The origin of the crater-shaped structures on the Uweinat-Howar Uplift

in the three country corner Egypt/Libya/Sudan

Norbert Brügge, Germany        
Dipl. - Geol.                           


Upload: 2004 !                              
New update:

1.1  The "Clayton Craters"
1.2  Mountains "Peter & Paul"

1.3  The basaltic plugs on top and nearby the southern Gilf Kebir plateau
1.4   Structures in the Great Sand Sea nearby the Gilf Kebir plateau
1.5  Structures at the western and northern foreland of Gilf Kebir

1.6  The crater "White Spot" on top of the Jebel Uweinat and further structures

2.0  The craters in the "Scarp-Contours" -- outside of the uplifted region (GKCF craters)
3.0  Further crater-fields at the Egyptian-Sudanese border

4.1  Crater B.P.

4.2  Crater Oasis

4.3  Craters Arkenu

4.4  Hadid Structure
4.4  Dalma Structures
5. Photogallery

Structural-geological History

Widely distributed and in unusually high numbers are sub-volcanic structures in the form of craters, dikes and plugs in a region in which the basement of the East Sahara Ghost Craton has risen to the surface (Uweinat-Howar Uplift).
The Uweinat-Howar Uplift between Kufra basin in the west and Dakhla basin in the east is a tectonically elevated block. Along main faults (possibly staggered), the basement has been lifted up to 2000 m compared to the Basement of the basins, and lie near surface level now (about +500m SL)
. The cause of the uplifting is hardly explored, but a continuously active plume in the earth's mantle is assumed by the author due to the long-lasting processes of uplifting (Ordovizium-Carboniferous) magmatism.
The overlying incomplete Palaeozoic sediments (Ordovizium-Carboniferous) were uplifted along with the basement above the plume. They are today as remains (plateaus) present, despite continuous erosion.

Last, during the late Eocene of the Tertiary period (about 46 - 42 Ma) in the underground of the Uplift, were initiated in the chamber with acidic magma new activities (ring-complexes of Jebels Uweinat, Arkenu, Babain, Bahari).
Then, in the Oligocene (38 - 28 Ma) in the Jebel Uweinat and Gilf Kebir region and surrounding was occur a culmination of subvolcanic activities. Various kinds of features are present, i.e. small-scaled cones, dykes or plugs as well as large crater-shaped structures. Frequently no volcanic rocks are exposed, or exist only as relics in the centre of the structures. In these cases, the circular pattern is manifested only by brecciated and hardened sediments with a higher resistance to erosion than the country rock. On other hand, basalt cones can be easely confounded with small sandstone hills covered with desert varnish.
The widespread plugs and dykes are either related to the Tertiary subvolcanic or intrusive ring complexes. In any case, there is an obvious correlation between igneous activity and the regional fault pattern. Very often subvolcanic rocks are situated at points of intersection of faults.
In general, the extrusives consist of alkaline, SiO2-undersaturated to oversaturated trachytes and related rocks, as well as of olivine-basalt. To a minor extent, intermediate to rhyolitic varieties are present.

  • Alkali olivine basalt: Cones and plugs of fine-grained alkali olivine basalts and associated rocks occur far beyond the boundaries of the Uweinat basement inlier. They can also be found on top of the southern Gilf Kebir plateau and in its eastern foreland.
  • Trachyte and related rocks: Alkali trachyte, saturated trachyte, trachy-phonolite, and phonolite are considered within this rock group which is the most common subvolcanic group in the entire region. Typical of all is their fine-grained trachytic fabric. Some rocks are clearly fluidally developed, while others are completely unoriented. When the trachytic rocks are considered together with the olivine basalt und with the related basanite, tephrite and phonotephrite outcrops from east of the Gillf Kebir plateau, this could mean that two or more such alkaline cycles have to be assumed.
  • Rhyolotic rocks: Extrusive rhyolitic rocks are scare within the Jebel Uweinat and Jebel Kamil.

From the many widespread subvolcanic structures two crater - fields are considered up to now mostly:

Gilf Kebir Crater Field - GKCF (Outside of the uplifted region)
The basaltic magma intruded into Basement, Paleozoic and Nubian layers with high energy. Thereby rocks and quartz grains were shaped by shock waves and destroys (breccia, planar lamelles) and in addition melted or fused by heat.
The melted or fused breccia became out pressed by the ascent of the magma and forms the rim of the craters. In the breccia are included demolished Basement material, broken parts of Paleozoic sandstones, debris from the layer between them (well-rounded quartz and angular debris) and finally light Nubian sandstones. The breccia is tips over at the rim of the crater to outside and is broken. The basaltic plug often is not lifted out or is spilled.

Clayton Craters (Central Uplift)
In the Clayton Craters are been found basaltic plugs. The rims of the craters have an other structure. The rims are composed of steeply erected Paleozoic sandstones. Nubian sandstones normally are missing (central Uplift !). Frequent are also dykes with Basalt between the edges. Breccias were not found up to now. It is evident, that the dynamic conditions were different. Presumably the basaltic magma had a slighter explosive power and is climbed slow and along longer time.

There are further striking subvolcanic structures, which should be discussed likewise here:

  • Libyan crater-shaped structures "Oasis" , "B.P." and Arkenu

  • Crater "White Spot" (Jebel Uweinat)

  • Hydrovolcanic pipes nearby "Regenfeld"

  • .... etc.

Map with crater-shaped structures and plugs in the Western Desert

1.0  The craters in the uplift-region around Gilf Kebir and Jebel Uweinat

1.1   The "Clayton Craters"

The main group of  the Clayton craters

"In the region of the Jebel Uweinat und Gilf Kebir, there are hundreds of intrusive plugs und dykes, ranging in composition from Carbonatites to Olivine Mela-Nephelinites, Alkali-Basalts and minor Phonolites and Trachytes. Olivine Mela-Nephelinites, Basanites and Alkali Basalts are the most abundant rock types. These rocks are from ring complexes and mafic plugs located between the Jebel Uweinat and the Gilf Kebir. These intrusive rocks range from 28.2 to 26.7 Ma in age. Olivine Mela-Nephelinites and Basanites are not genetically related to each other by fractionation but they represent primitive magmas generated by different degrees of partial melting of a metasomatised upper mantle source. Incompatible trace elements in Olivine Mela-Nephelinites may be modelled with small degrees of partial melting of such a source. Close relationships are also observed with the slightly older intrusive rocks from Gilf Kebir suggesting that Uweinat magmatism is possibly related to a northeastward migration of the African plate above an intracontinental Hot Spot." (Source:

On the active line following structures are found from the southwestern to the northeastern direction:

  • Crater "White Spot", dykes and basaltic plugs in the Jebel Uweinat,

  • many dykes and craters in the area between Jebel Uweinat and Gilf Kebir,

  • all groups of Clayton's Craters,

  • basalts and crater-shaped structures along and on top of the southern Gilf Kebir Plateau,

  • large crater fields of the "Scarp-Contours" in the eastern direction of Gilf Kebir,

  • hydrovolcanic pipes nearby "Regenfeld",

  • crater like structure "Jasper Mountain"

All of the craters - meant are the  Clayton Craters - are not volcanic explosion craters (in sense K. SANDFORD, 1934). The best argument against explosion events are Carboniferous layers in the centre of a large crater (with bright trachyte therein), which contain plant imprints (Carboniferous plant imprints).

