sethoflagos

For some reason, I got booted into a UK secondary school while I was still 10, the youngest by more than a month of a yearly intake of 360 pupils. The school had a good sports record, and being the youngest and among the smallest, I found the first year tough. But year two, I still qualified for the under-12s among whom I was one of the biggest, and had had an extra year of training against stronger opponents. This advantage was nothing to do with me being a Libra as such; it was simply down to the school year beginning in September.

This works well for social housing schemes with, say, several hundred family apartments serviced by a communal centralised utilities facility. Lots of leverage here from economy of scale. Great for those who relish the thought of living in a scaled up termite mound. (Not knocking the idea as such. Just saying...)

Just for comparison, a primary steam power station will typically produce main steam at 165 barg and 570oC. This implies 230o of superheat. The intermediate cycle would be superheated to the same temperature, but at ~60 barg. Bear in mind that energy content is almost independent of pressure: it's all about the temperature. But that's dry saturated steam at 200oC which just happens to be industry standard for the drying sections of pulp and paper mills, a vital cog in the wheels of the Finnish economy. No one serious generates power from this quality of steam.

Duly duplicitously duplicated on the basis that 'too good' is synonymous with 'so consistently poor it almost works'.

Another artless, atrophied appendage to our awful anthology. A sonnet created by ChatGPT, written in the style of William McGonagall lamenting the appropriation of his own unique style by LLMs such as ChatGPT. A kind of recursive parody. How about Gordon Ramsay has a go at Haiku after an unfortunate Eggs Benedict

O Muse, thou’s fled, like mist o’er Tay’s cauld stream, And left me here wi’ rage that gars me greet; For iron brains, wi’ neither soul nor dream, Do grind out verse mair swift than mortal feet. O cruel age! O time o’ doom and dread! When clatterin’ gears outsing the poet’s cry; And I, puir wretch, by hunger near struck dead, Must watch yon soulless scribblers multiply. Their lines, though neat, are cauld as winter’s breath, Nae spark o’ heart, nae trembling human pain; Yet publishers proclaim my art is death, And cast me oot like midden in the rain. O William McGonagall, thy shade I loudly invoke, For I, like thee, am scorned—yet forced tae croak!

I get it that there is an inverse relation between temperature and electron speed through a logic gate, and that processor clock speeds are selected according (in part) to this constraint. Admittedly, I've not done any machine code programming since 1MHz was a fair clock rate, but Google's AI is telling me that current generation processors don't start clock speed temperature throttling until chip temperature reaches 90-100oC suggesting that ambient air cooling should be viable in any climate providing heat transfer efficiency is appropriately dealt with at cabinet, rack, circuit board, and chip level, as an integrated part of the design. Of course, if these aspects are not being adequately addressed by the manufacturers, then datacentres would be obliged to crudely dial down the temperature of their data hall ventilation and rely on diffusion to do the business. That's the compromise available, and I guess reality must lie somewhere between these extremes. Somewhere no doubt there will be a bunch of accountants making decisions on topics they are ill-equipped to comprehend.

I wish I'd had ChatGPT in my schooldays to help with my English Literature homework. Possibly not such a good idea for Biology.

Is it? My gear never sees a room temperature below 250C, even at night. The only unit that complains now and then is my old phone, but that's when the body is hand hot. Are you really sure that individual components are prone to failure at below say 45oC? Your 200C isn't just a recommended AC setting for a server room is it? These numbers make a huge difference to what is feasible in large scale installations. Actually, thinking about it, I can see why 'high and dry' might appeal. But that's based on an experience of condensation and trace sulphides being the main environmental causes of failures in electronic equipment.

Not that cheap even where environmental protection laws are lax. Lots of civil works on the intakes, buffer storage, and outfalls, and the water treatment costs (filtration, biological control, corrosion control etc.) are much higher than closed loop systems. From what I could glean from the Guardian article, (and referenced impact study), no one is seriously proposing this. I don''t disagree entirely. But the situation is more complex than this, particularly if @npts2020 's information regarding the temperature dump shortfall (ambient wet bulb > target temperature of 20oC) is correct. This would pretty much enforce some degree of refrigeration cycle in the mix. I've attached a manufacturer's semi-technical brochure to give some indication of the current state of play in datacentre cooling system architecture. (In principle, not so different to other modern sectors). The trend seems to be moving away from water based systems where feasible. Araner_Whitepaper_DataCenter.pdf

One for the Trekkies. Didn't know whether to laugh or cry most of the time.

