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Timing of post-orogenic silicic volcanism in the eastern part of the European Variscides: constraints from SHRIMP U–Pb zircon study of the Permo-Carboniferous Góry Suche Rhyolitic Tuffs (the Intra-Sudetic Basin) | International Journal of Earth Sciences
<!DOCTYPE html> <html lang="en" class="no-js"> <head> <meta charset="UTF-8"> <meta http-equiv="X-UA-Compatible" content="IE=edge"> <meta name="applicable-device" content="pc,mobile"> <meta name="viewport" content="width=device-width, initial-scale=1"> <meta name="robots" content="max-image-preview:large"> <meta name="access" content="Yes"> <meta name="360-site-verification" content="1268d79b5e96aecf3ff2a7dac04ad990" /> <title>Timing of post-orogenic silicic volcanism in the eastern part of the European Variscides: constraints from SHRIMP U–Pb zircon study of the Permo-Carboniferous Góry Suche Rhyolitic Tuffs (the Intra-Sudetic Basin) | International Journal of Earth Sciences</title> <meta name="twitter:site" content="@SpringerLink"/> <meta name="twitter:card" content="summary_large_image"/> <meta name="twitter:image:alt" content="Content cover image"/> <meta name="twitter:title" content="Timing of post-orogenic silicic volcanism in the eastern part of the European Variscides: constraints from SHRIMP U–Pb zircon study of the Permo-Carboniferous Góry Suche Rhyolitic Tuffs (the Intra-Sudetic Basin)"/> <meta name="twitter:description" content="International Journal of Earth Sciences - The Góry Suche Rhyolitic Tuffs in the Intra-Sudetic Basin, in the eastern part of the Variscan Belt of Europe, represent a voluminous (ca. 100 km3),..."/> <meta name="twitter:image" content="https://static-content.springer.com/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Figa_HTML.png"/> <meta name="journal_id" content="531"/> <meta name="dc.title" content="Timing of post-orogenic silicic volcanism in the eastern part of the European Variscides: constraints from SHRIMP U–Pb zircon study of the Permo-Carboniferous Góry Suche Rhyolitic Tuffs (the Intra-Sudetic Basin)"/> <meta name="dc.source" content="International Journal of Earth Sciences 2024"/> <meta name="dc.format" content="text/html"/> <meta name="dc.publisher" content="Springer"/> <meta name="dc.date" content="2024-11-01"/> <meta name="dc.type" content="OriginalPaper"/> <meta name="dc.language" content="En"/> <meta name="dc.copyright" content="2024 The Author(s)"/> <meta name="dc.rights" content="2024 The Author(s)"/> <meta name="dc.rightsAgent" content="journalpermissions@springernature.com"/> <meta name="dc.description" content="The Góry Suche Rhyolitic Tuffs in the Intra-Sudetic Basin, in the eastern part of the Variscan Belt of Europe, represent a voluminous (ca. 100 km3), possibly caldera-related, ignimbrite-dominated complex and the Łomnica Rhyolites are associated, post-ignimbrite sills. Zircon separates from nine samples were dated using the U–Pb SHRIMP method. Well-defined concordia ages were determined in four ignimbrite samples (300.5 ± 2.0, 300.5 ± 1.4, 298.0 ± 1.6 and 297.2 ± 0.9&nbsp;Ma) and in two rhyolite samples (298.4 ± 1.5 and 292.6 ± 1.9&nbsp;Ma). Clustering of the ignimbrite sample ages between 300.5 ± 2.0 and 297.2 ± 0.9&nbsp;Ma and geological evidence indicate the eruption and deposition of the tuffs close to the Carboniferous/Permian boundary, in a geologically rapid event at approximately 299 Ma. Zircon assemblages in three tuff specimens are strongly dominated by xenocrysts of various Palaeozoic and Precambrian ages that were incorporated during the eruption through the basin fill. The emplacement of the tuffs was followed (and partly overlapped?) by the emplacement of the Łomnica Rhyolites as sills in two episodes in the early Permian. The Góry Suche Rhyolitic Tuffs may be a few million years older than assumed so far, and this, as well as rather imprecise biostratigraphic constraints from the host sedimentary rocks, suggest a need for revision of the existing lithostratigraphic and evolutionary schemes for the Permo-Carboniferous of the Intra-Sudetic Basin. The studied tuffs and rhyolites together with coeval granitic plutons in vicinity can be linked to the onset of post-Carboniferous lithospheric thinning in Central Europe."/> <meta name="prism.issn" content="1437-3262"/> <meta name="prism.publicationName" content="International Journal of Earth Sciences"/> <meta name="prism.publicationDate" content="2024-11-01"/> <meta name="prism.section" content="OriginalPaper"/> <meta name="prism.startingPage" content="1"/> <meta name="prism.endingPage" content="24"/> <meta name="prism.copyright" content="2024 The Author(s)"/> <meta name="prism.rightsAgent" content="journalpermissions@springernature.com"/> <meta name="prism.url" content="https://link.springer.com/article/10.1007/s00531-024-02474-y"/> <meta name="prism.doi" content="doi:10.1007/s00531-024-02474-y"/> <meta name="citation_pdf_url" content="https://link.springer.com/content/pdf/10.1007/s00531-024-02474-y.pdf"/> <meta name="citation_fulltext_html_url" content="https://link.springer.com/article/10.1007/s00531-024-02474-y"/> <meta name="citation_journal_title" content="International Journal of Earth Sciences"/> <meta name="citation_journal_abbrev" content="Int J Earth Sci (Geol Rundsch)"/> <meta name="citation_publisher" content="Springer Berlin Heidelberg"/> <meta name="citation_issn" content="1437-3262"/> <meta name="citation_title" content="Timing of post-orogenic silicic volcanism in the eastern part of the European Variscides: constraints from SHRIMP U–Pb zircon study of the Permo-Carboniferous Góry Suche Rhyolitic Tuffs (the Intra-Sudetic Basin)"/> <meta name="citation_online_date" content="2024/11/01"/> <meta name="citation_firstpage" content="1"/> <meta name="citation_lastpage" content="24"/> <meta name="citation_article_type" content="Original Paper"/> <meta name="citation_fulltext_world_readable" content=""/> <meta name="citation_language" content="en"/> <meta name="dc.identifier" content="doi:10.1007/s00531-024-02474-y"/> <meta name="DOI" content="10.1007/s00531-024-02474-y"/> <meta name="size" content="284578"/> <meta name="citation_doi" content="10.1007/s00531-024-02474-y"/> <meta name="citation_springer_api_url" content="http://api.springer.com/xmldata/jats?q=doi:10.1007/s00531-024-02474-y&api_key="/> <meta name="description" content="The Góry Suche Rhyolitic Tuffs in the Intra-Sudetic Basin, in the eastern part of the Variscan Belt of Europe, represent a voluminous (ca. 100 km3), p"/> <meta name="dc.creator" content="Awdankiewicz, Marek"/> <meta name="dc.creator" content="Pańczyk, Magdalena"/> <meta name="dc.creator" content="Ploch, Izabela"/> <meta name="dc.creator" content="Raczyński, Paweł"/> <meta name="dc.creator" content="Awdankiewicz, Honorata"/> <meta name="dc.creator" content="Górecka-Nowak, Anna"/> <meta name="dc.creator" content="Pawlak, Wojciech"/> <meta name="dc.creator" content="Peryt, Tadeusz"/> <meta name="dc.subject" content="Geology"/> <meta name="dc.subject" content="Geophysics/Geodesy"/> <meta name="dc.subject" content="Sedimentology"/> <meta name="dc.subject" content="Structural Geology"/> <meta name="dc.subject" content="Mineral Resources"/> <meta name="dc.subject" content="Geochemistry"/> <meta name="citation_reference" content="citation_journal_title=Geol Mag; 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Zircon separates from nine samples were dated using the U–Pb SHRIMP method. Well-defined concordia ages were determined in four ignimbrite samples (300.5 ± 2.0, 300.5 ± 1.4, 298.0 ± 1.6 and 297.2 ± 0.9 Ma) and in two rhyolite samples (298.4 ± 1.5 and 292.6 ± 1.9 Ma). Clustering of the ignimbrite sample ages between 300.5 ± 2.0 and 297.2 ± 0.9 Ma and geological evidence indicate the eruption and deposition of the tuffs close to the Carboniferous/Permian boundary, in a geologically rapid event at approximately 299 Ma. Zircon assemblages in three tuff specimens are strongly dominated by xenocrysts of various Palaeozoic and Precambrian ages that were incorporated during the eruption through the basin fill. The emplacement of the tuffs was followed (and partly overlapped?) by the emplacement of the Łomnica Rhyolites as sills in two episodes in the early Permian. The Góry Suche Rhyolitic Tuffs may be a few million years older than assumed so far, and this, as well as rather imprecise biostratigraphic constraints from the host sedimentary rocks, suggest a need for revision of the existing lithostratigraphic and evolutionary schemes for the Permo-Carboniferous of the Intra-Sudetic Basin. The studied tuffs and rhyolites together with coeval granitic plutons in vicinity can be linked to the onset of post-Carboniferous lithospheric thinning in Central Europe. 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Zircon separates from nine samples were dated using the U–Pb SHRIMP method. Well-defined concordia ages were determined in four ignimbrite samples (300.5 ± 2.0, 300.5 ± 1.4, 298.0 ± 1.6 and 297.2 ± 0.9 Ma) and in two rhyolite samples (298.4 ± 1.5 and 292.6 ± 1.9 Ma). Clustering of the ignimbrite sample ages between 300.5 ± 2.0 and 297.2 ± 0.9 Ma and geological evidence indicate the eruption and deposition of the tuffs close to the Carboniferous/Permian boundary, in a geologically rapid event at approximately 299 Ma. Zircon assemblages in three tuff specimens are strongly dominated by xenocrysts of various Palaeozoic and Precambrian ages that were incorporated during the eruption through the basin fill. The emplacement of the tuffs was followed (and partly overlapped?) by the emplacement of the Łomnica Rhyolites as sills in two episodes in the early Permian. The Góry Suche Rhyolitic Tuffs may be a few million years older than assumed so far, and this, as well as rather imprecise biostratigraphic constraints from the host sedimentary rocks, suggest a need for revision of the existing lithostratigraphic and evolutionary schemes for the Permo-Carboniferous of the Intra-Sudetic Basin. 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class="c-context-bar__container u-container"> <div class="c-context-bar__title"> Timing of post-orogenic silicic volcanism in the eastern part of the European Variscides: constraints from SHRIMP U–Pb zircon study of the Permo-Carboniferous Góry Suche Rhyolitic Tuffs (the Intra-Sudetic Basin) </div> <div data-test="inCoD" data-track-context="sticky banner"> <div class="c-pdf-container"> <div class="c-pdf-download u-clear-both u-mb-16"> <a href="/content/pdf/10.1007/s00531-024-02474-y.pdf" class="u-button u-button--full-width u-button--primary u-justify-content-space-between c-pdf-download__link" data-article-pdf="true" data-readcube-pdf-url="true" data-test="pdf-link" data-draft-ignore="true" data-track="content_download" data-track-type="article pdf download" data-track-action="download pdf" data-track-label="button" data-track-external download> <span class="c-pdf-download__text">Download PDF</span> <svg aria-hidden="true" focusable="false" width="16" height="16" class="u-icon"><use 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class="c-article-section__content" id="Abs1-content"><p>The Góry Suche Rhyolitic Tuffs in the Intra-Sudetic Basin, in the eastern part of the Variscan Belt of Europe, represent a voluminous (ca. 100 km<sup>3</sup>), possibly caldera-related, ignimbrite-dominated complex and the Łomnica Rhyolites are associated, post-ignimbrite sills. Zircon separates from nine samples were dated using the U–Pb SHRIMP method. Well-defined concordia ages were determined in four ignimbrite samples (300.5 ± 2.0, 300.5 ± 1.4, 298.0 ± 1.6 and 297.2 ± 0.9 Ma) and in two rhyolite samples (298.4 ± 1.5 and 292.6 ± 1.9 Ma). Clustering of the ignimbrite sample ages between 300.5 ± 2.0 and 297.2 ± 0.9 Ma and geological evidence indicate the eruption and deposition of the tuffs close to the Carboniferous/Permian boundary, in a geologically rapid event at approximately 299 Ma. Zircon assemblages in three tuff specimens are strongly dominated by xenocrysts of various Palaeozoic and Precambrian ages that were incorporated during the eruption through the basin fill. The emplacement of the tuffs was followed (and partly overlapped?) by the emplacement of the Łomnica Rhyolites as sills in two episodes in the early Permian. The Góry Suche Rhyolitic Tuffs may be a few million years older than assumed so far, and this, as well as rather imprecise biostratigraphic constraints from the host sedimentary rocks, suggest a need for revision of the existing lithostratigraphic and evolutionary schemes for the Permo-Carboniferous of the Intra-Sudetic Basin. The studied tuffs and rhyolites together with coeval granitic plutons in vicinity can be linked to the onset of post-Carboniferous lithospheric thinning in Central Europe.