The craters were first seen by an airplane during the 1932 Almasy - Clayton expedition by Sir Robert Clayton. Therefore the craters were named to him. The first serious study of the craters was done by K.S. Sandford, who accompanied the 1934 Bagnold expedition.
SANDFORDS's study is the most comprehensive in the region between Gebel Uweinat and the Gilf Kebir he described: 1) open craters, probably the result of single explosions. 2) craters with subidiary plugs of trachyte. 3) trachyte necks with boundary walls of indurated sandstone. 4) isolated hills capped with trachytic lava.
The crater walls he described as "almost vertical, of intensely indurated and silicified sandstones, brecciated on a large scale as weII as in the hand-specimen, locally with columnar structure imposed upon them, the prisms being more or less horizontal (at right angles to the source of heat). With the exception of the columnar joints, this general crater morphology was present even in those features that lacked central igneous masses.
The contact between sandstone and the various trachytic plugs was typically fused. From thin sections of these fused zones, Sandford described "heat or explosion-shattered grains of well-rounded quartz, with an isotropic black, brown, and glassy material between them"



           An  intrusive dyke in the foreground of the crater                                                                                                          An other dyke with erected layers

The rims of the craters are of sandstone, tilted vertical by intrusive forces, and fused by heat on their inner sides. There traces of intrusive rocks (Basalt or Trachyte) within some of the craters. The basaltic plugs are sometimes visible as small hexagonal columns.
Likely it was a slow upthrust of magma, that also explains the almost perfectly vertical walls. In some craters the magma remained, while in others it fully subsided, leaving empty craters only containing material from the erosion of the rim and inblown sand of the desert.

      Visible central plug of intrusive white Trachyte                                                               View of a crater  with erected Paleozoic sandstones

Many craters are associated with dykes formed by two parallel uptilted rows of sandstone, filled with white Trachyte in between. Some craters are imbued by the dykes even within their rims, and the only intrusive material was found in between the dyke walls.
There are also narrow dykes, which cross rim and bottom of the crater, where they have the same kind of sandwitched structure with two upright walls of sandstone, and intrusive material in between (Andras Zboray).
It is quite clear, that magma having welled here up along fissures. These dykes are a little bit younger or at most contemporary with the main structure, because they crossed the rims and the bottom of craters.
The magma-chamber in the underground was still activ. The magma in the plug was not yet hardened. New magma has been transported up on fresh fissures. The fissures can cross also craters and it plugs therein.
There are large and small dykes. The small dykes are only thin fissures. The filling with basaltic magma in all kinds of dykes is visible or not (similar like at the plugs). The erected walls at the dykes (large or small) within the craters are really no rubble. That means, that the plug is hidden more deeply. Over it lies a lifted stopper of original sandstone layers.

A. Zboray: "Here we noted that the crater floor is crossed by vertical sandstone dykes, and the only trace of volcanic material is located
 in a dyke flanked by parallel sandstone walls, running along the south edge of the crater."


Structural samples for the origin of the craters

A large significant crater with Carboniferous plant imprints and igneous trachyte inside


The large crater  .... inside (3)  ..... with white Trachyte (4)
          Erected sandstone wall
 Dykes (2) Basaltic Plug on uplifted Basement (22°18'01''N / 25°24'15''E)
Plug Basaltic plug   A large northern crater    


1.2  Mountains "Peter & Paul"

The area with the striking mountains "Peter & Paul" is located between Clayton Craters and the granitic "unknown" plateau in the north. The both mountains consist of trachyte intrusions.
A further hill east of Peter and Paul typifies the locality. It stands approximately 25 m above the plain. The upper half is composed of trachyte with characteristic jointing that gives it a columnar, steep-sided appearance. The lower half is composed of a mixture of trachyte and basal conglomerate with a distinct apron of debris.


  "Peter & Paul"   Granite in the foreground   Trachyte plug    


1.3   The basaltic plugs on top and nearby the southern Gilf Kebir plateau

In the area of the southern Gilf Kebir plateau (Kemal-el-Din Plateau) we can see on pictures of "Landsat" numerous craters on the uppermost altitude of the plateau, which is difficult accessible with cars. It is described, that the top of the plateau is perfectly flat and featureless, interrupted by low basalt hills frequently. It is however sure, that many of these "craters" include basaltic bodies.

Now exist the first remarkable photo of basalt columns in the Wadi Akhdar. This hill has a base of 300 x 125 m and was discovered by Andras Zboray in 2008. The first time also is documented a circular structure with a basaltic plug in the centre, found by Andras Zboray (2010) in the Wadi Mashi.  Up to the plateau -- in the wadis -- are to be found just further structures of basalt and trachyte. More photos are now available by Ursula Steiner, Switzerland.


  Documented Locations (Loc) 23° 07' 60'' N / 26° 02' 33'' E (Loc-1)  Crater ouside of Wadi Mashi with Basalt and Quartz Trachyte Wadi Wassa
Large basaltic Plug in the Wadi Akhdar (Loc-2) Basalt Wadi Mashi (Loc-3)      
Basalt Wadi Dayiq (Loc-4) Crater inside with Basalt (Loc-5) Twin peak Basalt (Loc-6) Trachyte or Basalt in a northern Wadi (Loc-7) Trachyte in a Wadi on east side of Gilf  Kebir (Loc-8)
Trachyte in the Wadi Mashi (Loc-9) Trachyte with included tuber of Iron oxide; Wadi Mashi Trachyte (Loc 10) Basalt Wadi Akhdar (Loc 11)
 Trachyte in the Wadi Akhdar (Loc 12) Small Ring-dyke, Mouth of Wadi Mashi Trachyte Bubble, Wadi Dayiq


Detected augite ferrobasalt at northeastern site auf Kemal-el-Din plateau

It was found a porphyritic, fine-grained igneous rock dominated by phenocrysts of olivine (30 vol% pheno) and augite in a groundmass of augite, abundant magnetite, minor plagioclase and nepheline. Olivine phenocrysts form colourless, euhedral crystals up to 2 mm in size and are partly altered to red brown iddingsite. Augite phenocrysts are euhedral crystals up to 1 mm in size and often contain magnetite inclusions. The groundmass consists of subhedral brown augite, small laths of plagioclase and euhedral magnetite. Nepheline occurs as areas of nepheline.
Specimen is a primitive basalt dominated by olivine and pyroxene with very little plagioclase. Minor amounts of nepheline indicate this is a silica undersaturated alkali basalt. Enough magnetite is present in the sample to make it highly magnetic.