Proudhon waives the rules

Orthogneisses and orthoschists are derived from igneous protoliths, while paragneisses and paraschists are derived from sedimentary protoliths. Remelting is not involved (except where gneiss is converted to migmatite). Is that matter of fact enough for you? Or do you intend to keep making up the basics as you go along? So has anything really changed due to AI other than the shear volume of people thinking they can chip in on topics they were previously oblivious of? And, of course, the ability to instantly translate a mundane report on cassava exports into the style of a Shakespearean regal proclamation. Its biggest plus in my book.

Still no. Drop the pettiness and read this instead. It explains why your fixation on superficial headrock age is misplaced. You're asking the wrong question. The answer lies deep in the basement. Mapping a hidden terrane boundary in the mantle lithosphere with lamprophyresArjan H. Dijkstra & Callum Hatch Nature Communications volume 9, Article number: 3770 (2018) Cite this article AbstractLamprophyres represent hydrous alkaline mantle melts that are a unique source of information about the composition of continental lithosphere. Throughout southwest Britain, post-Variscan lamprophyres are (ultra)potassic with strong incompatible element enrichments. Here we show that they form two distinct groups in terms of their Sr and Nd isotopic compositions, occurring on either side of a postulated, hitherto unrecognized terrane boundary. Lamprophyres emplaced north of the boundary fall on the mantle array with εNd −1 to +1.6. Those south of the boundary are enriched in radiogenic Sr, have initial εNd values of −0.3 to −3.5, and are isotopically indistinguishable from similar-aged lamprophyres in Armorican massifs in Europe. We conclude that an Armorican terrane was juxtaposed against Avalonia well before the closure of the Variscan oceans and the formation of Pangea. The giant Cornubian Tin-Tungsten Ore Province and associated batholith can be accounted for by the fertility of Armorican lower crust and mantle lithosphere. IntroductionWilson’s cycle1 of the opening and closing of ocean basins throughout Earth history was based on the similarity of Early Palaeozoic faunal assemblages in the Avalon Peninsula of Newfoundland and in Southern Britain, which were strikingly different from fauna of the same age in the rest of North America and in Northern Britain. These faunas had evolved on either side of a ‘Proto-Atlantic’ ocean. This eventually led to the notion of an ‘Avalonian terrane’, whose northern margin is represented by the Caledonian suture with Laurentia2. Subsequently, structural geology, palaeomagnetism and geochronology have been key among the many disciplines in Earth Sciences used to map out and trace the movements of the many tectonic terranes from which present and past continents were pieced together3,4,5,6,7,8,9. It is now clear that Avalonia is one of a collection of peri-Gondwana terranes, lithospheric fragments that rifted away from Gondwana and were accreted to Laurentia throughout the Early Paleozoic7,8,10,11. Their movements as independent terranes ended with the Variscan Orogeny and the formation of the supercontinent Pangea, complete by the Late Carboniferous. A key locality of Avalonia’s southern margin is southwest Britain, where Avalonia is juxtaposed against another peri-Gondwana terrane, Armorica. Early Paleozoic faunas in southern Britain differ from those in Brittany, France, showing that Avalonia and Armorica where separated by an intervening ocean basin, the Rheic Ocean, in Silurian-Devonian times2. The Lizard Ophiolite, exposed on the southernmost edge of Britain, is widely considered to be one of the best-preserved fragment of the Rheic Ocean and the locus of the suture12. Different terrane analysis approaches have shown that Avalonia can be traced back to a position next to South-American Gondwana, while Armorica originated closer to the African part of Gondwana3,5,13,14. There are, however, problems with the interpretation of the southern margin of Avalonia in Britain. Post-Variscan lamprophyre dykes found throughout Armorica have a strong subduction-type geochemical signature15,16, which is consistent with Armorica forming the overriding plate during the closure of the Rheic Ocean. However, identical igneous rocks in southwestern Britain—i.e., north of the Rheic suture—discussed in this paper, cannot be so easily explained if they are sited on the down-going Avalonian plate. Moreover, the Lizard Ophiolite has characteristics of a narrow Red Sea-like oceanic basin formed in a transtensional setting17,18 rather than of a full ocean basin formed at a mid-ocean ridge. Recent revisions of Variscan tectonics in Europe have highlighted the role of many small ocean basins19 and northward subduction of the Rheic Ocean and docking of Armorican terranes already in the Late Silurian, well before final closure of the other remaining oceanic basins in the