</p><h3 class="c-article__sub-heading" data-test="abstract-sub-heading">Graphical abstract</h3><div class="c-article-section__figure" data-test="figure" data-container-section="figure"><figure><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Figa_HTML.png?as=webp"><img src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Figa_HTML.png" alt="" loading="lazy" width="685" height="302"></picture></div></div></figure></div></div></div></section> <div data-test="cobranding-download"> </div> <section aria-labelledby="inline-recommendations" data-title="Inline Recommendations" class="c-article-recommendations" data-track-component="inline-recommendations"> <h3 class="c-article-recommendations-title" id="inline-recommendations">Similar content being viewed by others</h3> <div class="c-article-recommendations-list"> <div class="c-article-recommendations-list__item"> <article class="c-article-recommendations-card" itemscope itemtype="http://schema.org/ScholarlyArticle"> <div class="c-article-recommendations-card__img"><img src="https://media.springernature.com/w215h120/springer-static/image/art%3A10.1007%2Fs41513-018-0076-0/MediaObjects/41513_2018_76_Fig1_HTML.png" loading="lazy" alt=""></div> <div class="c-article-recommendations-card__main"> <h3 class="c-article-recommendations-card__heading" itemprop="name headline"> <a class="c-article-recommendations-card__link" itemprop="url" href="https://link.springer.com/10.1007/s41513-018-0076-0?fromPaywallRec=false" data-track="select_recommendations_1" data-track-context="inline recommendations" data-track-action="click recommendations inline - 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3" data-track-label="10.1007/s00531-020-01956-z">Calc-alkaline volcanic rocks and zircon ages of the late Tonian: early Cryogenian arc-related Big Naryn Complex in the Eastern Djetim-Too Range, Middle Tianshan block, Kyrgyzstan </a> </h3> <div class="c-article-meta-recommendations" data-test="recommendation-info"> <span class="c-article-meta-recommendations__item-type">Article</span> <span class="c-article-meta-recommendations__access-type">Open access</span> <span class="c-article-meta-recommendations__date">24 November 2020</span> </div> </div> </article> </div> </div> </section> <script> window.dataLayer = window.dataLayer || []; window.dataLayer.push({ recommendations: { recommender: 'semantic', model: 'specter', policy_id: 'NA', timestamp: 1732621287, embedded_user: 'null' } }); </script> <div class="app-card-service" data-test="article-checklist-banner"> <div> <a class="app-card-service__link" data-track="click_presubmission_checklist" data-track-context="article page top of reading companion" data-track-category="pre-submission-checklist" data-track-action="clicked article page checklist banner test 2 old version" data-track-label="link" href="https://beta.springernature.com/pre-submission?journalId=531" data-test="article-checklist-banner-link"> <span class="app-card-service__link-text">Use our pre-submission checklist</span> <svg class="app-card-service__link-icon" aria-hidden="true" focusable="false"><use xlink:href="#icon-eds-i-arrow-right-small"></use></svg> </a> <p class="app-card-service__description">Avoid common mistakes on your manuscript.</p> </div> <div class="app-card-service__icon-container"> <svg class="app-card-service__icon" aria-hidden="true" focusable="false"> <use xlink:href="#icon-eds-i-clipboard-check-medium"></use> </svg> </div> </div> <div class="main-content"> <section data-title="Introduction"><div class="c-article-section" id="Sec1-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="Sec1">Introduction</h2><div class="c-article-section__content" id="Sec1-content"><p>Silicic ignimbrite, caldera-related eruptions (e.g., Wilson <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2008" title="Wilson CJN (2008) Supereruptions and supervolcanoes: processes and products. Elements 4:29–34" href="/article/10.1007/s00531-024-02474-y#ref-CR105" id="ref-link-section-d17672574e449">2008</a>; Giordano and Cas <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2021" title="Giordano G, Cas RAF (2021) Classification of ignimbrites and their eruptions. Earth Sci Rev 220:103697" href="/article/10.1007/s00531-024-02474-y#ref-CR36" id="ref-link-section-d17672574e452">2021</a>) are amongst the largest and most significant volcanic events on Earth in terms of erupted magma volumes (up to 1000 km<sup>3</sup>), the size of resulting volcanic structures (collapse calderas tens of km in diameter surrounded by extensive ignimbrite shields) and environmental impacts (global climate changes). However, the large caldera-forming ignimbrite eruptions, the magma volumes of which exceeds a 100 km<sup>3</sup>, are relatively rare phenomena that (fortunately) did not occur in historic times and have not been witnessed by volcanologists. Thus, the knowledge on such events is based on the studies of recent small-volume equivalents, as well as studies of the larger ignimbrites preserved in older volcanic successions. Detailed studies of the latter, however, often prove difficult due to tectonics, erosion, redeposition, diagenesis that modify the primary distribution and thickness of original deposits and obliterate their primary composition and textures (e.g., Hencz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2024" title="Hencz M, Biró T, Németh K, Szakács A, Portnyagin M, Cseri Z, Pécskay Z, Szabó C, Müller S, Karátson D (2024) Lithostratigraphy of the ignimbrite-dominated Miocene Bükk Foreland Volcanic Area (Central Europe). J Volcanol Geoth Res 445:107960" href="/article/10.1007/s00531-024-02474-y#ref-CR41" id="ref-link-section-d17672574e459">2024</a>). Amongst the key problems in such studies are also the long term evolution of caldera systems and the timing of magmatic processes involved (van Zalinge et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="van Zalinge ME, Mark DF, Sparks RSJ, Tremblay MM, Keller CB, Cooper FJ, Rust A (2022) Timescales for pluton growth, magma-chamber formation and super-eruptions. Nature 608:87–92" href="/article/10.1007/s00531-024-02474-y#ref-CR99" id="ref-link-section-d17672574e463">2022</a>). Large caldera systems may remain active for a few millions of years (Cas and Wright <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1987" title="Cas RAF, Wright JV (1987) Volcanic successions: modern and ancient: a geological approach to processes, products and successions. Allen and Unwin" href="/article/10.1007/s00531-024-02474-y#ref-CR24" id="ref-link-section-d17672574e466">1987</a>), whereas the eruption and emplacement of even largest-volume ignimbrites are geologically instantaneous events the main phases of which last days to hours only (Wilson <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2008" title="Wilson CJN (2008) Supereruptions and supervolcanoes: processes and products. Elements 4:29–34" href="/article/10.1007/s00531-024-02474-y#ref-CR105" id="ref-link-section-d17672574e469">2008</a>). These contrasting timescales contribute to challenges in detailed studies and interpretations of ancient ignimbrites.</p><p>Intense volcanism, including the emplacement of widespread rhyolitic ignimbrites, affected large areas of Europe in late Palaeozoic times. This activity can be linked to the development of a silicic large igneous province in that region at Carboniferous-Permian transition, marked by a magmatic flare-up at ca. 300 Ma (Breitkreuz and Kennedy <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999" title="Breitkreuz C, Kennedy A (1999) Magmatic flare-up at the Carboniferous/Permian boundary in the NE German Basin revealed by SHRIMP zircon ages. Tectonophysics 302:307–326" href="/article/10.1007/s00531-024-02474-y#ref-CR21" id="ref-link-section-d17672574e475">1999</a>; Paulick and Breitkreuz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2005" title="Paulick H, Breitkreuz C (2005) The Late Paleozoic felsic lava-dominated large igneous province in northeast Germany: volcanic facies analysis based on drill cores. Int J Earth Sci (Geologische Rundschau) 94(5):834–850" href="/article/10.1007/s00531-024-02474-y#ref-CR77" id="ref-link-section-d17672574e478">2005</a>; Breitkreuz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2007" title="Breitkreuz C, Kennedy A, Geißler M, Ehling B-C, Kopp J, Muszynski A, Protas A, Stouge S (2007) Far Eastern Avalonia: its chronostratigraphic structure revealed by SHRIMP zircon ages from Upper Carboniferous to Lower Permian volcanic rocks (drill cores from Germany, Poland and Denmark). Geol Soc Am Spec Pap 423:173–190" href="/article/10.1007/s00531-024-02474-y#ref-CR22" id="ref-link-section-d17672574e481">2007</a>). Considering even wider distribution of the volcanic rocks towards north-western Africa, the activity of a mantle superplume beneath the centre of Pangea has been suggested (Doblas et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1998" title="Doblas M, Oyarzun R, Lopez-Ruiz J, Cebriá JM, Youbi N, Mahecha V, Lago M, Pocoví A, Cabanis B (1998) Permo-Carboniferous volcanism in Europe and northwest Africa: a superplume exhaust valve in the centre of Pangaea? J Afr Earth Sci 26(1):89–99" href="/article/10.1007/s00531-024-02474-y#ref-CR28" id="ref-link-section-d17672574e484">1998</a>). In the present Central Europe area this volcanism occurred in an evolving late- to post-orogenic, extensional continental setting, on top of decaying Variscan orogeny and in its foreland (Wilson et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Wilson M, Neumann E-R, Davies GR, Timmerman MJ, Heermans M, Larsen BT (eds) (2004) Permo-Carboniferous magmatism and rifting in Europe. Geological Society, London, Special Publications, p 223" href="/article/10.1007/s00531-024-02474-y#ref-CR106" id="ref-link-section-d17672574e487">2004</a>; McCann et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2006" title="McCann T, Pascal C, Timmerman M, Krzywiec P, López-Gómez J, Wetzel L, Krawczyk CM, Rieke H, Lamarche J (2006) Post-Variscan (end Carboniferous—Early Permian) basin evolution in Western and Central Europe. In: Gee DG, Stephenson RA (eds) European lithosphere dynamics, vol 32. Geological Society, London, Memoirs, pp 