Rock Library,  Imperial College London, Author: Matt Genge (2017)



1.4   Structures in the Great Sand Sea nearby the Gilf Kebir plateau


Crater El-Baz  nearby the Gilf Kebir
 24° 13' N / 26° 24' E

Crater-shaped structure"Qaret-el-Hanash"
southern of Silica field

Pillar of brecciated rocks
 in the northern Great Sand Sea
27° 07' 60" N / 26° 28' 60"E

Not far from the Gilf Kebir plateau are to be found in the northeastern direction further structures on pictures of "Landsat".  There only rare pictures of a pillar with brecciated rocks.  It is named "Sakhret-al-Amud". The most known is the crater El-Baz at the beginning of the Great Sand Sea. It is reported, that in this structure are to be found "black rocks". In the near past, remarkable finds were made of carbon/diamond in sediment. Sensational is the finding of large dark brown
diamonds in the structure Qaret-el-Hanash..




Crater "El-Baz" (3)

 Sakhret-al-Amud (2)  

"Qaret el Hanash" near Silica field: Breccias contain jasper and a black melt with diamonds

Carbon in sediment

Basaltic boulders with enclosed Silica


1.5  Structures at the western and northern foreland of Gilf Kebir

During the tour in 2010 the author found in the western foreland of the Gilf Kebir, between Wadi Sura and Aqaba passage, surprising many dykes, with erected layers therein.
On the satellite pictures is to see a network of such structures. This means that the subvolcanism in a larger area was active as known before.

Many volcanic Fissures with erected layers between Wadi Sura and Aqaba (6)

Hydrovolcano (Um Ras)

Ring intrusion



  Subvolcanic plugs in the "Crater Kebira" area

Pushed zone of white erratic blocks. Loc 24°32'25"N / 25°05'30"E      


1.6   The crater "White Spot" on top of the Jebel Uweinat and further structures

The crater "White Spot" on top of Jebel Uweinat (Hassanein plateau) is clearly a basaltic plug. At the bottom of the crater is basaltic material available. The rims of the crater are composed of Paleozoic sandstones. They are not erected in contrast to the Clayton Craters. Probably the sandstones were broken by the up-directed pressure in concentric steps. The originally horizontal stratification was therefore not changed in principle. Directly inside of the crater are to be found few up squeezed sandstones too. The crater is found on the top of Hassanein plateau. The whole plateau has been uplifted by an intrusive event.

Crater "White Spot" (21°55' 01'' N / 25°02'48'' E)


Crater "White Spot" Basalt/"White Spot" Volcanic plug ? (Karkur Talh) Volcanic Tracks in the Karkur Talh area (2)

Northern branch of Karkur Talh: Trachyte and Rhyolite intrusiva

 "Basalt" Wahesh fault

  Dyke; Karkur Talh foreland





2.0  The craters in the "Scarp-Contours" -- outside of the uplifted region (craters GKCF)

(the so named "Impact Craters Field" by Philippe Paillou, Observatoire Aquitain des Sciences de l'Univers in Floirac, France)

In the year 2004 explored Philippe Paillou and a team by two fieldworks (February and December) several of circular structures in the east of the Gilf Kebir plateau. In an area between 26°30' - 27°30' E and 23° 00' - 24°40' N (~21.000 km2) were detected many hundred crater-shaped structures in satellite-images. The fieldwork should confirm that is a large impact crater field. The impact origin was derived by the observation of shock-related structures, such as Shatter Cones (SC) and planar fractures (PF's) in quartz grains of breccias. In the first time 13 craters were studied. Shatter Cones were found on the border of three craters (GKCF-01, GKCF-02 and GKCF-12).

Some controversial observations

Andras Zboray, Hungary,  told me, that the crater (meant is GKCF-13) superficially looks almost the same as the Clayton Craters, with a major difference. The crater walls are very clear of horizontally bedded sandstone, whereas at Clayton Craters the walls are all rotated 90 degrees. The layers seem to dip slightly inwards (?). There became found a layer of fused sandstone breccia, with purple sandstone fragments embedded into a white sandstone matrix. However the purple fragments appear rounded and weathered (a brown cortex visible where rock fractured around the embedded fragments), not sharp angular.

Philippe Paillou has also described: "Abundant polymict breccias were observed along the rim of all craters, forming pluri-decimetric to metric beds, sometimes interbedded with sandstones. They consist of centimeter- to decimeter-sized irregular fragments, embedded in a fine-grained quartz matrix. Beds are systematically dipping inwards (?) the crater, with a steep dip dose to vertical on the highest rims down to about 30° on the lowest observable rims."

Are these observations possible?
I have the crater GKCF-13 and others seen also. In the craters the beds dipping not inwards, in contrary the beds climb upwards, were tipped over on the rim and broken outside. Consider the pictures below. My opinion for the origin of the crater GKCF-13 is presented in the sample below.
The Shatter Cones are not valid.
These structures are Pseudo Shatter Cones (PSC). The enormous Pseudo Shatter Cone structures were modelled by wind erosion. This forms were found also outside of the crater field in the Gilf Kebir region. There are however meanwhile further important knowledges, that the circular structures in the large field, are of subvolcanic origin. Some structures contain basalts. Also dykes are frequent. Breccias on the crater rims contain marks of subvolcanic activities.

The supposed "largest impact crater field on Earth in the Gilf Kebir region" is a legend therefore !