Carboniferous9. If the Lizard Ophiolite was derived from one of these many small ocean basins, then it is possible that as yet unknown fragments of Armorica are present in southern Britain. Lamprophyres are relatively rare volcanic or subvolcanic rocks characterized by dark mica or amphibole as the main phenocryst phase in a feldspar-rich groundmass20. The generally primitive nature of lamprophyres combined with high potassium and water content suggests that they are derived from previously metasomatised—probably veined—continental mantle lithosphere20,21,22,23,24,25,26,27,28, and they are genetically linked to kimberlites, lamproites, carbonatites and ultramafic lamprophyres20,21. Therefore, they are a unique source of information about the composition of the deep parts of the continental lithosphere. Post-orogenic calc-alkaline lamprophyres are relatively abundant in the Variscan Orogen of western and central Europe15,16,28,29,30,31. In addition, at least 30 localities of lamprophyres and closely related igneous rocks are known in southwestern Britain32,33,34,35. The lamprophyres are mica-rich and typically form 10 cm to m-wide dykes and other types of minor intrusions cutting across Variscan foliations in Carboniferous and Devonian rocks. Lamprophyre magmatism occurred between 295 and 285 Ma, coinciding with the first pulse of granite magmatism in the region34. Similar-aged potassic lavas are also found in the area, intercalated with Early Permian clastic sediments in graben structures33. Despite being largely mica-free, these calc-alkaline high-K lavas have trace element compositions showing that they are related to the lamprophyres33,34,35. This paper offers a new, mantle-based perspective on the tectonic make-up of the Avalonian margin: we use the compositions of lamprophyres to map distinct chemical domains in the mantle lithosphere of southwest Britain, revealing the presence of a hitherto unrecognized Armorican terrane fragment that lies hidden beneath Paleozoic rocks. ResultsPetrographyThe chemical compositions of samples of lamprophyres and potassic lavas from 22 locations in southwest Britain are reported in this paper (Fig. 1; see supplementary figure 1 and supplementary table 1 for details about locations). Many of the localities are poorly exposed overgrown quarries, but a few localities (e.g., MAW, PEN, and CRA) provide well-exposed lamprophyres in contact with country rocks (supplementary figure 2a). Nd and Sr isotope systematics are also reported for a subset of samples to better constrain the composition of their mantle source. Chemical compositions are reported in supplementary data 1. Fig. 1 The alternative text for this image may have been generated using AI. Full size image Geospatial analysis of post-Variscan lamprophyre geochemistry in southwest Britain. Inset map shows location of study area, with the generally assumed location of the Rheic suture marked by the Lizard-Start ophiolites complex. a Map of the study area with sample localities. Samples marked with circles are minette-type lamprophyres, squares are kersantite lamprophyres, and diamonds are mica-free K-rich lavas. Samples are also colour-coded based on K2O/Na2O ratios. Orange samples are ultrapotassic (K2O/Na2O >2.2) and represent the lowest degree of mantle melting; yellow symbols are potassic (1 < K2O/Na2O <2.2) and green symbols represent samples with K2O/Na2O <1. Two dashed contour lines delineate areas in north and south where deepest-derived magmas were emplaced, based on N-MORB normalized Dy/Yb ratios >2. b Chart showing negative correlation between depth and degree of melting. c Initial Sr and Nd isotope ratios calculated at 290 Ma plotted against northing (Ordnance Survey UK grid coordinates), showing a clear jump in values across thick dashed line. d Map showing the samples assigned to group 1 (red circles) and group 2 (blue squares) based on their initial Sr and Nd isotope ratios. Surface trace of the boundary between the two isotopically distinct lithospheric mantle domains is interpreted as a cryptic terrane boundary in the mantle lithosphere buried beneath Paleozoic metasedimentary rocks. SPL refers to the Start-Perranporth Line (see text). Data for locations TOW (Towan Head), HOB (Holywell Beach), TRE (Trelissick), HEL (Helfort) and FRE (Fremington Quay) are from ref 35. (only Nd data); all other data from this study. Locations are listed in Supplementary Table 1. Map adapted from regional view geological map from British Geological Survey59. © Crown Copyright and Database Right 2018. Ordnance Survey (Digimap Licence) The majority of samples are minettes consisting of phenocrysts of dark mica with <5% altered olivine phenocrysts in a finer-grained groundmass of feldspar, predominantly alkali-feldspar, mica, apatite and quartz. The mica phenocrysts generally consist of pale phlogopite cores with dark biotite rims (supplementary figure 2b). Two samples (CRA and LUR) are kersantites, containing dark mica in a plagioclase-dominant