355–388" href="/article/10.1007/s00531-024-02474-y#ref-CR64" id="ref-link-section-d17672574e491">2006</a>). A characteristic type of activity recognised in this region were ignimbrite supereruptions exceeding 1000 km<sup>3</sup> in volume from calderas up to ca. 40 km in diameter (e.g., the Ora ignimbrite, Willcock et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2013" title="Willcock MAW, Cas RAF, Giordano G, Morelli C (2013) The eruption, pyroclastic flow behaviour, and caldera in-filling processes of the extremely large volume (>1290 km3), intra- to extra-caldera, Permian Ora (Ignimbrite) Formation, Southern Alps, Italy. J Volcanol Geotherm Res 265:102–126" href="/article/10.1007/s00531-024-02474-y#ref-CR102" id="ref-link-section-d17672574e496">2013</a>; Wurzen ignimbrite, Repstock et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="Repstock A, Casas-García R, Zeug M, Breitkreuz C, Schulz B, Gevorgyan H, Heuer F, Gilbricht S, Lapp M (2022) The monotonous intermediate magma system of the Permian Wurzen caldera, Germany: Magma dynamics and petrogenetic constraints for a supereruption. J Volcanol Geoth Res 429:107596" href="/article/10.1007/s00531-024-02474-y#ref-CR82" id="ref-link-section-d17672574e499">2022</a>), as well as several smaller-scale events (e.g., Tharandt Forest Caldera and ignimbrites, Breitkreuz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2021" title="Breitkreuz C, Käßner A, Tichomirowa M, Lapp M, Huang S, Stanek K (2021) The Late Carboniferous deeply eroded Tharandt Forest caldera–Niederbobritzsch granite complex: a post-Variscan long-lived magmatic system in central Europe. Int J Earth Sci 110:1265–1292" href="/article/10.1007/s00531-024-02474-y#ref-CR20" id="ref-link-section-d17672574e502">2021</a>; Altenberg-Teplice Caldera and rhyolites, Tomek et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="Tomek F, Opluštil S, Svojtka M, Špillar V, Rapprich V, Míková J (2022) Altenberg-Teplice Caldera sourced Westphalian fall tuffs in the central and western Bohemian Carboniferous basins (eastern Variscan belt). Int Geol Rev 64:441–468" href="/article/10.1007/s00531-024-02474-y#ref-CR94" id="ref-link-section-d17672574e505">2022</a>). The Permo-Carboniferous volcanic successions in the Variscan foreland, although thickest and widely distributed, are largely covered by thick accumulations of younger deposits and recognised by hydrocarbon exploration drilling (Benek et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1996" title="Benek R, Kramer W, McCann T, Scheck M, Negendank JFW, Korich D, Huebscher HD, Bayer U (1996) Permo-Carboniferous magmatism of the Northeast German Basin. Tectonophysics 266:379–404" href="/article/10.1007/s00531-024-02474-y#ref-CR13" id="ref-link-section-d17672574e509">1996</a>; Breitkreuz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2007" title="Breitkreuz C, Kennedy A, Geißler M, Ehling B-C, Kopp J, Muszynski A, Protas A, Stouge S (2007) Far Eastern Avalonia: its chronostratigraphic structure revealed by SHRIMP zircon ages from Upper Carboniferous to Lower Permian volcanic rocks (drill cores from Germany, Poland and Denmark). Geol Soc Am Spec Pap 423:173–190" href="/article/10.1007/s00531-024-02474-y#ref-CR22" id="ref-link-section-d17672574e512">2007</a>; Peryt et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2010" title="Peryt TM, Geluk MC, Mathiesen A, Paul J, Smith K (2010) Zechstein. In: Doornenbal JC, Stevenson AG (eds) Petroleum geological atlas of the Southern Permian Basin area. EAGE Publications b.v., pp 123–147" href="/article/10.1007/s00531-024-02474-y#ref-CR79" id="ref-link-section-d17672574e515">2010</a>). However, equivalent deposits crop out in post-Variscan intramontane basins further south, such as the Intra-Sudetic Basin (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e518">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e521">b</a>) at the NE margin of the Bohemian Massif (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig1">1</a>).</p><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-1" data-title="Fig. 1"><figure><figcaption><b id="Fig1" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 1</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/1" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig1_HTML.jpg?as=webp"><img aria-describedby="Fig1" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig1_HTML.jpg" alt="figure 1" loading="lazy" width="685" height="411"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-1-desc"><p>Location of study area in the Variscan Belt and the Bohemian Massif. Green colour—crystalline massifs, yellow—other rock complexes. Zones of the Variscan orogeny: RH Rhenohercynian, ST Saxothuringian, TB Tepla–Barrandian, MO Moldanubian, MS Moravo–Silesian (modified from Mazur et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2006" title="Mazur S, Aleksandrowski P, Kryza R, Oberc-Dziedzic T (2006) The Variscan Orogen in Poland. Geol Q 50:89–118" href="/article/10.1007/s00531-024-02474-y#ref-CR61" id="ref-link-section-d17672574e538">2006</a>)</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/1" data-track-dest="link:Figure1 Full size image" aria-label="Full size image figure 1" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><p>The subject of this study are the Góry Suche Rhyolitic Tuffs (GSRT), ignimbrite-dominated deposits with volume of ca. 100 km<sup>3</sup> and associated subvolcanic rhyolites. Their emplacement marked the climax of volcanism in the Intra-Sudetic Basin correlated with the early Permian based on bio- and lithostratigraphic constraints (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e554">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e557">b</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Awdankiewicz M (2004) Sedimentation, volcanism and subvolcanic intrusions in a late Palaeozoic intramonatne trough (the Intra-Sudetic Basin, SW Poland). Geol Soc Lond Spec Publ 234:5–11" href="/article/10.1007/s00531-024-02474-y#ref-CR5" id="ref-link-section-d17672574e560">2004</a> and references cited there). However, preliminary SHRIMP U–Pb zircon dating (Awdankiewicz and Kryza <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2010" title="Awdankiewicz M, Kryza R (2010) The Góry Suche Rhyolitic Tuffs (Intra-Sudetic Basin, SW Poland): preliminary SHRIMP zircon age. Mineral Spec Pap 37:70" href="/article/10.1007/s00531-024-02474-y#ref-CR9" id="ref-link-section-d17672574e563">2010</a>; Awdankiewicz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2011" title="Awdankiewicz H, Awdankiewicz M, Kryza R (2011) Abundant xenocrystic zircon and rare juvenile zircon in rhyolitic ignimbrites: preliminary SHRIMP data from the Lower Permian of the Intra-Sudetic Basin (SW Poland). Mineral Spec Pap 38:69–70" href="/article/10.1007/s00531-024-02474-y#ref-CR2" id="ref-link-section-d17672574e567">2011</a>)suggested surprisingly old emplacement age of the Góry Suche ignimbrites of ca. 300 ± 4, up to 10 My older than considered before. In this paper we present the results of more extensive SHRIMP U–Pb geochronological study of these tuffs and rhyolites, based on nine samples. We discuss the emplacement age of these volcanic units, the duration of this silicic volcanism and the significance of zircon xenocryst ages. These results contribute to the discussion on the stratigraphic correlation of Permo-Carboniferous succession and evolution of the Intra-Sudetic Basin, one of the largest intramontane troughs in Central Europe. Comparison with other ignimbrite caldera systems and granitic plutons in adjacent areas puts further constraints on the significance of voluminous rhyolitic volcanism in the eastern part of the Permo-Carbonifeorus silicic large igneous province of Europe.</p></div></div></section><section data-title="Geological setting"><div class="c-article-section" id="Sec2-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="Sec2">Geological setting</h2><div class="c-article-section__content" id="Sec2-content"><h3 class="c-article__sub-heading" id="Sec3">The Intra-Sudetic Basin – regional context, evolution, Permo-Carboniferus volcanism</h3><p>The Bohemian Massif is one of the largest outcrops of pre-Mesozoic basement in Central Europe (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig1">1</a>). The study area of this paper is situated in the NE part of the Massif, in the Sudetes mountains, where a “mosaic” of several tectonostratigraphic units built up of Neoproterozoic—Palaeozoic metasedimentary and metaigneous rocks crops out. These units were variably metamorphosed, deformed and tectonically juxtaposed in the Late Devonian to the Early Carboniferous times, during the Variscan orogeny (cf. Mazur et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2006" title="Mazur S, Aleksandrowski P, Kryza R, Oberc-Dziedzic T (2006) The Variscan Orogen in Poland. Geol Q 50:89–118" href="/article/10.1007/s00531-024-02474-y#ref-CR61" id="ref-link-section-d17672574e585">2006</a>). A characteristic feature of the region are the NW-trending Elbe, Intra-Sudetic and Odra strike-slip fault zones, along which the Variscan orogenic belt has been affected by wrench tectonics (Mazur et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2020" title="Mazur S, Aleksandrowski P, Gągała Ł, Krzywiec P, Żaba J, Gaidzik K, Sikora R (2020) Late Palaeozoic strike-slip tectonics versus oroclinal bending at the SW outskirts of Baltica: case of the Variscan belt’s eastern end in Poland. Int J Earth Sci (Geologische Rundschau) 109:1133–1160" href="/article/10.1007/s00531-024-02474-y#ref-CR63" id="ref-link-section-d17672574e588">2020</a> and references therein). The Variscan orogenic processes were accompanied and followed by intense granitic plutonism (e.g., Kryza et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2014" title="Kryza R, Pin C, Oberc-Dziedzic T, Crowley QG, Larionov A (2014) Deciphering the geochronology of a large granitoid pluton (Karkonosze Granite, SW Poland): an assessment of U–Pb zircon SIMS and Rb–Sr whole-rock dates relative to U–Pb zircon CA-ID-TIMS. Int Geol Rev 56:756–782" href="/article/10.1007/s00531-024-02474-y#ref-CR50" id="ref-link-section-d17672574e591">2014</a>; Turniak et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2014" title="Turniak K, Mazur S, Domańska-Siuda J, Szuszkiewicz A (2014) SHRIMP U-Pb zircon dating for granitoids from the Strzegom-Sobótka Massif, SW Poland: constraints on the initial time of Permo-Mesozoic lithosphere thinning beneath Central Europe. Lithos 208–209:415–429" href="/article/10.1007/s00531-024-02474-y#ref-CR96" id="ref-link-section-d17672574e594">2014</a>; Oberc-Dziedzic et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2015" title="Oberc-Dziedzic T, Kryza R, Pin C (2015) Variscan granitoids related to shear zones and faults: examples from the Central Sudetes (Bohemian Massif) and the Middle Odra Fault Zone. Int J Earth Sci 104:1139–1166" href="/article/10.1007/s00531-024-02474-y#ref-CR72" id="ref-link-section-d17672574e598">2015</a>) as well as the development of intracontinental basins with accumulation of thick volcano-sedimentary successions (Baranowski et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1990" title="Baranowski Z, Haydukiewicz A, Kryza R, Lorenc S, Muszyński A, Dolecki A, Urbanek Z (1990) Outline of the geology of the Góry Kaczawskie (Sudetes, Poland). Neues Jb Geol Paläontol Abh 179:223–257" href="/article/10.1007/s00531-024-02474-y#ref-CR12" id="ref-link-section-d17672574e601">1990</a>; Dziedzic and Teisseyre <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1990" title="Dziedzic