Gilf Kebir Crater Fields (GKCF)
The red points are craters which were identified by the satellite SPOT.
Source: Paillou/CNES

Typical landscape of the crater field

Images from the prominent Crater GKCF-13

View into GKCF-13 from the northern position

View into the crater GKCF-13 with a diameter of 950m. Position: 23°18'23'' N / 26°55'28'' E





 Author 2004

Southern outside

Some as"impact proofs" presentd images of Philippe Paillou and team  
( )

Breccia  with included basement material  (GKCF-01and GKCF-05)  

 Broken sandstone with marks of
 hydrovolcanic solutions (GKCF-04)

Different brecciated material (GKCF-61)


Basalts hills and fused sediments of GKCF

A remarkable Basalt plug inside of a crater


Enormous Basalt Hill

"Beacon Hill" (2)

      "Red Hill"

Fused Sandstone (4)

Uplifted Sandstone (3)

Uplifted Breccias (3)




The supposed "largest impact crater field on Earth in the Gilf Kebir region" is a legend. The craters of the "Scarp-Contours" (and crater El-Baz) can be distinguished by a geological particularity from the Clayton Craters. The rims the of Clayton Craters contain only Paleozoic sandstones (Nubian sandstones were not deposited in the area of the uplift). The rims of the craters in the "Scarp-Contours" (GKCF-13 and others) contain Nubian sandstones with embedded breccia of Paleozoic debris or breccia with pure Basement material. The erected Nubian sandstones and the breccia were tipped over on the crater rim and broken outside. The breccia was changed by heat and pressure. Is it possible, that planar fractures in quartz grains emerge by effect of this intrusive magmatism ? I think it is possible. Planar fractures (PF's) in quartz grains are an indicator for low shock pressure ( e.g. 3-5 GPa). Clear proofs for impact structures does not give it up to now here. PF's in quartz grains are no clear proofs. Possible proofs would be the occurrence of Coesite and Stishovite. Both are high pressure modifications of quartz with high density. In the supposed "impact" craters in the Gilf Kebir region was found none. The evidence of solutions in breccias prove subvolcanic processes. The enormous Pseudo Shatter Cone structures were modelled by wind erosion.
These important counterevidences are considered too slight up to now.   It is also remarkable, that in the crater field were found basalts and many dykes. Some structures are cut by dykes. New investigations of the geological aspects were made now by Di Martino and team (2005).


What's new since 2004:


No "largest impact crater field on Earth in the Gilf Kebir region" ?


"We (Philippe Paillou and team) visited 62 structures during two expeditions in February and December 2004. Their diameters range from 10 to 2120 m. Except for a couple of small structures covered by the Quaternary sand sheet, most of them present well-defined rims, with heights ranging from a couple of meters to more than 80 m. Most structures are more or less filled with Quaternary aeolian deposits, their centre being in general higher than the surroundings. Rims are made of tilted sandstone layers of the Sabaya Formation (Albian age, around 110 Ma) covered by breccia, some-times also covered by paleo-soils. Some structures are cross-cut by basalt dykes, indicating that volcanism took place after their formation. Since basalts in the region are of Lutetian age (46 Ma), we can conclude that the structures certainly formed before this time. Shatter-cone-like features were found along the rim of several crater structures. However, wind erosion of exposed rocks can produce such features, and we could not clearly observe the typical striation patterns of shatter cones. Abundant occurrences of breccias were observed along the rim of numerous structures, forming pluri-decimetric to metric beds, sometimes interbedded with breccia formations can be produced by classical geological processes such as tectonics and rock falls, but they do also occur in and around impact structures. Optical microscopic analysis of thin sections of breccia and sandstone samples collected on the rims of several structures have shown that quartz is the predominant mineral component of all samples; minor components include phyllosilicates, iron oxides, and some accessory minerals such as zircon. Many quartz grain in these samples contain planar and sub-planar micro-deformations, strongly reminiscent of planar fractures (PFs), known from weakly shocked quartz of many impact structures, but also from tectonic settings. GPR soundings were performed on 10 of the visited structures and on some areas between these structures. The collected data showed the occurrence of faulting, fractures and chaotic buried terrains in the quasi totality of the radar transects. All GPR profiles reveal the same subsurface morphology: a perturbed paraboloid structure buried under sediments. In terms of lack of stratigraphy and scattering phenomena, they are quite different from typical profiles observed for volcanic craters for instance."
"The typical size (about 150 m) and number (more than 1300) of the structures in the Gilf Kebir region are compatible with the hydrothermal vent hypothesis and the brecciated sediments found around most of the structures that were visited could have been produced by fluidized sediments reaching the surface. However, southwestern Egypt is not known as part of a large igneous province, it is thus required to discover a major (and still unknown) hydrothermal event there that could have produced such vent complexes. GPR sounding performed on several structures revealed a flat floor covered by sedimentary deposits: hydrothermal vents should show tracks of a vertical structure, the conduit zone connecting to the tip of a sill intrusion. Also, we could not find evidence of sediment dykes and pipes in the 62 structures we visited, even though they should be abundant in the case of hydrothermal vents."



Non-impact origin of the crater field in the Gilf Kebir region (SW Egypt)

M. Di Martino 1, L. Orti 2,3, L. Matassoni 2, M. Morelli 2,3, R. Serra 4, A. Buzzigoli 5
1) INAF-Osservatorio Astronomico di Torino, Pino Torinese, Italy
2) Museo di Scienze Planetarie, Prato, Italy
3) Dipartimento di Scienze della Terra, Università di Firenze, Italy
4) Dipartimento di Fisica, Università di Bologna, Italy
5) Laboratorio di Geofisica Applicata, Dipartimento di Ingegneria Civile, Università di Firenze, Italy