groundmass; the kersantites also contain relatively abundant chlorite. Habits of pseudomorphs after olivine are often blade-shaped or skeletal (supplementary figure 2c, d) in the lamprophyres. Many samples contain igneous carbonate (supplementary figure 2e). Most of the lamprophyres contain round mm-sized quartz xenocrysts (supplementary figure 2c), but other xenolithic material is uncommon. Some samples contain small autolithic inclusions of phlogopite-rich cumulate (supplementary figure 2f). Some dark mica phenocrysts have textures that seem reminiscent of sieve textures in their core, overgrown by contiguous rims of phlogopite grading outwards to biotite (supplementary figure 2b); these are interpreted here as remelted antecrysts or xenocrysts. Olivine is always strongly altered to carbonate or to serpentine; this is interpreted as largely due to autometasomatism20 as a result of the high volatile content of the magmas, as completely altered olivine is found in otherwise completely fresh lamprophyres. Some clinopyroxene is found in rims around xenoliths of quartz-rich sediments. Two lamprophyric samples are vesiculated (WAS and HOL) and have an aphanitic groundmass, resembling lamprophyric lavas. Four samples of mica-free high-K lavas (DUN, KNO, POS and POC) are also included in the study. These lavas contain (altered) olivine and plagioclase phenocrysts in an aphanitic K-feldspar-rich groundmass. Based on petrographic analysis, samples with predominantly clear, non-clouded feldspars, with primary carbonates and with clearly zoned micas with a pale centre and darker but clear pleochroic rim resembling biotite, are deemed ‘fresh’ in our study (e.g., supplementary figure 2b, e, f). Other samples are moderately altered, containing feldspars with cloudy patches, generally darker micas showing development of opaque rims and inclusions (e.g., supplementary figure 2c, d). Strongly altered lamprophyres are not included in our study, but K-rich basaltic lavas generally show significant alteration, with feldspars strongly altered to secondary saussurite assemblages, and with formation of abundant opaque phases. Chemical compositionsThe lamprophyres studied here are typical calc-alkaline lamprophyres: they generally have intermediate compositions (SiO2 = 51–57%), high alkali and volatile content, and strong enrichments in large ion lithophile trace elements (LILE) when normalized to normal mid-ocean ridge basalt36 (Fig. 2). The minette-type lamprophyres are highly potassic (K2O/Na2O >1), and approximately half of the samples are classified as ultrapotassic (K2O/Na2O > 2.2). The value of 2.2 instead of 2.0 is chosen as the lower limit, as these samples form a coherent group in the K2O–SiO2 diagram in supplementary figures 3a, b. Fig. 2 The alternative text for this image may have been generated using AI. Full size image Extended trace element spidergrams for selected samples. Shown are six of the least altered lamprophyres, and three potassic calc-alkaline lavas, with concentrations normalized to normal mid-ocean ridge basalt (N-MORB). Diagrams show the enrichment in incompatible elements and the steep slope of the heavy rare earth elements The relatively high SiO2 and high alkali contents are coupled with primitive magma characteristics such as the presence of (altered) olivine phenocrysts, high bulk mg-numbers (mg# = molar Mg/(Mg + Fe) up to 0.73) and high Ni and Cr (typically 100–200 and 150–600 ppm, respectively, supplementary figure 3c,d). The skeletal nature of the olivine observed in several samples excludes a xenocrystic origin. These primitive characteristics rule out an origin of the parental magmas by extensive crustal contamination, and they are regarded as near-primary mantle melts. Experiments show that in a hydrous mantle source, pyroxene makes a relatively large contribution to the partial melting reaction compared to olivine, leading to relatively SiO2-rich (52–64 wt% SiO2) primary magmas37. The lamprophyres are strongly enriched in incompatible elements, but depleted in Nb and Ti compared to other incompatible elements, and depleted in the heaviest rare earth elements (REE) Er to Lu compared to normal mid-ocean ridge basalt (N-MORB) (Fig. 2). A relatively deep origin for the parental magmas is confirmed by the steep heavy REE (HREE) slopes (Yb/Dy normalized to N-MORB fall in the range 1.5–2.6), generally interpreted as the signature of residual garnet in the source38. This indicates a depth of origin >60–85 km38, with the highest ratios indicating a source close to the base of the lithosphere at the time, assumed to be at least similar to the present-day depth of the lithosphere–asthenosphere boundary of 100–125 km in southern Britain39. Sr and Nd isotopesWhile lamprophyres from across the study area are broadly similar in mineralogy, texture and bulk major and trace element composition, their Nd and Sr isotopic compositions fall into two clearly distinguishable groups (Fig. 3). One group of samples of