K, Teisseyre AK (1990) The Hercynian molasse and younger deposits in the Intra-Sudetic Depression, SW Poland. Neues Jb Geol Paläontol Abh 179:285–305" href="/article/10.1007/s00531-024-02474-y#ref-CR32" id="ref-link-section-d17672574e604">1990</a>; Awdankiewicz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2003" title="Awdankiewicz M, Kurowski L, Mastalerz K, Raczyński P (2003) The Intra-Sudetic Basin—a record of sedimentary and volcanic processes in late- to post-orogenic tectonic setting. Geolines 16:165–183" href="/article/10.1007/s00531-024-02474-y#ref-CR11" id="ref-link-section-d17672574e607">2003</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2014a" title="Awdankiewicz M, Awdankiewicz H, Rapprich V, Stárková M (2014a) A Permian andesitic tuff ring at Rožmitál (the Intra-Sudetic Basin, Czech Republic)—evolution from explosive to effusive and high-level intrusive activity. Geol Q 58:759–778" href="/article/10.1007/s00531-024-02474-y#ref-CR8" id="ref-link-section-d17672574e610">2014a</a>). After the decline of the Variscan orogeny, the continental to marine sedimentation continued in the Late Triassic and then in the Late Cretaceous, followed by uplift and polyphase tectonic inversion (e.g., Dziedzic and Teisseyre <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1990" title="Dziedzic K, Teisseyre AK (1990) The Hercynian molasse and younger deposits in the Intra-Sudetic Depression, SW Poland. Neues Jb Geol Paläontol Abh 179:285–305" href="/article/10.1007/s00531-024-02474-y#ref-CR32" id="ref-link-section-d17672574e613">1990</a>; Mazur et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2006" title="Mazur S, Aleksandrowski P, Kryza R, Oberc-Dziedzic T (2006) The Variscan Orogen in Poland. Geol Q 50:89–118" href="/article/10.1007/s00531-024-02474-y#ref-CR61" id="ref-link-section-d17672574e617">2006</a>; Botor et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2019" title="Botor D, Anczkiewicz AA, Mazur S, Siwecki T (2019) Post-Variscan thermal history of the Intra-Sudetic Basin (Sudetes, Bohemian Massif) based on apatite fission track analysis. Int J Earth Sci 108:2561–2576" href="/article/10.1007/s00531-024-02474-y#ref-CR18" id="ref-link-section-d17672574e620">2019</a>).</p><p>The Intra-Sudetic Basin (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig2">2</a>), also known as the Intra-Sudetic Synclinorium, is amongst the earliest and largest of the late- to post-orogenic intracontinental basins in the region. It is considered as a pull-apart structure related to the Intra-Sudetic Fault (Aleksandrowski et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1997" title="Aleksandrowski P, Kryza R, Mazur S, Żaba J (1997) Kinematic data on major Variscan strike-slip faults and shear zones in the Polish Sudetes, northeast Bohemian Massif. Geol Mag 133:727–739" href="/article/10.1007/s00531-024-02474-y#ref-CR1" id="ref-link-section-d17672574e629">1997</a>). It is a NW–SE aligned, tectonically-bounded depression, ca. 70-km long and 35 km wide (Dziedzic and Teisseyre <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1990" title="Dziedzic K, Teisseyre AK (1990) The Hercynian molasse and younger deposits in the Intra-Sudetic Depression, SW Poland. Neues Jb Geol Paläontol Abh 179:285–305" href="/article/10.1007/s00531-024-02474-y#ref-CR32" id="ref-link-section-d17672574e632">1990</a>; Mastalerz and Prouza <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1995" title="Mastalerz K, Prouza V (1995) Development of the Intra-Sudetic Basin during Carboniferous and Permian. In: Mastalerz K, Prouza V, Kurowski L, Bossowski A, Ihnatowicz A, Nowak G (eds) Sedimentary record of the Variscan orogeny and climate—Intra-Sudetic Basin, Poland and Czech Republic. Guide to Excursion B1. XIII International Congress on Carboniferous-Permian August 28-September 2, 1995, Kraków, Poland. Państwowy Instytut Geologiczny" href="/article/10.1007/s00531-024-02474-y#ref-CR60" id="ref-link-section-d17672574e635">1995</a>). The Permo-Carboniferous basin fill accumulated between the late Viséan (ca. 335–333 Ma; Turnau et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2002" title="Turnau E, Żelaźniewicz A, Franke W (2002) Middle to early late Viséan onset of late orogenic sedimentation in the Intra-Sudetic Basin, West Sudetes: miospore evidence and tectonic implications. Geol Sudet 34:9–16" href="/article/10.1007/s00531-024-02474-y#ref-CR95" id="ref-link-section-d17672574e638">2002</a>) and the middle-late Permian (Saxonian-Thuringian in the mid-European classical subdivisions; e.g., Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e642">2016a</a>). This succession comprises mainly continental, siliciclastic rocks with volcanic intercalations, including 6.5-km thick lower Carboniferous, 2-km thick upper Carboniferous and 1.5-km thick Permian deposits. Due to the asymmetric distribution of these deposits (the thickest accumulations of older deposits in the NW and thinner, younger deposits in the SE) the total observed thickness does not exceed 4–5 km (Nemec et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1982" title="Nemec W, Porębski S, Teisseyre AK (1982) Explanatory notes to the Lithotectonic Molasse profile of the Intra-Sudetic Basin, Polish Part (Sudety Mts., Carboniferous-Permian). Veröffentlichung Des Zentralinstituts Für Physik der Erde AdW DDR, Potsdam 66:267–277" href="/article/10.1007/s00531-024-02474-y#ref-CR69" id="ref-link-section-d17672574e645">1982</a>).</p><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-2" data-title="Fig. 2"><figure><figcaption><b id="Fig2" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 2</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/2" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig2_HTML.png?as=webp"><img aria-describedby="Fig2" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig2_HTML.png" alt="figure 2" loading="lazy" width="685" height="655"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-2-desc"><p>Schematic geological map of the Intra-Sudetic Basin (modified from Bossowski et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1981" title="Bossowski A, Sawicki L, Wroński J (1981) Mapa geologiczna Polski 1:200 000. B—mapa bez utworów czwartorzędowych. Arkusz Wałbrzych. Wydawnictwa Geologiczne, Warszawa" href="/article/10.1007/s00531-024-02474-y#ref-CR17" id="ref-link-section-d17672574e658">1981</a>; Sawicki <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1988" title="Sawicki L (1988) Mapa geologiczna Polski 1:200 000. B—mapa bez utworów czwartorzędowych. Arkusz Kłodzko. Wydawnictwa Geologiczne, Warszawa" href="/article/10.1007/s00531-024-02474-y#ref-CR84" id="ref-link-section-d17672574e661">1988</a>; Milewicz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1989" title="Milewicz J, Szałamacha J, Szałamacha M (1989) Mapa geologiczna Polski 1:200 000. B—mapa bez utworów czwartorzędowych. Arkusz Jelenia Góra. Wydawnictwa Geologiczne, Warszawa" href="/article/10.1007/s00531-024-02474-y#ref-CR66" id="ref-link-section-d17672574e664">1989</a>; Kodym et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1967" title="Kodym O, Fusán O, Matějka A (eds) (1967) Geological map of Czechoslovakia 1: 500 000, West. Geological Survey of Czechoslovakia, Praha" href="/article/10.1007/s00531-024-02474-y#ref-CR47" id="ref-link-section-d17672574e667">1967</a>) that shows the distribution of the Góry Suche Rhyolitic Tuffs and Łomnica Rhyolites relative to other Permo-Carboniferous volcanic rocks. The location of the dated samples is indicated (for coordinates see Table <a data-track="click" data-track-label="link" data-track-action="table anchor" href="/article/10.1007/s00531-024-02474-y#Tab1">1</a>) together with other samples dated in previous studies</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/2" data-track-dest="link:Figure2 Full size image" aria-label="Full size image figure 2" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><p>Sedimentation in the Permo-Carboniferous times occurred predominantly in alluvial environments under a strong tectonic control, which resulted in several fining-upwards megacyclothems of conglomerates, sandstones and mudstones (Wojewoda and Mastalerz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1989" title="Wojewoda J, Mastalerz K (1989) Ewolucja klimatu oraz allocykliczność i autocykliczność sedymentacji na przykładzie osadów kontynentalnych górnego karbonu i permu w Sudetach. Przegląd Geologiczny 37(4):173–180" href="/article/10.1007/s00531-024-02474-y#ref-CR107" id="ref-link-section-d17672574e684">1989</a>). Marine deposits occur in the Upper Viséan, coal intercalations in the Upper Pennsylvanian, and lacustrine shales and limestones terminate the uppermost Pennsylvanian–lower Permian cyclothems. A gradual drying of climate is reflected in the transition from greenish-grey Carboniferous deposits to latest Carboniferous–Permian red beds (Mastalerz and Prouza <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1995" title="Mastalerz K, Prouza V (1995) Development of the Intra-Sudetic Basin during Carboniferous and Permian. In: Mastalerz K, Prouza V, Kurowski L, Bossowski A, Ihnatowicz A, Nowak G (eds) Sedimentary record of the Variscan orogeny and climate—Intra-Sudetic Basin, Poland and Czech Republic. Guide to Excursion B1. XIII International Congress on Carboniferous-Permian August 28-September 2, 1995, Kraków, Poland. Państwowy Instytut Geologiczny" href="/article/10.1007/s00531-024-02474-y#ref-CR60" id="ref-link-section-d17672574e687">1995</a>). The megacyclic structure and biostratigraphic data were the basis for the lithostratigraphic subdivision of the succession (Nemec et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1982" title="Nemec W, Porębski S, Teisseyre AK (1982) Explanatory notes to the Lithotectonic Molasse profile of the Intra-Sudetic Basin, Polish Part (Sudety Mts., Carboniferous-Permian). Veröffentlichung Des Zentralinstituts Für Physik der Erde AdW DDR, Potsdam 66:267–277" href="/article/10.1007/s00531-024-02474-y#ref-CR69" id="ref-link-section-d17672574e690">1982</a>; Wojewoda and Mastalerz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1989" title="Wojewoda J, Mastalerz K (1989) Ewolucja klimatu oraz allocykliczność i autocykliczność sedymentacji na przykładzie osadów kontynentalnych górnego karbonu i permu w Sudetach. Przegląd Geologiczny 37(4):173–180" href="/article/10.1007/s00531-024-02474-y#ref-CR107" id="ref-link-section-d17672574e693">1989</a>; Mastalerz and Prouza <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1995" title="Mastalerz K, Prouza V (1995) Development of the Intra-Sudetic Basin during Carboniferous and Permian. In: Mastalerz K, Prouza V, Kurowski L, Bossowski A, Ihnatowicz A, Nowak G (eds) Sedimentary record of the Variscan orogeny and climate—Intra-Sudetic Basin, Poland and Czech Republic. Guide to Excursion B1. XIII International Congress on Carboniferous-Permian August 28-September 2, 1995, Kraków, Poland. Państwowy Instytut Geologiczny" href="/article/10.1007/s00531-024-02474-y#ref-CR60" id="ref-link-section-d17672574e696">1995</a>; Wagner <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2008" title="Wagner R (ed) (2008) Tabela stratygraficzna Polski. Polska pozakarpacka. Ministerstwo Środowiska, Warszawa" href="/article/10.1007/s00531-024-02474-y#ref-CR100" id="ref-link-section-d17672574e700">2008</a>). However, fossils are scarce in several rock units, or their stratigraphic interpretation is not unequivocal (e.g., miospores in the Permian Walchia shale; Dunn <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2001" title="Dunn MT (2001) Palynology of the Carboniferous-Permian boundary stratotype, Aidaralash Creek, Kazakhstan. Rev Palaeobot Palynol 116:175–194" href="/article/10.1007/s00531-024-02474-y#ref-CR30" id="ref-link-section-d17672574e703">2001</a>). The lithostratigraphic schemes of Carboniferous—Permian deposits were partly verified and correlated to the international chronostratigraphic scale with the help of precise U–Pb dating of zircon from tonstein, tuff and lava intercalations in the SW part of the Intra-Sudetic Basin and other basins to the west (Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e706">2016a</a>).