analysis made by Dr. Ann Therriault, in: Ernstson, K., Claudin, F., Schüssler, U. & Hradil, K. (2002): The mid-Tertiary Azuara and Rubielos de la Cérida paired impact structures (Spain). – Treb. Mus. Geol. Barcelona, 11, 5-65 – KLICK here, and on shockeffects ). We assume that the prominent spall fractures in the large quartzite boulders have originated also from the initial shock event, although a formation by collision of quartzite boulders during excavation and ejection must also be taken into consideration.

An Impact Crater Chain in Northern Spain:

This is the title of an article only recently published in

METEORITE, The International Quarterly of Meteorites and Meteorite Science

For the readers of METEORITE (and others), the black-and-whites of the article are shown here as original color prints.


Fig. 1. Location map for the Azuara – Rubielos
de la Cérida impact crater chain (frame in
Fig. 2) and suspected impact locations (A, B, C).

Fig. 2. The topography of the Azuara/Rubielos
de la Cérida crater chain (from the digital map
of Spain, 1 : 250,000; provided by Manuel Cabedo).

Fig. 3. Photomicrograph of strongly shocked
quartz from the Rubielos de la Cérida basin.

Fig. 4. Part of the central uplift chain emerging from the Rubielos de la Cérida impact basin.

Fig. 5. The crater rim in the southern
part of the impact chain.

Fig. 6. Megabreccia and polished friction plane
in the southern part of the central-uplift chain.

Fig. 7. Impact breccia (suevite) exposed in
the southern part of the central-uplift chain.

Fig. 8. Probable impact ejecta near
Peñacerrada (location B in Fig. 1).

Ries impact structure: Bunte Breccia ejecta resting on scoured, Upper Jurassic limestone

The 26 km-diameter 15 m.y. Ries crater (Nördlinger Ries) in Germany belongs to the few large terrestrial impact structures with a well-preserved ejecta blanket. The multicolored (= bunt) appearance of the ejecta results from an intense mixture of green, dark grey, purple, red and yellowish clays with sandstones of diverse colours, white limestones, rocks from the crystalline basement and even organic material (charcoal; probably from the incorporation of local material upon landing). The Bunte Breccia reflects the major excavation and comprises more than 90% of the ejected material outside the crater rim.
 A  B
Image A shows the typical aspect of the Bunte Breccia in the Gundelsheim quarry 20 km from the center of the structure. In this quarry, the Bunte Breccia is removed little by little to enable the exploitation of the Malmian limestone. Thereby, prominent linear scour marks become visible having originated from the ballistic ejecta emplacement on the competent limestones (Image B). Similar scour marks are exposed all around the Ries crater, and a statistical analysis shows them to pointing radially away from the center of the structure. (Also see Hörz, F. (1982) Ejecta of the Ries Crater, Germany. – Geol. Soc. Am. Special Paper 190, 39-55.).

Azuara impact structure (Spain): Evidence of shock fluidization of competent limestones

Image A: Shattered chert nodule embedded in Muschelkalk limestone

Image B: Flow lines of white chert splinters
Near the village of Monforte de Moyuela at the SSW rim of the Azuara structure, chert nodules in Muschelkalk limestones show very peculiar deformations. The nodules are heavily shattered, fragmented down to millimeter-sized sharp-edged splinters and partly even pulverized (Image A). From these shattered nodules, flow lines of miniature chert splinters run into the limestone as shown in Image B and, for reasons of clarification, in the sketch of Image C. The area interspersed with the flow lines is of the order of some 100 square meters. A statistical analysis of the strike of the flow lines shows a distinct maximum pointing to the center of the impact structure (rose diagram in Image D).

Image C: Sketch of Muschelkalk – chert flow texture

Image D: Midpoint of rose diagram (strike of flow lines) corresponds to the location of Monforte de Moyuela
A diagenetic origin of this peculiar texture can clearly be excluded, and we suggest a short-term shock-induced fragmentation and fluidization of the Muschelkalk limestones and the embedded chert nodules. A relation may be seen to the acoustic fluidization proposed as possible mechanism to enable impact crater collapse in the modification stage (H. J. Melosh (1989): Impact Cratering. A Geologic Process).