lamprophyres exhibit initial isotopic compositions that coincide with the mantle array line between Bulk Silicate Earth and Depleted Mantle for 290 Ma, with initial εNd values of −1 to +1.6. The potassic lavas studied also fall in this group; their Nd isotopic signature shows that they formed from lithospheric magmas closely related to the lamprophyres, and that they do not have a petrogenetic affinity with shoshonitic arc magmas26. The second group of samples shows a displacement off the mantle array line to higher, more radiogenic initial 87Sr/86Sr ratios, with negative initial εNd values (−0.3 to −3.5). Fig. 3 The alternative text for this image may have been generated using AI. Full size image Initial Sr–Nd isotopic compositions of magmas from southwest Britain at 290 Ma. Group 1 samples (red circles) fall on the mantle array, whereas group 2 samples (blue squares) are systematically displaced to more radiogenic Sr isotopic values. Isotopic compositions for similar-aged lamprophyres from Armorican massifs in Europe (locations in Fig. 5; published data15,16) are shown for comparison (grey diamonds: lamprophyres from various Armorican massifs and the Massif Central in France; filled grey circles: lamprophyres from the Vosges mountains and the Black Forest). Group 2 lamprophyres from southwest Britain are isotopically identical to lamprophyres from Armorica. Green circle marks the composition of a 380 Ma olivine dolerite dyke from Coverack in the Lizard Ophiolite (LIZ380) analysed alongside the lamprophyres. DM depleted mantle, CHUR chrondritic uniform reservoir (Nd), UR uniform reservoir (Sr) DiscussionThe alkali and light REE (LREE) concentrations are used here as a proxy for the overall degree of melting in the mantle source: in a metasomatised source, mineral assemblages in mineral pockets or vein assemblages rich in LILE, LREE and volatiles have lower solidus temperatures compared to ambient mantle peridotite and will be the dominant contribution to a mantle melt at very low degrees of melting, whereas typical depleted mantle wall rocks will contribute progressively more to the magma as melting progresses23,25. Due to the continuous breakdown of hydrous minerals in the mantle during the melting, water is continuously available and the source remains fusible and can produce up to 20% melt37. In southwest Britain, ultrapotassic lamprophyres occur to the north and south of a central area of slightly elevated degrees of mantle melting that yielded potassic lamprophyres and lavas with 1 < K2O/Na2O < 2.2 (Fig. 1a). One lava (DUN) in this area of elevated melting is a high-K calc-alkaline basalt with K2O = 2.1 wt% and K2O/Na2O = 0.7, representing the highest degree of melting. Similarly, the HREE slope Yb/Dy (garnet signature38) is taken as an indication of the relative depth of the source of the magma. There is an inverse correlation between degree and depth of melting in the area, with the most alkaline and LREE-enriched samples having the deepest origin (Fig. 1b). The mantle domain that experienced the shallowest and highest degree of post-orogenic, Early Permian mantle melting thus mapped out (Fig. 1a, b) underlies a region of Carboniferous sedimentation (the Culm basin); this pattern is most easily explained as an area of localized lithospheric thinning causing low-degree decompression melting driven by Early Permian post-Variscan extension. The coincidence with the Carboniferous sedimentary basin suggests that the formation of this ‘lithospheric neck’ was already initiated during an Early Carboniferous phase of intra-plate extension. Group 2 lamprophyres plot off the mantle array for 290 Ma towards more radiogenic Sr isotopic ratios, coupled with mildly lower εNd values. Alteration can be ruled out as a cause for this radiogenic Sr enrichment, as this group includes several very fresh samples (PEN, MAW and LEM). We investigated whether the radiogenic Sr isotopic compositions of group 2 samples can be explained by contamination of mantle-derived lamprophyric magmas with crustal material during the emplacement of the lamprophyres. Supplementary figure 4 shows the results of a test consisting of three mixing models between a typical group 1 lamprophyre magma (composition of KIL6) with three different contaminants. None of the models shown can plausibly explain the composition of group 2 lamprophyres by a contamination and assimilation process, as they require in excess of 35% crustal contaminant. Such high degrees of assimilation are wholly inconsistent with the primitive nature of many of the lamprophyres. Instead, the isotopic composition must reflect the mantle source. Rather than being exceptional, post-orogenic lamprophyres with radiogenic Sr isotope ratios are the norm in the Variscan belt of Europe, and have been recorded as far east as Poland29. In many recent studies, such Sr isotopic compositions in lamprophyres were interpreted as reflecting the isotopic signature of old subducted sediments in the mantle