</p><p>Volcanic and subvolcanic activity in the basin (Kozłowski <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1963" title="Kozłowski S (1963) Geologia wulkanitów permskich w centralnej części niecki śródsudeckiej. Prace Geologiczne, Komitet Nauk Geologicznych PAN, Kraków, p 14" href="/article/10.1007/s00531-024-02474-y#ref-CR48" id="ref-link-section-d17672574e712">1963</a>; Nowakowski <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1968" title="Nowakowski A (1968) Wulkanity permskie Gór Suchych w niecce śródsudeckiej. Geol Sudet 4:299–408" href="/article/10.1007/s00531-024-02474-y#ref-CR70" id="ref-link-section-d17672574e715">1968</a>; Dziedzic <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1998" title="Dziedzic K (1998) Genesis and evolution of Sudetic late hercynian volcanic rocks inferred from trace element modelling. Geol Sudet 38:79–91" href="/article/10.1007/s00531-024-02474-y#ref-CR31" id="ref-link-section-d17672574e718">1998</a>; Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e721">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e724">b</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Awdankiewicz M (2004) Sedimentation, volcanism and subvolcanic intrusions in a late Palaeozoic intramonatne trough (the Intra-Sudetic Basin, SW Poland). Geol Soc Lond Spec Publ 234:5–11" href="/article/10.1007/s00531-024-02474-y#ref-CR5" id="ref-link-section-d17672574e728">2004</a>; Awdankiewicz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2003" title="Awdankiewicz M, Kurowski L, Mastalerz K, Raczyński P (2003) The Intra-Sudetic Basin—a record of sedimentary and volcanic processes in late- to post-orogenic tectonic setting. Geolines 16:165–183" href="/article/10.1007/s00531-024-02474-y#ref-CR11" id="ref-link-section-d17672574e731">2003</a>; Ulrych et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Ulrych J, Fediuk F, Lang M, Martinec P (2004) Late Palaeozoic volcanic rocks of the Intra-Sudetic Basin, Bohemian Massif: petrological and geochemical characteristics. Chemie der Erde Geochem 64:127–153" href="/article/10.1007/s00531-024-02474-y#ref-CR97" id="ref-link-section-d17672574e734">2004</a>) occurred in two major stages, the older in Carboniferous and the younger in Permian (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="Awdankiewicz M (2022) Polyphase Permo-Carboniferous magmatism adjacent to the Intra-Sudetic Fault: constraints from U-Pb SHRIMP zircon study of felsic subvolcanic intrusions in the Intra-Sudetic Basin, SW Poland. Int J Earth Sci 111:2199–2224" href="/article/10.1007/s00531-024-02474-y#ref-CR6" id="ref-link-section-d17672574e737">2022</a>). The older volcanic suite shows calc-alkaline, volcanic arc-like geochemical features, whereas the younger volcanic suite grades towards mildly alkaline, within plate characteristics (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e740">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e743">b</a>). Magmas were derived from metasomatized mantle sources and evolved due to fractional crystallisation with a weaker influence of open-system processes like crustal contamination (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e747">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e750">b</a>) or were strongly affected by assimilation-fractional crystallisation (Dziedzic <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1998" title="Dziedzic K (1998) Genesis and evolution of Sudetic late hercynian volcanic rocks inferred from trace element modelling. Geol Sudet 38:79–91" href="/article/10.1007/s00531-024-02474-y#ref-CR31" id="ref-link-section-d17672574e753">1998</a>; Ulrych et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Ulrych J, Fediuk F, Lang M, Martinec P (2004) Late Palaeozoic volcanic rocks of the Intra-Sudetic Basin, Bohemian Massif: petrological and geochemical characteristics. Chemie der Erde Geochem 64:127–153" href="/article/10.1007/s00531-024-02474-y#ref-CR97" id="ref-link-section-d17672574e756">2004</a>).</p><p>In the northern and western parts of the basin (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig2">2</a>) rhyodacite laccoliths and lavas (313–310 Ma) together with minor rhyodacite and andesite sills (306–305 Ma) reflect episodic, low-volume, dominantly subvolcanic Carboniferous activity, followed by younger rhyolitic laccoliths and dikes in the Permian (ca. 293 Ma; Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="Awdankiewicz M (2022) Polyphase Permo-Carboniferous magmatism adjacent to the Intra-Sudetic Fault: constraints from U-Pb SHRIMP zircon study of felsic subvolcanic intrusions in the Intra-Sudetic Basin, SW Poland. Int J Earth Sci 111:2199–2224" href="/article/10.1007/s00531-024-02474-y#ref-CR6" id="ref-link-section-d17672574e766">2022</a>). The latter activity is linked with the main, most voluminous phase of volcanism which occurred across the basin and resulted in extensive succession of trachyandesites, rhyolites and rhyolitic tuffs up to ca. 700 m in total thickness. Several volcanic centres were identified, such as small basaltic trachyandesite shield volcanoes, rhyolite extrusions and rhyolitic-trachyandesitic multivent volcanoes (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e769">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e772">b</a>). This volcanism reached climactic phase in the caldera-forming ignimbrite eruption of the GSRT exceeding 300 m in maximum thickness (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e775">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e779">b</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Awdankiewicz M (2004) Sedimentation, volcanism and subvolcanic intrusions in a late Palaeozoic intramonatne trough (the Intra-Sudetic Basin, SW Poland). Geol Soc Lond Spec Publ 234:5–11" href="/article/10.1007/s00531-024-02474-y#ref-CR5" id="ref-link-section-d17672574e782">2004</a>). The emplacement of trachyandesitic and rhyolitic sills and laccoliths below the ignimbrites, as well as local andesitic to rhyolitic eruptions terminated volcanism (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e785">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e788">b</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Awdankiewicz M (2004) Sedimentation, volcanism and subvolcanic intrusions in a late Palaeozoic intramonatne trough (the Intra-Sudetic Basin, SW Poland). Geol Soc Lond Spec Publ 234:5–11" href="/article/10.1007/s00531-024-02474-y#ref-CR5" id="ref-link-section-d17672574e791">2004</a>; Awdankiewicz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2014b" title="Awdankiewicz M, Kryza R, Szczepara N (2014b) Timing of post-collisional volcanism in the eastern part of the Variscan Belt: constraints from SHRIMP zircon dating of Permian rhyolites in the North-Sudetic Basin (SW Poland). Geol Mag 151:611–628" href="/article/10.1007/s00531-024-02474-y#ref-CR10" id="ref-link-section-d17672574e794">2014b</a>). Within this complex volcanic succession, only the Góry Krucze (Vrani Hory) Rhyolites in the western limb of the basin were dated (CA-ID-TIMS dating of 297.11 ± 0.04 Ma, Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e798">2016a</a>) and the age of the other volcanic rocks is only constrained by indirect evidence.</p><h3 class="c-article__sub-heading" id="Sec4">The stratigraphic position of volcanic rocks</h3><p>The dominantly red and brown-coloured Upper Carboniferous to Lower Permian (Rotliegendes) sedimentary rocks of the Intra-Sudetic Basin are subdivided into the Ludwikowice, Krajanów and Słupiec formations, the first one included into Carboniferous and the two latter into the Permian (Nemec et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1982" title="Nemec W, Porębski S, Teisseyre AK (1982) Explanatory notes to the Lithotectonic Molasse profile of the Intra-Sudetic Basin, Polish Part (Sudety Mts., Carboniferous-Permian). Veröffentlichung Des Zentralinstituts Für Physik der Erde AdW DDR, Potsdam 66:267–277" href="/article/10.1007/s00531-024-02474-y#ref-CR69" id="ref-link-section-d17672574e809">1982</a>). The most widespread complex of volcanic rocks in the Intra-Sudetic Basin is part of the Słupiec Formation, also known as the Broumov Formation (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig3">3</a>). The dual lithostratigraphic terminology reflects outcropping of the basin fill across the Polish-Czech border and the specific subdivisions used in the two countries. However, the stratigraphic position of the Słupiec Formation is not precisely constrained (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig3">3</a>a). It has been variably assigned to Sakmarian (Wagner <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2008" title="Wagner R (ed) (2008) Tabela stratygraficzna Polski. Polska pozakarpacka. Ministerstwo Środowiska, Warszawa" href="/article/10.1007/s00531-024-02474-y#ref-CR100" id="ref-link-section-d17672574e818">2008</a>), upper Asselian and Sakmarian (McCann et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2006" title="McCann T, Pascal C, Timmerman M, Krzywiec P, López-Gómez J, Wetzel L, Krawczyk CM, Rieke H, Lamarche J (2006) Post-Variscan (end Carboniferous—Early Permian) basin evolution in Western and Central Europe. In: Gee DG, Stephenson RA (eds) European lithosphere dynamics, vol 32. Geological Society, London, Memoirs, pp 355–388" href="/article/10.1007/s00531-024-02474-y#ref-CR64" id="ref-link-section-d17672574e821">2006</a>), Asselian-Sakmarian (Štamberg and Zajíc <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2008" title="Štamberg S, Zajíc J (2008) Carboniferous and Permian faunas and their occurence in the limnic basins of the Czech Republic. Muzeum východních Čech v Hradci Králové, Hradec Králové" href="/article/10.1007/s00531-024-02474-y#ref-CR88" id="ref-link-section-d17672574e825">2008</a>), Asselian and lowermost Sakmarian (Schneider et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1995" title="Schneider JW, Rӧssler R, Gaitzsch B (1995) Time lines of the Late Variscan volcanism—a holostratigraphic synthesis. Zentralblatt Für Geologie und Paläontologie, Teil I 5(6):477–490" href="/article/10.1007/s00531-024-02474-y#ref-CR86" id="ref-link-section-d17672574e828">1995</a>), or Asselian (Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2017b" title="Opluštil S, Šimůnek Z, Pšenička J, Bek J, Libertín M (2017b) A 25 million year macrofloral record (Carboniferous–Permian) in the Czech part of the Intra-Sudetic Basin; biostratigraphy, plant diversity and vegetation patterns. Rev Palaeobot Palynol 244:241–307" href="/article/10.1007/s00531-024-02474-y#ref-CR76" id="ref-link-section-d17672574e831">2017b</a>). The Słupiec/Broumov Formation is further subdivided (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig3">3</a>b) into the Building sandstone (the Nowa Ruda Member in the Czech subdivision) and the Walchia shale (corresponding to the Olivetin and Martinkovice members). In the central part of the ISB, where the volcano sedimentary succession is most complete, the volcanic rocks occur in the middle part of the Słupiec Formation: above the Building sandstone and below the Walchia shale. Although there is a local interstratification of the sedimentary and volcanic rocks, the outcrop of the latter is distinctive across the basin, and hence the volcanic rocks are grouped into a separate unit, the Lower Permian Volcanic Complex (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e837">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e840">b</a>).