"November 2005 expedition we carried out fieldwork on 7 of 13 craters identified as impact craters, namely GKCF-01, GKCF-06, GKCF-07, GKCF-08, GKCF-11, GKCF-12, GKCF-13, and we collected rock samples from GKCF-01, GKCF-07, GKCF-11, GKCF-13, on which petrographic studies has been in part performed. Also some other similar circular structures in the surroundings have been examined.
Macroscopic and petrographic observations
The outcropping lithologies in the investigated area mainly consists of quartz-arenites and minor micro-conglomerates. There is also the presence of two kinds of breccias, one of which is an intraformational (sedimentary) the other one possibly of hydrothermal origin.
Quartz-arenites, micro-conglomerates. Medium- to coarse-grained, rarely fine-grained, sandstones with sub-rounded/sub-angular elements mainly composed of quartz and minor sedimentary lithic grains (fine-grained quartz-arenites). Matrix, when not altered, is composed of very fine quartz grains and phyllosilicates; more commonly it’s partially or totally replaced by iron oxides/hydroxides cement and minor ferriferous carbonates. Accessory minerals: zircon, tourmaline, muscovite. Quartz grains often show micro-fracturing. Polycrystalline quartz is present. In some places the arenites grades to micro-conglomerates with rounded/sub-rounded quartz grains and sedimentary lithic clasts (fine-grained quartz-arenites) mm- to cm-sized.
They outcrop in the inner parts of the circular structures but also in the surroundings external parts. Intraformational breccias are constituted by quartz-arenitic clasts, angular/sub-angular in shape, cm- to dm-sized, rarely up to 20-40 cm. Their stratigraphic position is not always clear, but they seems intercalated with quartz-arenites. Breccias of possible hydrothermal origin are constituted by sub-angular/sub-rounded quartz grains, mm- to cm-sized and by rock fragments (fine- to coarse-grained quartz-arenites and minor siltites), cm- to dm-sized and varying in shape from angular/sub-angular to sub-rounded. In this second kind of breccia rare boulders constituted by sedimentary breccia are included. When not altered, matrix is composed of fine-grained quartz grains and phyllosilicates; often it’s totally replaced by iron oxides/hydroxides cement and minor ferriferous carbonates. Accessory minerals: zircon, tourmaline (<1%). Quartz grains often show micro-fracturing. Polycrystalline quartz is rarely present.
Morphology and Structural Setting
In some cases the rim of these roughly circular features is made by tilted layers of sandstones. In some other cases there is the presence of arc-shaped (and concentric) nearly vertical fracture planes, which characterize not only the supposed “impact craters”, but are also present around their periphery and in isolated structures in the surroundings.
These fracture planes are often associated with Fe-oxide/hydroxide mineralizations (situation observable not only at the “crater-scale” but also at smaller scale) and with breccia bodies of probable hydrothermal origin.
Pseudo-shatter cones
The surfaces of the outcropping rocks in the craters area are characterized by striations that, in some cases, resemble very much to shatter cones. From the data collected in the field it’s possible to say that:
- the striations observed are superficial and not pervasive;
- these features are characterized by directions always varying from N 20° to N 340°, rather consistent with the main winds direction (from N and N-E at present, from NW in the early Holocene, and no more present);
- the same striations are visible also on the breccia surfaces and on the surfaces of rocks out of the craters area;
- they are not fracture surfaces but occur on outcrops surfaces.
From these observations we conclude that this “pseudo-shatter cones features” are likely due to wind abrasion. GKCF-01, GKCF-13, El-Baz volcanic crater.

It has been suggested that the Gilf Kebir crater field could be the result of a meteorite impacts (Paillou et al., 2004; Paillou et al., 2006). The present study has been carried out in order to confirm or not the impact origin of these structures. From the fieldwork and from the preliminary analyses, the following results can be summarized.
“Target rocks”:            Don’t show any macroscopic or microscopic shock effects, in particular no PDF’s, no evidence of melting, no glass.
Breccias:                        Don’t show any macroscopic or microscopic shock effects. They are of intraformational and possibly hydrothermal origins.
Pseudo-shatter cones: The striations which characterize some rocks near the “craters”and identified as shatter cones are due, very likely, to the wind erosion.
Morphology:                  The same morphology, characteristic of the supposed “impact craters”, is identifiable (both in the field and in satellite images) in many others structures in their surroundings
                                         with sizes ranging from some tens of meters to kilometers (and some of these are associated with basalts).
These evidences indicates that all these features have a common non impact origin.

On the basis of this preliminary investigation, we can say that there are no clear and unequivocal evidence for an impact origin of the circular structures in Gilf Kebir region:
the origin of the craters is very probably associated to endogenic geological processes. The hydrothermal venting could account for the origin of such an extended field of circular structures. In this case the brecciation could be fluid-induced, probably for the fluctuations in pore fluids pressure. These hydrothermal fluids could also have been enriched with iron oxide during their way to the surface, crossing oxidized sediments or paleo-soils. The pre-existing sets of fractures planes could have driven partly the fluids circulation.
The presence of such an extended field of circular structures, linked to a widespread volcanic activity in the surroundings, leads to take in consideration a hydrothermal origin for these structures."

View into the crater GKCF-01 of diameter 630m. Position: 23°14' 37'' N / 27° 27' 37'' E


  GKCF-13/Breccias (4) GKCF-13/Solutions GKCF-13 GKCF-07/Rim
GKCK-01/Rim (2) GKCF-01/Rim (2)  GKCF-01/ Rim (3)


GKCF-01/Breccia GKCF-01/Breccia basement GKCF-01/Breccia GKCF-01/Changed arenite  Small crater south of GKCF-13  GKCF-02

Further proofs for the hydrovolcanic origin of the GKCF structures

New images from structures of the GKCF

Small Crater nearby GKCF-13 (Author 2010 Hydrovolcanic Structure  Tilted Layers (Author 2010)
Small Crater (Author 2010)  Hill with uplifted red layers (2) Crater Field nearby Jasper Mountain (6)

Hydrovolcanic pipes nearby Abu Ballas and "Regenfeld"

Jasper Mountain nearby Abu Ballas

Jasper Crater

Jasper Mountain

 Blood Jasper


Quartz, Chalcedony

Photos by Ursula Steiner, Switzerland

Jasper breccia (Gilf Kebir; Wadi Hamra)




3.0  Further crater-fields at the Egyptian-Sudanese border
(Jebel Kamil and surrounding)

In 2009, the author have discoverd further crater - fields by Google-Earth, which are located in east of Jebel Uweinat (Jebel Kamil) and southwest of this in northern Sudan. Most of the structures are similarly of them in the large crater - field "GKCF" in the east of Gilf Kebir ("Scarp-Contours").
Amid the crater-shaped structures are to be recognized basaltic cones. The crater-field in the Jebel Kamil has the coordinates between 21° 58' to 22° 03' N and 26° 13' to 26° 20' E. The crater-field in the northern Sudan has the coordinates 21°50' to 21°58' N and 25°51' to 26° 00' E.
Some other such structures have recently been found further south in the vicinity of the so-called Lakia structure (Krisztian Klajnik). 20.60 ° N / 26.55 ° E

Basalts between the crater-shaped structures at the Jebel Kamil

Basalts between the crater-shaped structures

Large structure: 21°26' 28'' N / 26° 04' 42'' E




4.0  The supposed "impact" craters in Libya

4.1  Crater B.P.

The B.P. structure, located at 25°19' N/24°20'E, was first referred by Martin (1969). It is a complex structure with a small central area of strongly deformed, upturned strata, and a prominent ring of up to 50 m high hills at 1 km from the center of the structure. The morphology of this crater structure suggests that it is eroded, with the hills representing the remaining roots of the crater rim not showing overturning, and only a small fragment of the original central uplift having remained. The rocks in the B.P. area are more or less ferruginous sandstones, with intercalated siltstones and local conglomerate exposures.