Rubielos de la Cérida impact structure (Spain): Impact-induced internal rock polish.

Image A shows part of an extended megabreccia deposit in the southern central uplift of the Rubielos de la Cérida impact structure. Within a chaotic accumulation of limestone blocks and fragments, a large surface displaying prominent striae and polish occurs (hammer length 40 cm). Any relation to tectonic structures is clearly missing. It is assumed that the peculiar deformations formed in the highly compressive process of the central uplift development (modification stage of impact cratering).  A
 B An internal polish of strongly brecciated rocks is abundantly observed in the Rubielos de la Cérida structure; see Image B: mirror polish in a grit-brecciated megaclast of the Barrachina megabreccia.


The type locality of the peculiar curved joint pattern (Images A, B) has been found by H. Müller in the course of his diploma thesis mapping at the south-western ring of the Azuara impact structure (UTM coordinates, 684500/4555400, near Moneva) some 15 km from its center. The exposure shows fossiliferous Dogger limestones, which have undergone strong brittle fracturing. The joint sets under discussion are well exposed by their strong curvature. Two evidently conjugate sets with parallel strike form a system, which is nearly symmetrical to the vertical, and cut the rock into bars of approximately rhomboid shape. This often results in a rhomboid-within-rhomboid structure. Small displacements with slickensides parallel to dip have been observed to occur on the order of centimeters.
Proceeding with field examinations, more joint systems with quite similar shape were found throughout the ring terrain of the Azuara structure. However, in contrast with the sets in Image A , the curved joints in Image C (south of Belchite) display counter convexity, and Image D (near Almonacid de la Cuba) shows the phenomenon on a smaller scale with a more irregular pattern.
 C  D

E: All locations are displayed in Image E where the strike directions of the curved sets are plotted. Although statistically only weakly exemplified, there is a trend of radial strike related to the center of the impact structure

Discussion. – In contrast to well established rhomboid structures resulting from the intersection of linear joints, strongly curved conjugate joint sets producing rhomboid-within-rhomboid structures are virtually unknown up to now. In a proceedings paper, pp. 257-263 (Image F), Müller and Ernstson excluded a relation to listric faulting, a formation by sedimentational and diagenetic processes, and presented a model of a dynamic formation which considers the modulation of running fractures in the impact cratering process. According to this model, the stress field of the shock-driven excavation flow combines with the stress field of the rising rarefaction pulse to a time-varying stress field causing the propagation of fractures along curved paths. Such a process is well known in experimental fracture mechanics: The modulation of a running fracture by ultra-sonic waves produces an undulating fracture surface.In our paper, we compute and show that in the early (excavation) stage of the impact cratering process, the conditions of the formation of curved conjugate joint sets can be met locally and during a short period of time.The model is not only consistent with the Azuara observations (radial strike with respect to the center, convex and concave curvature, different radii of curvature, rhomboid-within-rhomboid structures) but also predicts curved joint sets to belong to the regular structural inventory of impact craters.

Azuara impact structure (Spain), Ries impact structure (Germany): impact as a geologic process