</p><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-3" data-title="Fig. 3"><figure><figcaption><b id="Fig3" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 3</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/3" rel="nofollow"><picture><img aria-describedby="Fig3" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig3_HTML.png" alt="figure 3" loading="lazy" width="685" height="353"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-3-desc"><p><b>a</b> Changing views on the position of the Słupiec Formation in the global chronostratigraphic scale (Cohen et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2013" title="Cohen KM, Finney SC, Gibbard PL, Fan J-X (2013) The ICS international chronostratigraphic chart. Episodes 36:199–204" href="/article/10.1007/s00531-024-02474-y#ref-CR27" id="ref-link-section-d17672574e856">2013</a>, updated). S 1995: Schneider et al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1995" title="Schneider JW, Rӧssler R, Gaitzsch B (1995) Time lines of the Late Variscan volcanism—a holostratigraphic synthesis. Zentralblatt Für Geologie und Paläontologie, Teil I 5(6):477–490" href="/article/10.1007/s00531-024-02474-y#ref-CR86" id="ref-link-section-d17672574e859">1995</a>); SZ 2008: Štamberg and Zajíc (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2008" title="Štamberg S, Zajíc J (2008) Carboniferous and Permian faunas and their occurence in the limnic basins of the Czech Republic. Muzeum východních Čech v Hradci Králové, Hradec Králové" href="/article/10.1007/s00531-024-02474-y#ref-CR88" id="ref-link-section-d17672574e862">2008</a>); MC 2008: McCann et al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2006" title="McCann T, Pascal C, Timmerman M, Krzywiec P, López-Gómez J, Wetzel L, Krawczyk CM, Rieke H, Lamarche J (2006) Post-Variscan (end Carboniferous—Early Permian) basin evolution in Western and Central Europe. In: Gee DG, Stephenson RA (eds) European lithosphere dynamics, vol 32. Geological Society, London, Memoirs, pp 355–388" href="/article/10.1007/s00531-024-02474-y#ref-CR64" id="ref-link-section-d17672574e865">2006</a>); W 2008: Wagner (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2008" title="Wagner R (ed) (2008) Tabela stratygraficzna Polski. Polska pozakarpacka. Ministerstwo Środowiska, Warszawa" href="/article/10.1007/s00531-024-02474-y#ref-CR100" id="ref-link-section-d17672574e868">2008</a>); O 2017: Opluštilet al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2017b" title="Opluštil S, Šimůnek Z, Pšenička J, Bek J, Libertín M (2017b) A 25 million year macrofloral record (Carboniferous–Permian) in the Czech part of the Intra-Sudetic Basin; biostratigraphy, plant diversity and vegetation patterns. Rev Palaeobot Palynol 244:241–307" href="/article/10.1007/s00531-024-02474-y#ref-CR76" id="ref-link-section-d17672574e872">2017b</a>). <b>b</b> Lithostratigraphic subdivision of the Słupiec (Broumov) Formation showing the Lower Permian Volcanic Complex, the Góry Suche Rhyolitic Tuffs and the Łomnica Rhyolites (based on Mastalerz and Prouza <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1995" title="Mastalerz K, Prouza V (1995) Development of the Intra-Sudetic Basin during Carboniferous and Permian. In: Mastalerz K, Prouza V, Kurowski L, Bossowski A, Ihnatowicz A, Nowak G (eds) Sedimentary record of the Variscan orogeny and climate—Intra-Sudetic Basin, Poland and Czech Republic. Guide to Excursion B1. XIII International Congress on Carboniferous-Permian August 28-September 2, 1995, Kraków, Poland. Państwowy Instytut Geologiczny" href="/article/10.1007/s00531-024-02474-y#ref-CR60" id="ref-link-section-d17672574e878">1995</a>; Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e881">1999a</a>)</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/3" data-track-dest="link:Figure3 Full size image" aria-label="Full size image figure 3" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><p>The Lower Permian Volcanic Complex comprises a number of smaller volcanic rock units, reflecting several eruptive stages and the emplacement of subvolcanic intrusions at distinct volcanic centres (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e895">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e898">b</a>). The most extensive are the GSRT that comprise ca. 50% of the total outcrops of the Lower Permian Volcanic Complex and make up the upper part of this Complex (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig2">2</a>). To the NW the GSRT are in tectonic contact, across a SW-NE trending fault, with other Permian volcanic rocks, including the Góry Krucze Rhyolites (dated at 297.11 ± 0.04 Ma by Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e904">2016a</a>). In the central part of the ISB the GSRT overlie older volcanic rocks with an erosional unconformity (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e907">1999a</a>). Further east and south-east, younger volcanic rocks locally overlie the GSRT and subvolcanic intrusions (sills) straddle the contact of the GSRT with the underlying Building sandstone. These intrusions are mostly trachyandesites, but include also the Łomnica Rhyolites (ŁR) in the northern part. Two volcanic rocks units, the GSRT and the ŁR, which are the subjects of SHRIMP study reported in this paper, are characterised in more detail below.</p><h3 class="c-article__sub-heading" id="Sec5">The Góry Suche Rhyolitic Tuffs and the Łomnica Rhyolites—origin, distribution, lithofacies</h3><p>The GSRT (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig2">2</a>) represent an extensive, ignimbrite-dominated pyroclastic deposit which is linked to eruption from a caldera located near the centre of the Intra-Sudetic Basin (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e921">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e924">b</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Awdankiewicz M (2004) Sedimentation, volcanism and subvolcanic intrusions in a late Palaeozoic intramonatne trough (the Intra-Sudetic Basin, SW Poland). Geol Soc Lond Spec Publ 234:5–11" href="/article/10.1007/s00531-024-02474-y#ref-CR5" id="ref-link-section-d17672574e927">2004</a>). The presence of a collapse caldera, NW–SE aligned and ca. 15 km across, has been inferred from indirect geological evidence: (1) the supposed caldera corresponds to intrabasinal depression, which acted as the depositional centre of the Intra-Sudetic Basin in the latest Carboniferous to Permian times, and (2) the N, NE and S margins of the above depression are straddled by abundant post-GSRT trachyandesite and rhyolite subvolcanic intrusions, which indicate post-ignimbrite magmatism focussed along the margins of the depression. Recently, transport directions of pyroclastic flows were determined from the anisotropy of magnetic suspectibility (AMS) of the GSRT ignimbrites. These preliminary results are consistent with the interpretation of the above depression as the source caldera of the GSRT (Romero et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2023" title="Romero L, Petronis MS, Awdankiewicz M, Rapprich V (2023) Emplacement of Caldera-Related Rhyolitic Ignimbrite in a Variscan post-orogenic basin—constraints from paleomagnetic and anisotropy of magnetic susceptibility data from the Permian Gory Suche Rhyolitic Tuff. AGU23, 11–15 Dec, GP11B-0469. 
 https://agu.confex.com/agu/fm23/meetingapp.cgi/Paper/1377413
 
 " href="/article/10.1007/s00531-024-02474-y#ref-CR83" id="ref-link-section-d17672574e930">2023</a>).</p><p>The main outcrop of the GSRT extends for 55 km from NW to SE, across the inferred caldera. Smaller outcrops of the GSRT, isolated due to younger tectonics and erosion, are found in two intrabasinal tectonic troughs in the east (Don <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1961" title="Don J (1961) Utwory młodopaleozoiczne okolic Nowej Rudy. Zeszyty Naukowe Uniwersytetu Wrocławskiego, Nauki Przyrodnicze, Nauki o Ziemi III, Seria b, Nr 6:3–54" href="/article/10.1007/s00531-024-02474-y#ref-CR29" id="ref-link-section-d17672574e936">1961</a>). The total thickness of the GSRT exceeds 300 m in the northern part of the inferred caldera (possibly over 500 m between Ruprechtice and Heřmánkovice; Hrdličková <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1966" title="Hrdličková D (1966) Ignimbrite volcanism in the Broumov area in north-eastern Bohemia. In: Paleovolcanites of the Bohemian Massif. Praha, pp 191–199" href="/article/10.1007/s00531-024-02474-y#ref-CR43" id="ref-link-section-d17672574e939">1966</a>), varies within 100–200 m NW of the caldera and within 10–50 m SE and E of the caldera. In addition, abundant felsic volcanogenic detritus recognised in alluvial to lacustrine sedimentary rocks overlying the GSRT (the Olivetin Member; Prouza <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1988" title="Prouza V (1988) Geologic map of the Czechoslovakia, sheet 04–32 Broumov (in Czech). Geological Survey of Czechoslovakia, Prague" href="/article/10.1007/s00531-024-02474-y#ref-CR81" id="ref-link-section-d17672574e942">1988</a>; Blecha <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1992" title="Blecha M (1992) Laterální přechod z aluviálních kuželů do lakustrinního prostředí; model sedimentace svrchních olivětínských vrstev (autun) v české části vnitrosudetské pánve. Věsrník Českého Geologického Ústavu 67(5):347–362" href="/article/10.1007/s00531-024-02474-y#ref-CR16" id="ref-link-section-d17672574e945">1992</a>) reflects massive erosion and reworking of silicic volcanogenic rocks.</p><p>The total magma volume of the GSRT eruption (dense rock equivalent, DRE) can be roughly estimated at 50–100 km<sup>3</sup>. This estimate assumes distribution of the tuffs similar to the present outcrop (area ca. 55 × 18 km), a mean thickness of 0.1 km in the present outcrop area, and a primary porosity up to 50%. A more sophisticated calculation seems problematic due to several unknowns, related to post-emplacement erosion of the GSRT (locally up to a half of the original thickness?; Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e953">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e956">b</a>), unclear primary extent of the deposit beyond the present tectonic margins of the basin and the unknown volume of distal co-ignimbrite ash-fall deposits, which may represent up to 50% of total erupted volume (e.g., Brown and Andrews <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2015" title="Brown RJ, Andrews GDM (2015) Deposits of pyroclastic density currents. In: Sigurdson H (ed) Encyclopedia of volcanoes. Elsevier, pp 631–648" href="/article/10.1007/s00531-024-02474-y#ref-CR23" id="ref-link-section-d17672574e959">2015</a>). Thus the GSRT volume approximation of ca. 100 km<sup>3</sup> may rather reflect the lower range of magma volume erupted.