Koeberl et al. (2005) reported a remote sensing study and first outcomes of their fieldwork of 2001. Their field work indicated that the actual diameter of the BP structure is just about 2 km. The crater rim (their ‘‘middle ring’’) was characterized by a distinct series of hills of up to 30 m elevation above the surrounding desert, with sandstone dipping outward. They observed that some parts of the rim were strongly folded and faulted. The innermost elevation is a complex terrain of strongly folded sandstone hills, quite a few of which show steeply upturned bedding. No datable phases (such as melt breccia or authigenic minerals) have been discovered.
According to French et al. (1974), medium- to coarse-grained orthoquarzite was sampled with quartz grains that displayed multiple sets of ‘‘planar elements’’. In particular, PDFs and planar fluid inclusion trails were summarily termed planar elements.

French el al. (1974) and Underwood and Fisk (1980) described BP as consisting of two discontinuous rings that surrounded a central block; the outer ring of hills is 2.8 km in diameter with about 20 m of maximum relief, with sandstone beds dipping inward (?) at 3°-15°. The inner ring of hills is more deformed, has a diameter of about 2 km, and an average relief of 30 m. Most of these beds dip outward at 20°-40°. These two rings form an asymmetric (wider on the eastern side) ring syncline. According to Underwood and Fisk (1980), the inner ring also shows numerous gently plunging folds with axes tangent to the structure and dipping outwards by as much as 70°. The central block is 0.6 km in diameter and has about 38 m of relief. Beds arc intensely jointed, and the eroded southern half of the block exposes the oldest rock in the area, a light-coloured (purplish to whitish) sandstone that has been complexly folded.
Within the structure itself, Underwood and Fisk (1980) reported only Nubian Sandstone. These authors noted that the structure consisted of three near-circular concentric rock outcrops. The innermost ring had high-angle and chaotic dips forming a mass of craggy outcrop. The middle ring consisted of uniformly outward-dipping (30°-50°) strata. The third ring dipped inward (?) at 5°-15° and formed a low scarp, for most of its extent barely protruding above the surface. Underwood and Fisk (1980) interpreted these outer two rings to define a ring syncline.

Erected and broken sandstone walls


B.P. ring dyke structure with central uplift

The uplifted sandstones from the central block were subjected intense shear-movements



4.2  Crater Oasis

The Oasis structure is centred at 24° 35' N and 24° 24' E. The structure was reported by Underwood and Fisk (1980) to have a "disturbed zone" of 11.5 km diameter, but the discontinuous hills that compose the topographically prominent part of the structure form a circular array of 5.1 km diameter. Most of the rocks in this prominent ring dip outward, and locally they are intensely folded, Hills reach a maximum height of about 100 m. Outside of this ring, the disturbed rocks have only a meter of relief. There is no observed central uplift-structure.
The strata within this ring are intensely crushed, and in some places strata are overturned or vertical. Although there have not been any megabreccias found at Oasis, a team of scientists in the 1970s identified a glass-bearing microbreccia in the rocks. This microbreccia consists of shock quartz grains and pieces of sandstone, intermixed with partially devitrified glass, all within a recrystallized matrix.
Shock metamorphism is abundant in the sandstone. The most diagnostic features are open fractures and planar deformation features (PDF's), which are quite abundant. Planar deformation fractures are present but poorly developed.
Gibson et al. (2011) found that the rocks of the central parts of the structure highly kaolinitized and contain iron and manganese nodules, zones of iron impregnation and, locally, chert, all of which signifies extensive fluid movement. 
Volume-trically smaller dark gray and red breccias occur in the southeastern- and eastern-central sectors. Both show extensive hematitic alteration, and the red breccia contains highly irregular, altered, mm-scale fragments that may be glass particles.
Remarkable are findings of Lepidodendron and trace fossils in some strata of the inner ring revealed that in the crater Oasis are involves sandstones, siltstones and claystones of Carboniferous age. In the inner ring and interior depression, some breccia occurrences were noted. The prominent hills of the inner ring are capped by highly resistant, siliceous sandstones of the Cretaceous (?), whereas the surrounding flats are underlain by less resistant Carboniferous beds. A distinct quartz-pebble conglomerate horizon that allegedly marks the base of the Carboniferous occurs widespread throughout the structure.


A dyke nearby the Oasis structure

Crater field Oasis (prominent plugs in the north)

Bleached sandstone

Oasis ring dyke structure with central uplift

Crater inside .......

........ with Carboniferous layer: Bryozoa fossils and Ledidodendron plant imprint

According to UNDERWOOD & FISK (1980), about 6-8 km north and northeast of Oasis, a field of circular or rounded knobs of sandstone occur. These are 10-100 m in diameter and 10-50 m high. These authors suggested that the knobs might be linked to the crater-forming impact event. They described them as clastic plugs, apparently composed of Nubian sandstone, which had been emplaced by vertical flow of impact-fluidized sand. Our investigation indicated that in some cases they have a distinct chimney-like form with sandstone strata in the central areas having near-vertical bedding orientations. However, no evidence for fluidization of sand - as speculated by UNDERWOOD & FISK (1980) – was found. In contrast, several distinct ridges were recognized as erosional remnants of complex fold structures. The question whether or not this folding is related to the impact event, or reflects regional tectonic deformation, still remains open. It appears reasonable to interpret these plug-like structures as remnants of folds, of which the fold hinges have been completely eroded, leaving the vertically standing strata of the fold cores behind."

Remark: It is not sure, that the northern plugs in the centre contain vertical oriented sandstone layers. There also could be white Trachyte harden without development of the distinctive column-like structure.


Prominent plugs of Trachyte in the northern direction with erected layers at outside

                           Plug in the Jebel Babein

Plugs of Trachyte with fused layers in the northwestern direction of  Oasis structure
24° 45' N / 23° 52' E

In the foreground a fused conglomerate

4.3  Craters Arkenu


The JERS-1 radar mosaic reveals two circular structures partially hidden by Quaternary deposits. The radar scene then clearly reveals a double circular structure composed of a southwestern crater 10.3 km in diameter and a northeastern crater of diameter 6.8 km. The NE crater is composed of concentric inner and outer rings separated by a depression filled with sediments, also observed in the optical scene. The SW crater also presents a circular shape with possibly three concentric annular ridges. The host rock of the double circular structure is a cross-bedded coarse-grained to conglomeratic sandstone and  containing plant fossils and thin shale interbeds (Carboniferous ?).