source, imparted by fluids derived from a subducting slab just before or during lamprophyre emplacement event15,16,31,40. Below we argue, however, that this signature in the mantle source of group 2 lamprophyres of southwest Britain may be the result of older, possibly Neoproterozoic–Cambrian metasomatism. A significant discovery of this study is the spatial distribution of isotopic groups 1 and 2 lamprophyres: group 1 lamprophyres are only found in the north of the area while group 2 lamprophyres are only found in the south (Fig. 1c, d). The linear character and the perfect separation suggest that there is a steep boundary in the mantle lithosphere of southwest Britain. The strong Sr and Nd isotopic contrast between the domains on either side clearly indicates a long-term compositional difference and provides strong evidence for the presence of an ancient (Lower Paleozoic) steep terrane boundary that was hitherto unrecognized. A geochemical study using lamprophyres showed a clear Nd isotopic contrast in the mantle on either side of the well-exposed lithospheric-scale Great Glen Fault in Scotland41. The mapped mantle boundary in southwest Britain is, however, cryptic and does not have an obvious tectonic surface expression. It is parallel to several steep east–west faults recognized as having caused sedimentary basin segmentation in the Devonian sequences42 of which one, the Start-Perranporth Line (SPL, Fig. 1d), was previously proposed as a crustal terrane boundary43. It is proposed here that these faults in the crust are near-surface splays of the much deeper lithospheric-scale transcurrent fault mapped here by lamprophyre isotopic compositions. The terrane boundary is overlain by the Carboniferous Culm Basin, and its surface trace is apparently ‘stitched’ by the Early Permian Dartmoor granite intrusion. Significant facies differences between Devonian sedimentary sequences on either side44 are permissive of completion of terrane juxtaposition as late as the Middle or Late Devonian, but more likely represent the control of basement faults related to reactivation of the terrane boundary. The absence of obvious unconformities in the Devonian sedimentary successions44,45 suggests that the terrane boundary was formed not later than the Early Devonian. This seems to be broadly coeval with the postulated soft collision between the Armorican-derived terranes and Avalonia further in north-central Europe at the end of the Silurian9. The enrichment in radiogenic Sr of group 2 lamprophyres, interpreted as a subducted sediment signature, is absent in group 1 lamprophyres, which otherwise exhibit the same evidence for extensive potassic and volatile metasomatism in their mantle source. This suggests that the radiogenic Sr enrichment and the potassic metasomatism are two separate events. The former event is only found in the southern terrane and predates the terrane juxtaposition, while the latter affected the whole region, and thus postdates the terrane boundary (and is an ‘overlap assemblage’ in terrane analysis terminology). In this case, the radiogenic Sr signature is not due to subduction of old sediment during lamprophyre emplacement15,16,31,40, but resulted from partial melting of mantle lithosphere that had been modified by metasomatism in the past, prior to the terrane juxtaposition. The metasomatism probably involved sediment-derived fluids and formation of mica-peridotites. The lamprophyres of the southern terrane exhibiting the radiogenic Sr isotope signature are isotopically indistinguishable from similar-aged lamprophyres in Armorican massifs in Europe (Fig. 3). Given that the radiogenic Sr enrichment is so prevalent in the source of post-Variscan lamprophyres throughout Europe, the likely geological context for this event is the Cadomian Orogeny. This period of accretionary mountain-building at the active margin of Gondwana during the late Neoproterozoic to Cambrian has affected all major pre-Variscan continental blocks in Armorican Europe, which have otherwise disparate older histories14,46. The more widespread potassic-hydrous metasomatism that overprinted the terrane boundary can most easily be explained as having occurred above a north-dipping slab during Variscan subduction of oceanic lithosphere, although Late Devonian-Early Carboniferous alkaline intra-plate magmatism in the region47 is not fully discounted here as a contributing cause of the metasomatism. Seismic imaging of steep lithosphere-scale continental strike-slip zones in the mantle remains inherently difficult48,49, and the lack of sharp Moho off-sets on major continental strike-slip zones is often explained by a distributed nature of the deformation in the lower crust and mantle50,51. This study shows that geochemical mapping of terrane boundaries using post-orogenic, lithosphere-derived igneous rocks such as lamprophyres can be a powerful complement to traditional geophysical methods. Our geochemical mapping of the base of the mantle lithosphere (>60–85 