</p><p>Three main lithofacies can be distinguished within the GSRT, from base to top: (1) bedded tuffs and lapilli tuffs, (2) massive, nonwelded tuffs, (3) massive, welded tuffs (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig4">4</a>). The bedded tuffs and lapilli tuffs are interpreted as pyroclastic fall and surge deposits, locally reworked. The massive tuffs are interpreted as pyroclastic flow deposits—ignimbrites, including nonwelded and welded facies (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e970">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e973">b</a> and references cited therein). The main characteristics of these rocks given below are based on published work (Awdankiewicz, op. cit.) and photomicrographs of representative samples used in this study are given in Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>.</p><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-4" data-title="Fig. 4"><figure><figcaption><b id="Fig4" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 4</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/4" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig4_HTML.png?as=webp"><img aria-describedby="Fig4" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig4_HTML.png" alt="figure 4" loading="lazy" width="685" height="1363"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-4-desc"><p>Generalized log of the Góry Suche Rhyolitic Tuffs and the Łomnica Rhyolites, highlighting lithofacies in the tuffs, dated samples and their ages and relationships to other volcanic rocks discussed in the text</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/4" data-track-dest="link:Figure4 Full size image" aria-label="Full size image figure 4" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-5" data-title="Fig. 5"><figure><figcaption><b id="Fig5" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 5</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/5" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig5_HTML.jpg?as=webp"><img aria-describedby="Fig5" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig5_HTML.jpg" alt="figure 5" loading="lazy" width="685" height="693"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-5-desc"><p>Photomicrographs of the studied samples (<b>a</b>–<b>d</b>, <b>f</b>—plane-polarized light, <b>e</b>—crossed polarizers). <b>a</b> Sample Go1, porphyritic rhyolite. Phenocrysts of K-feldspar, embayed quartz and albitized plagioclase in microcrystalline, felsitic groundmass of anhedral alkali feldspars and quartz with Fe–Ti oxide pigment and larger opaque aggregates. <b>b</b> Sample Pu2, lithic-rich tuff. The main components are brown to opaque clasts of micro to cryptocrystalline rhyolites and crystals of K-feldspar and quartz. Alignment of fragments parallels bedding seen in hand-specimen. <b>c</b> Sample Wl1, massive non-welded tuff. Altered glass shards, broken crystals of quartz and K-feldspar and lithics (rhyolite, trachyandesite) are set in recrystallized finest fractions with abundant Fe-oxide pigment. <b>d</b> Sample Mi1, massive non-welded tuff. The texture and composition (altered glass shards, quartz, K-feldspar, lithics) are similar to sample Wl1. <b>e</b> Sample Gr1, slightly welded and recrystallized tuff with broken crystals of quartz, K-feldspar and rhyolite clasts in a recrystallized matrix of glass shards. <b>f</b> Sample Mi2, welded tuff with eutaxitic texture. Glass shards, flattened and squeezed between crystals of quartz and K-feldspar, are recrystallized into fibrous aggregates of alkali feldspar and quartz. G—glass shards, Kfs—K-feldspar, Pl—plagioclase, Q—quartz, R—rhyolite clasts, Ta—trachyandesite clasts</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/5" data-track-dest="link:Figure5 Full size image" aria-label="Full size image figure 5" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><p>The bedded tuffs and lapilli tuffs occur mainly in the north and north-west of the GSRT outcrop, with sparse, local occurrence in the east and south east. Their variable thickness in the NW may reflect deposition over pre-existing volcanic topography modified by erosion (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e1049">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e1052">b</a>). The bedded tuffs and lapilli tuffs are poorly exposed and can be observed almost exclusively in loose in-situ blocks. The tuffs are red to brown or green in colour, finely bedded to laminated at cm-mm scale. Planar, subhorizontal bedding is typical but wavy and low-angle cross bedding are observed in some specimens. The largest clasts do not exceed 20 mm across and the finer, ash-sized fractions predominate. Normal, as well as reverse grain-size grading and impact sags associated with larger lithics and with accretionary lapilli are observed in some specimens. The tuffs are composed of variable amounts of strongly altered hypo- to microcrystalline clasts of rhyolites as well as quartz and feldspar crystals (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>b), which partly may represent broken phenocrysts as well as detrital grains.</p><p>The massive nonwelded tuffs are the dominant lithology found across the basin. They are characterised by lack of bedding and relatively homogeneous structure even at larger exposures, 10–20 m high. Indistinct layering occurs in places, but variable joints and cracks are most typical. The tuffs are red to brown often with greenish spots, patches and streaks cm to dm in size. This tuffs show crystalo-vitroclastic textures and their main components are ash-sized glass shards (strongly altered, recrystallized) as well as broken crystals of quartz, feldspar (alkali feldspar, albitized plagioclase), rarely biotite (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>c, d). There are variable but small amounts (< 10–15%) of fine lithic clasts (typically < 5 mm, more rarely several cm across), both volcanic and non-volcanic (e.g., texturally variable trachyandesites and rhyolites, also shales) and rarely poorly preserved, broken accretionary lapilli. The tuffs are locally highly porous and some larger, mm to cm-sized cavities possibly formed after weathered pumice clasts. In the south-east of the GSRT outcrop the massive nonwelded tuffs often contain abundant analcite replacing glass shards as well as nodules, up to few cm in diameter, which are more strongly lithified compared to the surrounding tuff (Awdankiewicz and Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2015" title="Awdankiewicz M, Awdankiewicz H (2015) Variable post-magmatic mineral assemblages and bulk-rock chemistry of the Góry Suche Rhyolitic Tuffs (Permian, the Intra-Sudetic Basin, SW Poland). Mineral Spec Pap 44:19" href="/article/10.1007/s00531-024-02474-y#ref-CR7" id="ref-link-section-d17672574e1064">2015</a>). Some nodules exhibit central, irregular cavity (after weathered pumice clasts?).</p><p>The massive welded tuffs occur as discontinuous layers at the top of the GSRT in the central to NW parts of the outcrop. Some interdigitation of nonwelded and variably welded tuffs is locally recognised (Hrdličková <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1966" title="Hrdličková D (1966) Ignimbrite volcanism in the Broumov area in north-eastern Bohemia. In: Paleovolcanites of the Bohemian Massif. Praha, pp 191–199" href="/article/10.1007/s00531-024-02474-y#ref-CR43" id="ref-link-section-d17672574e1070">1966</a>). The massive welded tuffs are pale-coloured with pink, reddish or grey shades. Similar to the nonwelded tuffs, indistinct layering as well as irregular to platy joints are observed. Compared to the nonwelded tuffs, however, the welded lithology shows more compact texture resembling porphyritic rhyolites, with up to ca. 30% of broken quartz and feldspar phenocrysts. Larger clasts of the lapilli fraction, either flattened (fiamme) or angular (lithics, such as texturally variable rhyolites) are rare. Crystalovitroclastic and eutaxitic textures, with flattened and aligned glass shards and pumice warped around broken phenocrysts of quartz and feldspars (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>e, f), are characteristic in thin sections.</p><p>The GSRT show pronounced petrographic evidence of post-emplacement recrystallization and alteration which can be related to cooling- and vapour phase-processes, as well as diagenesis (cf. McPhie et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1993" title="McPhie J, Allen RL, Doyle M (1993) Volcanic textures: a guide to the interpretation of textures in volcanic rocks. University of Tasmania, Centre for Ore Deposit and Exploration Studies" href="/article/10.1007/s00531-024-02474-y#ref-CR65" id="ref-link-section-d17672574e1079">1993</a>). Primary volcanic glass is always replaced by variable assemblages of secondary minerals. In the NW half of the outcrop these are usually quartz, K-feldspar, carbonates (calcite, dolomite) and clay minerals (e.g., kaolinite), whereas in the SE there is also abundant analcite. Plagioclase is replaced by albite, carbonates and kaolinite. Recrystallization and alteration partly obscure the primary vitroclastic texture. These mineralogical and textural modifications were also accompanied by bulk-rock chemical changes such as variable contents of silica and alkalis (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e1082">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e1085">b</a>; Awdankiewicz and Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2015" title="Awdankiewicz M, Awdankiewicz H (2015) Variable post-magmatic mineral assemblages and bulk-rock chemistry of the Góry Suche Rhyolitic Tuffs (Permian, the Intra-Sudetic Basin, SW Poland). Mineral Spec Pap 44:19" href="/article/10.1007/s00531-024-02474-y#ref-CR7" id="ref-link-section-d17672574e1088">2015</a>).</p><p>The ŁR (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e1094">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e1097">b</a>) crop out near the northern margin of the inferred GSRT source caldera. The rhyolite subvolcanic intrusive bodies are emplaced in mudstones and sandstones of the Słupiec Formation. There are two larger intrusions and a third smaller, possibly all interconnected at deeper levels. The intrusions, lensoidal in shape, are up to ca. 250 m thick, laterally extend for up to 2 km, and are thick sills or laccoliths. Northwards (down-sequence) petrographically equivalent rhyolites are found as small plugs or short dikes within the underlying Carboniferous to Permian sedimentary rocks adjacent to NNE-striking fault. These small intrusive bodies possibly indicate feeder zones of the rhyolite magma. All the intrusions are monotonous in terms of lithology and mainly formed by massive porphyritic rhyolites, with quartz and feldspar phenocrysts in a felsitic microcrystalline groundmass (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>a). Local brecciation of rhyolites at the contacts with mudstones and a weak thermal alteration of the latter are reported by Kozłowski (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1963" title="Kozłowski S (1963) Geologia wulkanitów permskich w centralnej części niecki śródsudeckiej. Prace Geologiczne, Komitet Nauk Geologicznych PAN, Kraków, p 14" href="/article/10.1007/s00531-024-02474-y#ref-CR48" id="ref-link-section-d17672574e1103">1963</a>).