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26-578: The Arfon Group is a stratigraphically defined geological group of rocks that are present in the Cymru Terrane around Bangor in North Wales , United Kingdom . The group contains volcanogenic conglomeratic sandstone, fine-grained tuffite and tuffaceous sediment . This Precambrian volcano-sedimentary group incorporates over 4000 m of deposits and were previously considered to be of Cambrian age. Uranium–lead (U–Pb) isotope ratio data suggests that

52-474: A U-Pb zircon from the lower part of the succession as 614+/-2Ma and 604.7+/-1.6Ma confirms a Neoproterozoic age. These strata have an angular and discordant relationship with both formations having variable thickness controlled by bounding fault lines that are likely to have controlled the depositional regime of the rocks. The formations exist to the west of the Aber Dinlle Fault. The Minfordd Formation

78-622: A bounded half-graben (or graben ). Isotope data shows a zircon from the lower part of the succession as having a U–Pb isotope date of 614±2 Ma and 604.7±1.6 Ma and as such confirms a Neoproterozoic age. Cymru Terrane The Proterozoic rocks of the Cymru Terrane are typified in North Wales by the Arfon Group , Sarn Complex and the Twt Hill Granite . The former

104-408: A period of erosion or non-deposition. Disconformities are marked by features of subaerial erosion. This type of erosion can leave channels and paleosols in the rock record. A nonconformity exists between sedimentary rocks and metamorphic or igneous rocks when the sedimentary rock lies above and was deposited on the pre-existing and eroded metamorphic or igneous rock. Namely, if the rock below

130-565: A proximal source. This outcrops mainly on Anglesey but a sliver of it also occurs along the Berw Fault and its properties are similar to that of the Arfon Group ash-flow tuff and as such constrain the docking of the western Monian Composite Terrane . Although evidence can be interpreted to the contrary as the Bwlch Gwyn outcrop may be faulted post-Berw and pre-Arenig. The Bryn-teg borehole

156-420: A region or were subsequently eroded before the next deposition. The local record for that time interval is missing and geologists must use other clues to discover that part of the geologic history of that area. The interval of geologic time not represented is called a hiatus . It is a kind of relative dating . A disconformity is an unconformity between parallel layers of sedimentary rocks which represents

182-486: Is a sandstone dominated epiclastic and tuffaceous lithology which has a broad upward fining sequence with the presence of thick welded and non-welded ash-flow tuffs that elucidates an amount of volcanism. The basal rocks of the Minfordd Formation contain clasts of granite , vein quartz , quartzitic sandstone, quartzose schists and were thought to be Cambrian basal conglomerate . The Bangor Formation overlies

208-691: Is in the Bangor area (S & SW) with the latter two located on the Llyn Peninsula . The St Davids Granophyre and the Pebidian Supergroup are located on the coastline of St Davids Peninsula. Inferred Proterozoic volcanic deposits are noted in the Bryn-Teg Borehole ( Trawsfynydd , Gwynedd ). The Padarn Tuff , which is thought to be contemporaneous with the Sarn Complex , is unconformable with

234-468: Is interbedded basic lavas and acid tuffs , is cut by the St David's Granophyre. There is evidence presented that subaerial and subaqueous deposition has occurred in a Welsh Basin that is likely to have been undergoing varying rates of subsidence thus promoting aerial emergence. Greenschist alteration is in keeping with the regional metamorphism that is characteristic of Welsh Neoproterozoic rocks. In

260-663: Is located near Trawsfynydd in the Harlech Dome and exhibits over 140 m of Neoproterozoic rocks. There is a sharp erosional contact with the Cambrian Dolwen Formation . No Ediacaran fauna has been found in the Welsh Terrane to date. The age of the Bryn-teg Volcanic Formation is constrained by Lower Cambrian foraminifera in overlying beds. The Playsolenites cooperi are only otherwise known in

286-469: Is noted to exhibit a volcanic arc signature. Correlation of the granophyric intrusion with the Arfon Group rather than the nearby Coomb Volcanic Formation has been suggested with a tentative U-Pb isotopic age of 625+/-25Ma being suggested. The largest plutonic body in the terrane has limited outcrop and is sheared by the Llyn Shear Zone in the west and covered by later ( Arenig ) sediments to

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312-507: Is presented by the Briançonnais realm (Swiss and French Prealps) during the Jurassic. Angular unconformities can occur in ash fall layers of pyroclastic rock deposited by volcanoes during explosive eruptions . In these cases, the hiatus in deposition represented by the unconformity may be geologically very short – hours, days or weeks. A paraconformity is a type of unconformity in which

338-605: The Llyn Shear Zone . This is conjectured to be one of two probabilities, either as an exotic sliver, or as a metamorphic slice from the Monian Composite Terrane. The Granitoid Gneiss has Sm-Nd ages of 1350 Ma which is in the same temporal region as the Sarn Granite In the southwest of Wales is the St Davids Granophyre the stratigraphical relationship of which was subject of heated debates towards