A few kilometers outside the northern ring of the Azuara impact structure near Belchite, a handful of isolated large blocks of Jurassic limestones emerge from the post-impact Upper Tertiary Ebro basin sediments. Quarrying in these blocks has enabled instructive insight into the drastic impact deformations experienced by very large rock volumes.
A  B
Image A shows part of a large quarry located at UTM coordinates 0687000, 4583000. The visible length in the image is roughly 300 m. The limestones are drastically destroyed through and through to form a more or less continuous breccia displaying grit (gries) brecciation and mortar texture (see Images B – E).  C
 D  E
Comparable strong and continuous deformations (Images F, G) can be observed in a limestone quarry located in another block at UTM coordinates 0683000, 4583000.
 F  G
H and I Ries impact structure; Iggenhausen quarry
 H  I
Comment: The Azuara region and the Jurassic limestones underwent Alpidic tectonics with some folding and block faulting, but we emphasize that Alpidic tectonics can not possibly have caused these disastrous deformations over hundreds of meters.
Impact cratering is the only reasonable process to have produced this impressive geologic scenario, and the same deformations are well known to occur in large allochthonous limestone megablocks ejected from the 25km-diameter Ries impact structure (Germany) (Images H, J; Iggenhausen quarry).We suggest that those geologists from the Zaragoza university and the Center of Astrobiology (Madrid) vehemently refusing an Azuara impact visit these highlighting outcrops. Since they like to contrast the Azuara structure with the Ries crater (see their MAPS paper referred to in the Controversy section), they will get a lot of illustrative material.There is one more point we want to refer to. As already said, impact is the only reasonable geologic process that explains these desastrous and voluminous deformations. In other words, there’s actually no need for the well documented strong shock effects in Azuara polymictic breccias to establish Azuara as an impact structure (see below in the Archives and ). The outcrops under discussion here are as well a convincing proof.Usually, the impact nature of a structure under discussion is established by the occurrence of shock metamorphism. Reasonably, it is argued that there are no endogenetic processes known to produce, e.g., diaplectic glass or planar deformation features (PDFs) in quartz. Likewise, we argue that there are no endogenetic geologic processes known to have catastrophically destroyed the Jurassic limestones near Belchite.

Therefore, geologists should be aware of their competence to establish in some cases an impact structure from pure field evidence. The time has come to give up the very limited point of view of some impact researchers that TEM analyses of PDFs or geochemical signature of the projectile are the ultimate requirement for establishing an impact structure.

Rubielos de la Cérida impact structure (Spain): impact melt glass from the central uplift

 A  B
The glass shown in A, B (B: the field is 14 mm wide) is coating a sandstone exposed in the central uplift of the Rubielos de la Cérida impact structure. The glass has a greenish to whitisch color and is transparent to milky. In thin section (C, D (xx nicols) – the field is 6 mm wide), the sandstone shows heavily damaged, and intense cataclastic flow texture is observed to merge with the glass. Quartz grains are strongly fractured and show multiple sets of planar fractures (PFs) and planar deformation features (PDFs).
 C  D
Interpretation: Despite the occurrence of shock features in the sandstone, the glass probably did not form by shock melting. We suggest frictional melting by extreme dynamic metamorphism in the impact event (excavation or – more probably – modification stage when the uplift formed) and the glass to be pseudotachylite. Temperatures in excess of 2,000 °C were probably required for the homogenization of this glass (David Griscom, pers. com.).
The location of this spectacular exposure of the glass-bearing sandstone remains secret for the moment in order to prevent it from destruction by rock hunters.

Rubielos de la Cérida impact structure, Spain: at the crater floor

This peculiar fold is exposed in a region of an extended megabreccia near the village of Barrachina in the Rubielos de la Cérida impact structure. The fold is portrayed by a competent, however heavily brecciated Lower Tertiary limestone layer. The core of the fold is a pulp of nearly pulverized carbonate rock without any regular internal structure. Only a few limestone fragments are preserved.

Interpretation: The exposure is assumed to be located at or near the crater floor of the Rubielos de la Cérida impact structure (for more details see:

Fieldguide – Stages of Crater

Fieldguide – Stop 7


where giant rock masses moved in the excavation and modification stage of impact cratering to form the now exposed megabreccia. The fold is interpreted to be the result of a high-pressure injection of extremely brecciated material from below. A tectonic origin of this peculiar structure is hardly to understand. Local geologists (from the Zaragoza university and the Center of Astrobiology, Madrid) suggest collapse by dissolution of gypsum to have produced the megabrecciation – need we comment?