First time, the team Philippe Paillou observed quantities of Shatter Cone structures on the site, all located close to the inner ridge of the NE crater. Large outcrops of allochthonous breccia could also be observed in both craters. He could find several quartz grains presenting planar fractures (PF's) in these breccia.

Di Martino et al. (2008)
reported about a field visit that they could not detect any shock deformation in quartz and reported that the shatter cones alleged by Paillou et al. were the result of wind erosion (ventifacts). They categorically stated that they could not find any evidence that would support an impact origin. According to Di Martino et al. the local geology involves Paleozoic sandstones and siltstones. The strata in the areas of the structures are impregnated by Fe-oxide minerals. In Arkenu 1, the sandstones are quite well preserved in the structure’s interior.
In Arkenu 2 they are disaggregated and contain massive magnetite deposits. The authors interpret the local geology as the result of partial ‘‘digestion of sandstones by a subvolcanic intrusive body (now partially outcropping within the crater area)’’. In Arkenu 2 they observed a first mafic hypabyssal phase, followed by granite that is locally preserved in the northern sector of this structure.
They concluded that these crater-like features could be the result of intrusion of two nearly cylindrical sub-volcanic pipes, which was accompanied by hydrothermal venting and dike injection.

Most recently, Cigolini et al. (2012) reported further evidence in support of a volcanic genesis of the Arkenu bodies from field and petrographic work. They did not observe shock metamorphic evidence in samples of sandstone from the Arkenu circular structures and also state clearly that the alleged shatter cones have an origin as wind-ablation features. They support the conclusion that the two features represent volcanic stocks and interpret their existence as a consequence of intrusion of syenitic porphyritic rocks into the sandstone formation. These volcanics are part of a ‘‘rather simple and eroded ring complex’’. They make a case for hydrothermal activity subsequent to volcanic intrusion, which deposited massive magnetite-hematite, coeval with the emplacement of silicified dikes in the environs. Finally, they observed ‘‘plugs of tephritic-phonolitic rocks and lamprophyres (monchiquites) inject into the sandstone along conjugate fracture zones.

Craters Arkenu:  Ark 1 position  22° 05' N / 23° 47' E

Centre of crater Arkenu-2

Subvolcanic structures at the western edge of Arkenu-2

Western edge of the structure Arkenu-2

Bleached white breccia

.........  at crater rim



Arkenu-1: Yellow Jasper in silicified sandstone - formed by hydrovolcanic solutions


Hardened breccia with not rounded fragments of basement material


Two small craters; 40 km WNW from the Arkenu structures


Crater southeast of Arkenu 2                                                                                                    (21° 57' 50' N/ 23° 46' 39'' E)

What's new:

C. Cigolini, M. Di Martino, M.Laiolo, D. Coppala, P. Rosetti, M. Morelli -- Meteoritics & Planetary Science 47, Nr 11, 1772–1788 (2012); doi: 10.1111/maps.12012

Field Observations
In the Arkenu 1 structure the sandstone cover is locally overlain by massive magnetite–hematite bodies, whereas in the Arkenu 2 area such bodies are sparse and limited to some sectors in the southern area. Rocks are essentially brownish porous medium to coarse-grained, occasionally fine-grained, moderately to poorly sorted sandstones with subrounded to subangular quartz and rarely sedimentary lithic fragments. Thin bedded siltsones underlie quartz-arenites.
In the north-central part of the Arkenu 1 structure, were found a decameter-sized body of syenite porphyry locally surrounded by meter-thick veins of similar composition. In some sectors of the structure’s floor these rocks may show a shell of argillic alteration.
At the contact with syenite intrusive veins, were found a brownish horizon of muscovite-rich fragmental feldspathic material (containing magnetite, apatite, barite, and Mn and Zn oxides) that is overlain by a massive magnetite–hematite unit with subhorizontal attitude and a thickness of several meters. This unit is mainly composed of massive magnetite (partially transformed to hematite and ⁄ or limonitic products), with abundant centimeter-sized cavities often lined with octahedral magnetite crystals that are vertically oriented.
In some places, in the eastern sector the contact between the sandstones and the overlying massive magnetite–hematite horizon is marked by a few-meters thick hydrovolcanic breccia. This breccia in places shows silicified syenite clasts embedded in apatite-rich veinlets. Pervasive hydrothermal alteration was observed at the bottom of the Arkenu 2 structure, in the central part of the southwestern sector, where a finegrained sandstone is strongly affected by argillic alteration and shows typically bleached white to gray color. Together with the findings at Arkenu 1, this strongly supports the idea that ‘‘paired’’ syenitic bodies may be present at depth.
At the inner rim of Arkenu 1, the magnetite–hematite horizons are covered by the above described porous sandstones, but this sedimentary unit is missing at the top of the mesas in the interior of the structures.
In the surroundings of both Arkenu 1 and Arkenu 2 were found silicified dikes that transect the sandstones. These dikes are essentially vertical at the surface but seem to follow a cone sheets geometry, at depth, that extend coaxially (for approximately 5 km) from the central axis of the circular structures. Within these circular features were found the presence of hypabyssal tephrite to phonolite and lamprophyric plugs (the latters may also outcrop outside the circular cone sheet area). In fact, these intrusive bodies inject the sandstone along conjugate fracture zones trending NE–SW (parallel with the orientation of the circular structures).