km) of southwest Britain has revealed the presence of a narrowly defined terrane boundary with an apparent width <20 km, with the terranes of either side having distinct isotopic compositions (Fig. 4). The terrane boundary can be tentatively correlated with a system of major transcurrent faults in Europe (Fig. 5). Fig. 4 The alternative text for this image may have been generated using AI. Full size image Schematic north–south cross-section showing the terrane boundary around the time of emplacement of the lamprophyres (c. 290 Ma), after the Variscan Orogeny. Armorican mantle lithosphere in yellow with characteristic high 87Sr/86Sr is juxtaposed against Avalonian mantle lithosphere in blue. Both domains had been affected by potassic-hydrous metasomatism (orange veins in basal part of the lithosphere), possibly above a (north-dipping?) subduction zone. These metasomatised mantle rocks formed the source for the lamprophyres on both sides. Deepest-derived lamprophyric magmas are formed on either side of a central area of thinned lithosphere. Dashed lines in lower crust denote inferred basement faults which controlled the segmentation of the Devonian sedimentary basins and which were re-activated as thrusts during the Variscan Orogeny. Upper crustal rocks (after published cross-section42) mainly comprised of Devonian and Carboniferous sedimentary rocks were probably deposited after terrane juxtaposition and are shown in grey Fig. 5 The alternative text for this image may have been generated using AI. Full size image Location of the newly recognized terrane boundary in its wider tectonic context. Other major faults including the Bray fault and its previously proposed extension (dashed) in Britain45. Symbols show locations of the Armorican lamprophyres for which isotopic compositions are shown in Fig. 3 (using the same symbols). Pre-Variscan Massifs: AM Armorican Massif, MC Massif Central, IB Iberia, VM Vosges Mountains, BF Black Forest, RM Rhenish Massif. Map adapted from published tectonic map45 Critically, since the lamprophyres of the southern terrane are isotopically indistinguishable from similar-aged lamprophyres in Armorican massifs in Europe, we conclude that the newly recognized terrane boundary juxtaposed Armorican mantle in the south against Avalonian mantle in the north. The implications of this conclusion are manifold. The southern margin of Avalonia in Britain is not defined by a single collisional suture, but instead by one or more steep transcurrent45 terrane boundaries. The ‘suture’ defined by the Lizard Ophiolite is instead a structure related to the closure of a minor tract of the Rheic Ocean (Fig. 4). This is fully consistent with recent interpretations of the Lizard Ophiolite in a relatively small transtensional ocean basin17. Docking of Armorican fragments started well before the peak of the Variscan Orogeny, and the terrane juxtaposition in southwest Britain cannot be assigned unambiguously to either the Caledonian or the Variscan Orogeny. Ultimately, this shows that in Britain, just like in North America11 and in Northern Europe9,52, the closure of Wilson’s (1966) ‘Proto-Atlantic Ocean’ consisted of a protracted history of accretion of terranes, rather than two (Caledonian and Variscan) punctuated collisions events. Finally, the post-Variscan giant Cornubian Sn-W orefield and the associated peraluminous granitic batholith of southwest Britain53 are superimposed on the Armorican terrane, and the general absence of mineralized veins north of the terrane boundary is striking (Fig. 6). Similar mineralization associated with peraluminous granitoids can be found throughout the Armorican massifs of Europe, most notably in the giant Erzgebirge Ore Province54,55,56. This shows that the Armorican lower crust generally had the right composition (e.g., metagreywacke54) to produce the Sn-W-rich peraluminous granitic magmas, as opposed to the crust of the Avalonian terrane. The lamprophyre magmas transferred fluids as well as heat-producing elements (K and Th) from the metasomatised lithospheric mantle to the crust, and thus probably played a significant role in crustal melting and formation of the mineral resources. Fig. 6 The alternative text for this image may have been generated using AI. Full size image The distribution of mineral veins in southwest Britain and the location of the giant Cornubian W-Sn orefield. Estimated resource sizes (contained metal Sn and W in kilo-tonnes of reserves and resources) of the main ore districts recognized in the region are indicated by open circles (diameter proportional to resource size), after published data56. Also shown is the active world-class Hemerdon W-Sn mine. Mineral veins from 1:50,000 digital data set (DigimapGB-50) from British Geological Survey. Map adapted from regional view geological map from British Geological Survey59. © Crown Copyright and Database Right 2018. Ordnance Survey (Digimap Licence) ... or just watch this, which leads up to and discusses the above.