364-553: The sedimentary geologic record . The significance of angular unconformity (see below) was shown by James Hutton , who found examples of Hutton's Unconformity at Jedburgh in 1787 and at Siccar Point in Berwickshire in 1788, both in Scotland. The rocks above an unconformity are younger than the rocks beneath (unless the sequence has been overturned). An unconformity represents time during which no sediments were preserved in

390-616: The Minfordd Formation and it underlies the Llanberis Slates and is a similar lithology to the Minfordd Formation excepting the basal conglomerate. This is thought to be the lateral equivalent of the Bangor and Minfordd Formations on the eastern side of the Aber Dinelle Fault. The Fachwen and Bangor Formations are both dominated by acidic volcanic deposits but they also contain minor basic tuffs that preserve scoria textures which suggest

416-600: The Pebidian Supergroup in the Precambrian. The issue was finally resolved by Green by revealing, in an excavation, an unconformity in which an excavation of a Cambrian basal conglomerate is shown to cut the granophyre. The St David's Granophyre has historically been incorrectly assigned to be alaskite or trondhjemite due to low concentrations of potassium feldspar but this has been shown to be an alteration product from its original calc-alkaline granite which

442-601: The Pebidian Supergroup the basal unit is largely basaltic and exhibits columnar jointing , auto brecciated lavas, scoriaceous and fine grained tuffs. The volcano-sediments have an increased acid component until the uppermost beds of the unit exhibit the basaltic influence once again. Such information is preserved in the Rhosson Group as autobrecciated lava, tuffs and scoria deposits. This volcano-sedimentary group incorporates over 4000m of deposits and were previously considered to be of Cambrian age. U-Pb data suggests that

468-461: The Placentian of SE Newfoundland. Unconformity An unconformity is a buried erosional or non-depositional surface separating two rock masses or strata of different ages, indicating that sediment deposition was not continuous. In general, the older layer was exposed to erosion for an interval of time before deposition of the younger layer, but the term is used to describe any break in

494-438: The break is igneous or has lost its bedding due to metamorphism, then the plane of juncture is a nonconformity. An angular unconformity is an unconformity where horizontally parallel strata of sedimentary rock are deposited on tilted and eroded layers, producing an angular discordance with the overlying horizontal layers. The whole sequence may later be deformed and tilted by further orogenic activity. A typical case history

520-444: The east. Altered to Greenschist facies the pluton contains a bimodal suite of gabbro - diorite , monzogranite (Sarn Granite) and granodiorite . The Sarn Granite is leucocratic and covers an expanse of c.6 km^2 in contrast to the gabbro and diorite that exist as small and scattered exposures. The dioritic component has been confirmed as having a Neoproterozoic age of 614Ma+/-2Ma using U-Pb Zircon dating. So therefore,

546-643: The end of the 19th Century predominantly between Sir Archibald Geikie and Henry Hicks . Geikie (then director of the Geological Survey) insisted upon the Pebidian Supergroup and the high-level intrusion being placed in the Cambrian sequence with Hicks taking the opposing view and suggesting that the Granophyre which cross cuts the Pebidian Supergroup should be placed in the Precambrian and by consequence placing

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572-551: The overlying Fachwen Formation and the unconformity has been constrained with dates noted of 604.7 Ma+/-1.6Ma from the tuffs and 572.5 Ma+/-1.2Ma from the Fachwen Formation. Information on the basement is somewhat sparse with no zircons noted to be older than 617 to 638 Ma. However, there are outcrops of the Parwyd Gneiss which are retrogressed granitoid gneiss and garnet amphibolite that occur with

598-400: The sedimentary layers above and below the unconformity are parallel, but there is no obvious erosional break between them. A break in sedimentation is indicated, for example, by fossil evidence. It is also called nondepositional unconformity or pseudoconformity. Short paraconformities are called diastems . A buttress unconformity also known as onlap unconformity, occurs when younger bedding

624-831: The shearing of the Llyn is also temporally constrained by the date. This is a small fine-grained, leucocratic intrusive body that cuts the Padarn Tuff at the western end of the Bangor-Caernarfon Ridge. The thick sequences of volcano-sedimentary facies are present in North Wales (as the Arfon Group) and South Wales (as the Pebidian Supergroup) and are generally considered to be coeval but are geochemically distinct, showing acidic and basic qualities respectively. Both are cut by minor granitic intrusions. The Pebidian Supergroup

650-442: The whole succession is indeed Precambrian Neoproterozoic age. Exposure of the lower unit ( Padarn Tuff ) is exhibited on a ridge between Bangor and Caernarfon and also on a ridge near Llyn Padarn This is noted to be a thick sequence of acid ash flow tuffs and exhibits welding and are thought to be rapid deposition of thin air-fall tuffs and rhyolite flows placed in a bounded half-graben (or graben ) . Isotope data shows

676-462: The whole succession is indeed Precambrian Neoproterozoic age. Exposure of the lower unit ( Padarn Tuff ) is exhibited on a ridge between Bangor and Caernarfon (both located in North Wales) and also on a ridge near Llyn Padarn . This is noted to be a thick sequence of acid ash flow tuffs and exhibits welding and are thought to be rapid deposition of thin air-fall tuffs and rhyolite flows placed in

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