Petrography of Igneous Rocks
There are two types of syenite porphyries. They outcrop within the northeastern sector of the Arkenu 1 structure. Syenite of the first type is more peripheral and is proximal to the intrastructural massive magnetite bodies and shows a porphyritic texture consisting of large K-feldspar (sanidine with subordinated microcline) grains, up to 5 mm across and very rare albite at the rims of feldspar laths in a fine-grained feldspathic matrix. The rock has been subject to strong potassic alteration. Secondary phases are sericite, carbonate, ankerite, and Fe-Mn oxides. Sparse zircon, apatite, and rutile are accessory phases.
The second type is a quartz-bearing syenite porphyry with crystals of sanidine-microcline, albite, abundant microphertite, rare biotite flakes, and patches of acicular greenish amphibole (likely of the richteritearfedsonite series) locally altered to chlorite. Matrix minerals are of the same mineral phases with patches of granophyric intergrowths consisting of K-feldspar and quartz. Secondary minerals are sericite, Mg-chlorite, carbonate, ankerite, and Fe-Mn oxides (in veinlets). Zircon, apatite, rutile, allanite, opaques (Ti-magnetite and ilmenite) are accessory phases.
Tephrites-phonotephrite-tephriphonolites and phonolites are well represented in the Arkenu area. These rocks are found as necks and dikes that crosscut the sandstones in the areas surrounding both Arkenu structures.
Tephrites and related lavas (phonotephritetephriphonolites) show a porphyritic texture with laths (up to 2–3 mm across) of euhedral plagioclase (albiteoligoclase), subhedral amphibole (of the richteritearfedsonite series), microphenocrysts of nepheline and sanidine in a microgranular texture consisting of these same mineral phases. Additional matrix minerals are calcite and ankerite, apatite, Fe-Mn oxides. In more altered samples the amphibole is altered to chlorite; secondary K-feldspar replaces sodalite; secondary carbonate and ankerite are common and coexist with zeolites. Accessory minerals are zircon and apatite.
Only a single neck of phonolite has been observed in the area SE of Arkenu 1. It shows a porphyritic texture with sanidine macrophenocrysts (up to 5 mm across), phenocrysts of aegirine, and laths of subhedral phlogopite in a microfelsitic matrix of the same phases, nepheline and secondary zeolites, carbonates and opaques. Accessory phases are sparse zircon and apatite.
Lamprophyres are also well represented as plugs and subordinate dikes. They show a holocrystalline porphyritic texture of euhedral olivine (with 2 mm on average size) locally altered to iddingsite, euhedral to subhedral Ti-augite, kaersutitic amphibole, microphenocryts of nepheline, and late poikiolitic phlogopite (which locally overgrows iddingsitic alteration haloes around olivine), in a pilotaxitic to cryptofelsitic matrix consisting of these mineral phases plus abundant rutile, sparse apatite, and microgranular zircon. Secondary phases are zeolites in patches and analcime.

Quartz-arenitic silicified dyke produced by hydrovolcanic fluid circulation Phonolitic plug about 2 km from the SSE rim of Arkenu Hydrovolcanic altered breccia in altered syenite at the contact with magnetite bodies Muscovite-rich hornfels magnetite bodies Syenite apophysis with fragmental brownish gangue (upper contact) overlain by massive magnetite and vacuolar sandstone


M. Di Martino, C. Cigolini, L. Orti -

“The interpretation of Arkenu structures as impact-related is based on the observation of shatter cones and impact breccias with planar fractures in quartz grains."
"We visited the area on November 2007 and we carried out a preliminary geological and structural survey.”
“In fact, we did not observe PDF in the collected quartz grains and, in addition, the so called “shatter cones” (brought by Paillou and co-workers as an evidence of an impact event) have been likely produced by the erosion of sandstones. All of them, in fact, are oriented in the same direction of the dominant winds (we prefer to name these structures as “pseudo-shatter cones)".

Geological Survey: The rocks outcropping in the craters’ area are a variety of sandstones and subordinated siltstones. Sandstones on the top of the sequence that also outcrop within the craters, are coarser and carry abundant concretions of diagenetic hematite (millimeters to tens of centimeters in size). These sandstones are well preserved within the Arkenu 2. Conversely, within Arkenu 1 the floor consists essentially of disaggregated portions of these rocks coexisting with massive magnetite deposits. In this case, field evidence and mineral distribution (diagenetic hematite recrystallized as magnetite), suggests digestion of the above sandstones by a subvolcanic intrusive body (now partially outcropping within the crater area). The intrusion is characterized by a mafic precursor, followed by granite locally preserved in the northern sector of the crater. It is suggested that the mafic precursor contributed to the melting of the original sandstone sequence and was then followed by the injection of a granitic magma within the subvolcanic region.

Discussion: We, therefore, suggest the craters forming episode is the result of intrusion of a paired, nearly cylindrical subvolcanic stocks (coupled with ring dike injection in the surroundings) accompanied by hydrothermal degassing. This process was then followed by local structural adjustments, likely due to thermal contraction of the whole edifices along circular fractures. This produced moderate folding and subsidence of the “crater sectors” (currently delimited by the crater rims) as well as the origin of the outer circular structures. Erosion did its cycle and finally revealed the architecture we are now observing.


4.4 Hadid Structure

The Jebel Hadid Structure is located in southeast Libya (20°52'07"N / 22°42'15"E). It is made up of five concentric rings, the outermost of which is approximately 4.7 km across.
In 2009 a paper appeared in the journal Marine and Petroleum Geology in which M. Schmieder and E. Buchner of the Institut für Planetologie at Universität Stuttgart and D.P. Le Heron of Royal Holloway, University of London, propose that the Jabal Hadid structure is an impact structure.
This is an error. The structure fits in with the other subvolcanic structures in the region.

4.5 Dalma Structures

Further crater-like structures are located far north, at the terminus of the Howar-Uweinat Uplift, on the Jabal Dalma in Libya.

25.64320° / 22.78860° 26.21851° / 24°97064 26.20818° /24.79096°







Structural sample for the origin the Libyan craters Oasis and BP

The "impact" craters in Libya are comparably to the craters of the "Scarp-Contours" in Egypt (GKCF craters). We can see erected and tipped over sandstones and crushed breccia. The breccia contains differently material. Clear igneous material was only found in the Arkenu structures, because it has climbed probably rarely to the surface. There is ultimately no imperative proofs, that the craters have emerged by an impact. The kind of the planar lamelles point to a low pressure.

The breccia is formed by heat and contains also material from Paleozoic underground and the deeper basement. Microbreccia with shock-quartz fragments and pieces of sandstone, mixes with partially devitrified glass, all within a crystallized matrix, are no convincing proofs for an impact.

In the north direction of the crater Oasis are to be seen further structures, which can contain basaltic material
. In the northwest of the crater a clear evidence for intrusive material exist. The ring-shaped structures outside of the crater are dykes, on them are placed plugs.

All intrusive plugs, dykes and to it belong craters in the region have emerged probably at the same time in the Tertiary period. Them all become found at the Howar-Uweinat Uplift nearby of tectonic features and lineaments. This conspicuous cluster of crater-like structures may be related to a magmatic plume in the Earth's mantle. The activities evidently were joined with subvolcanic and hydrovolcanic processes, which could have led also to the origin of the unique Libyan Desert Glass.