For 2 metres lift (~20% of atmospheric pressure), wouldn't you need a diurnual absolute temperature swing of ~20%, ie ~60 K. A bit optimistic for a system without collection mirrors perhaps. And then there's the problem of vacuum collapse of the vessel. It may have to be located at or below the input liquid level to maintain a positive hoop stress.

That would be a Weber 32 DFM NLA IIRC E car? Now get a hot-rolled Dellorto, Hateg won race!

It's lit and the knob is at maximum. Maybe 200o C ish(?). No fan.

Makes sense. When I work out the ratios, my standard (Delia) loaf actually calls for a higher water content (43.7% as against 42.8% for the sourdough). The latter just feels a lot wetter which suggests it's something to do with the fermentation process. I've been baking it in a loaf tin rather the recommended casserole dish, and I'm not even sure my oven will do gas mk 9. Probably, need to experiment and risk the odd burnt offering.

Last week I had a blob of chapati dough start to ferment on me, so I grasped the opportunity to try my hand at making sourdough bread roughly in accordance with: Good FoodWhite sourdoughMaster the art of how to make sourdough bread with our step-by-step recipe. Learn how to create a starter, levain and the loaf itself with our expert tips.I've just sampled my second loaf (bit of crust lightly spread with bacon drip) and can definitely declare it to be edible. Few questions: The recipe I'm using seems to involve an awful lot of faffing about. Is this all absolutely necessary? I've already upped the baking time from 35 to 45 minutes (at gas mark Nigeria). The crust isn't burning, but it is well crisp, and yet the heart of it is still definitely on the moist and claggy side. Is this how it is supposed to be? The starter is very lively in my kitchen conditions, so rather than throw half of it away as instructed (wasteful), I'm using 200 g of starter as the levain. Is this a mortal sin? The dough is a lot wetter than I'm used to. Is this normal? I'm using approximately half quantities as I'm not exactly feeding the village here. Though it does seem to keep a lot better than my 'normal' 1 lb loaf.

I think you are asking the AI a loaded question: a presupposition that either unit has a narrowly definable age that can be compared. Compare your results with those of my reworded version. Significant improvement, yes? Then we have to do the filtering. Le plus ça change, la plus c'est la même chose.

Ultimately, we all have to commit to some significant level of trust in some foundational reference material. For me, it was the likes of Rogers & Mayhew Steam Tables and a small group of similar. I wouldn't say the trust was absolute, but it was necessary in order to function effectively in the workplace.

Perhaps one of the mods could perform the surgical extraction?

It's a life lesson. What you get out of it is a direct function of the quality and quantity of effort you put into it. Some will learn this and adapt accordingly. Others not so much. ...or how old are the electrons that define your external form? Yes, the recent development in interpreting naturally parsed queries is useful, but there's still no substitute for filtering out the dross by using carefully selected, specific keywords as we learned with Webcrawler etc many moons ago. Nothing beats picking keywords that only appear in the sources you're interested in and nothing else. (Try 'aerobates' for example) However, with the more selective searched I do seem to be receiving the following or similar with increasing frequency: Switching my VPN location usually clears it, but it's still irritating.

I've just checked my ancient copy of the Stainer & Barrett Dictionary of Musical Terms. For sesquialtera it has: 1) Numbers in the proportion 3:2 2) An organ stop consisting of several ranks of pipes, sounding high harmonics for the purpose of strengthening the ground tone. My money would be on this being accomplished via sum-and-difference tones, specifically the latter. Now that IS a subject worth arguing about.

I shall endeavour to remember that when @TheVat speaks, this is what is meant. But what of the looser speech of others? I'm more than comfortable with 'mixed meter'. But some clearly do consider America to be a hemiola rhythm, and whoever last authored the Wikipedia entry doesn't even seem to know what classic sequential hemiola is anyway. In the words of our esteemed leader ''Forget it, Jake - it's Crackpot Town". It's not science, so it's just not worth stressing out over the strictest of definitions. Few will take any notice. My own understanding is probably based on an exercise for the hemiola in Arban's Complete Method for Cornet, which consisted solely of alternating duplets and triplets repeated indefinitely. Or at least until the pattern was imprinted forever in my marrow.