</p></div></div></section><section data-title="Methods"><div class="c-article-section" id="Sec6-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="Sec6">Methods</h2><div class="c-article-section__content" id="Sec6-content"><p>Nine samples were collected for the SHRIMP U–Pb zircon dating. The location of samples and their relative stratigraphic positions are indicated in Figs. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig2">2</a> and <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig4">4</a> and the coordinates of sampling sites are given in Table <a data-track="click" data-track-label="link" data-track-action="table anchor" href="/article/10.1007/s00531-024-02474-y#Tab1">1</a>. The samples were studied in thin sections using a standard petrographic microscope. Zircons were separated at the Polish Geological Institute—National Research Institute, Lower Silesian Branch. Samples ca. 5 kg in weight were crushed in jaw-crusher, sieved, and the heavy fraction (0.06–0.25 mm) was separated using Nd magnet and heavy liquid (sodium polytungstate). Zircon crystals were hand-picked from the concentrates under a binocular microscope and mounted with reference material (the TEMORA II standard <sup>206</sup>Pb/<sup>238</sup>U = 0.06683; Black et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2003" title="Black LP, Kamo SL, Allen CM, Aleinikoff JN, Davis DW, Korsch RJ, Foudoulis C (2003) TEMORA 1: a new zircon standard for Phanerozoic U–Pb geochronology. Chem Geol 200:155–170" href="/article/10.1007/s00531-024-02474-y#ref-CR14" id="ref-link-section-d17672574e1129">2003</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Black LP, Kamo SL, Allen CM, Davis DW, Aleinikoff JN, Valley JW, Mundil R, Campbell IH, Korsch RJ, Williams IS, Foudoulis C (2004) Improved Pb-206/U-218 microprobe geochronology by the monitoring of a trace-element-related matrix effect; SHRIMP, ID-TIMS, ELA-ICP-MS and oxygen isotope documentation for a series of zircon standards. Chem Geol 205:115–140" href="/article/10.1007/s00531-024-02474-y#ref-CR15" id="ref-link-section-d17672574e1132">2004</a>) and zircon standard 91,500 for uranium concentration calibration U = 82.5 ppm; Wiedenbeck et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Wiedenbeck M, Hanchar JM, Peck WH, Sylvester P, Valley J, Whitehouse M, Kronz A, Morishita Y, Nasdala L, Fiebig J, Franchi I, Girard JP, Greenwood RC, Hinton R, Kita N, Mason PRD, Norman M, Ogasawara M, Piccoli PM, Rhede D, Satoh H, Schulz-Dobrick B, Skår Ø, Spicuzza MJ, Terada K, Tindle A, Togashi S, Vennemann T, Xie Q, Zheng YF (2004) Further characterisation of the 91500 zircon crystal. Geostand Geoanal Res 28:9–39" href="/article/10.1007/s00531-024-02474-y#ref-CR101" id="ref-link-section-d17672574e1135">2004</a>) into epoxy mounts. The samples were polished and documented under the optical microscope (reflected and transmitted light), then imaged by cathodoluminescence (CL) using a Hitachi SU3500 scanning electron microscope for selection of crystals and spots for isotope analyses. Zircon crystals with any traces of cracks and inclusions were excluded from analysis. In rare cases of zircons with cores analytical spots were located in the rims only. The samples were analysed using the SHRIMP IIe/MC ion microprobe in the Micro-area Analysis Laboratory of the Polish Geological Institute—NRI. The procedures based on those described by Williams and Cleasson (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1987" title="Williams IS, Cleasson S (1987) Isotopic evidence for the Precambrian provenance and Caledonian metamorphism of high grade paragneisses from the Seve Nappes, Scandinavian Caledonides: II Ion microprobe zircon U-Th-Pb. Contrib Miner Petrol 97:205–217" href="/article/10.1007/s00531-024-02474-y#ref-CR104" id="ref-link-section-d17672574e1138">1987</a>) were applied. The following analytical requirements were fulfilled: 3 nA negative O<sub>2</sub>—primary ion stream centred on a ca. 23-µm spot; mass accuracy ca. 5500; isotope ratio quantification by single electron multiplier and periodic maximum stepping. Before each analysis, the analytical spot was pre-cleaned by rastering of the primary beam for ca. three min. to reduce the amount of common Pb on the mount surface. Analysis in each spot took about 17 min. Data were collected in six sets of mass scans (<sup>196</sup>Zr<sub>2</sub>O—2 s; <sup>204</sup>Pb—5 s; 204.1 background—5 s; <sup>206</sup>Pb—15 s; <sup>207</sup>Pb—15 s; <sup>208</sup>Pb—15 s; <sup>238</sup>U—10 s; <sup>248</sup>ThO—5 s; <sup>254</sup>UO—2 s), with TEMORA zircon examined after each three consecutive analyses. The data were reduced in a manner similar to that described by Williams (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1998" title="Williams IS (1998) U-Th-Pb Geochronology by Ion Microprobe. In: McKibben MA, Shanks III WC, Ridley WI (Eds), Applications of microanalytical techniques to understanding mineralizing processes. Reviews in Economic Geology, vol 7, pp 1–35" href="/article/10.1007/s00531-024-02474-y#ref-CR103" id="ref-link-section-d17672574e1163">1998</a>, and references therein), using the SQUID Excel Macro of Ludwig (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2000" title="Ludwig KR (2000) Squid 1.0—a user’s manual. Berkeley Geochronology Center, Special Publication. No. 2, 17 pp" href="/article/10.1007/s00531-024-02474-y#ref-CR56" id="ref-link-section-d17672574e1166">2000</a>). All the measurements of zircons were corrected for common Pb content using the measured <sup>204</sup>Pb. The ages were calculated using the constants recommended by the IUGS Subcommission on Geochronology (Steiger and Jäger <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1977" title="Steiger RH, Jäger E (1977) Subcommission on geochronology: convention on the use of decay constants in geo- and cosmochronology. Earth Planet Sci Lett 36:359–362" href="/article/10.1007/s00531-024-02474-y#ref-CR89" id="ref-link-section-d17672574e1171">1977</a>). The obtained results for Temora standards are characterised by high precision and accuracy of ca. 1% for each SHRIMP session. Most of the obtained ages for single analytical points for both the Temora standard and for each sample are with very low uncertainties up to 1% (1 sigma). For diagrams and concordia age calculation, zircon dates with discordance less than 20% were used. The concordia plots of SHRIMP results were prepared using ISOPLOT/EX (Ludwig <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2003" title="Ludwig KR (2003) User’s manual for Isoplot/EX Version 3.00. A geochronological toolkit for Microsoft Excel. Berkeley Geochronology Center, Special Publication No. 4:72pp" href="/article/10.1007/s00531-024-02474-y#ref-CR57" id="ref-link-section-d17672574e1175">2003</a>) whereas the probability density-distribution plots were prepared using the Excel’s macro prepared by Gehrels (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2007" title="Gehrels G (2007) Excel 2003 macro: normalized age probability plots. University of Arizona, Arizona Laser Chron Center, Tuscon. Accessed 12 Oct 2016" href="/article/10.1007/s00531-024-02474-y#ref-CR35" id="ref-link-section-d17672574e1178">2007</a>). The obtained results were filtered according to discordance and age as well as isotopic ratio uncertainty. The probability density plots were calculated using <sup>207</sup>Pb/<sup>206</sup>Pb ages for detrital grains older than 1000 Ma, and <sup>206</sup>Pb/<sup>238</sup>U ages for zircons younger than 1000 Ma, both with one sigma uncertainty.</p><div class="c-article-table" data-test="inline-table" data-container-section="table" id="table-1"><figure><figcaption class="c-article-table__figcaption"><b id="Tab1" data-test="table-caption">Table 1 List of samples dated in the present study</b></figcaption><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="table-link" data-track="click" data-track-action="view table" data-track-label="button" rel="nofollow" href="/article/10.1007/s00531-024-02474-y/tables/1" aria-label="Full size table 1"><span>Full size table</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div></div></div></section><section data-title="Results"><div class="c-article-section" id="Sec7-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="Sec7">Results</h2><div class="c-article-section__content" id="Sec7-content"><h3 class="c-article__sub-heading" id="Sec8">Petrographic characteristics of the samples</h3><p>Two samples of the ŁR subvolcanic intrusions below the GSRT, Lo1 and Go1, were collected from the two main rhyolite outcrops, from the dominant, massive, porphyritic lithology. The samples are almost identical in terms of their petrographic features and sample Go1 is shown in Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>a. The specimens are phenocryst-rich rocks with ca. 25% of phenocrysts typically a few mm in size (up to 15 mm). The phenocrysts are quartz (often embayed), alkali feldspar, albitized plagioclase, rarely biotite or pseudomorphs after hornblende(?). The groundmass is microcrystalline, felsitic, and consists of anhedral quartz and alkali feldspars with accessory apatite, local opaque aggregates and dispersed, fine-grained Fe-Ti oxides.</p><p>The other seven specimens represent the GSRT and were sampled from several locations along the GSRT outcrop, from various levels, from all main lithologies. Sample Pu2 represents the bedded tuffs and lapilli tuffs from the NW part of the GSRT outcrop. This sample can be classified as a lithic tuff. It consists of altered, hypo- to microcrystalline rhyolite clasts, dark brown to opaque in thin section, as well as feldspar and quartz grains (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>b). The clasts are angular to subrounded. The sample is relatively fine-grained and well-sorted (compared to other lapilli tuffs from this horizon), with compact framework and a slight alignment of clasts parallel to bedding. Some quartz crystals show embayments typical of pyrogenic quartz.</p><p>Three samples, Tl1, Wl1, Mi1, are massive nonwelded tuffs. First two, Tl1 and Wl1 (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>c), represent massive tuffs typical of the SE part of the basin. Thin sections reveal a characteristic crystalovitroclastic texture. Angular fragments of crystals of quartz, alkali feldspars and albitized plagioclase together with small pumice shards are loosely set in a finer matrix of platy, cuspate and bubble-wall, altered glass shards. The original volcanic glass is replaced by aggregates of quartz, calcite or dolomite and analcite with abundant haematite “pigment” in the finest fractions. Lithic clasts of microcrystalline rhyolites as well as mudstones/shales and trachyandesites are present is small amounts (a few percent). Sample Mi1 (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>d) was collected from an equivalent massive tuff lithology in the NW part of the basin. This sample shows similar primary components as samples Wl1 and Tl1 (broken phenocrysts, pumice shards, various types of glass shards, some lithic clasts) and textural features (e.g., poor sorting). The main differences are larger crystals of quartz and feldspars and the alteration mineral assemblage of the glass shards, which comprises quartz and alkali feldspar without analcite.</p><p>The last three samples, Gr1 (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>e), Mi2 (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>f) and Hy2, represent massive, welded tuffs from the uppermost part of the deposits in the NW to central part of the GSRT outcrop. Sample Mi2 shows the highest degree of welding with a typical eutaxitic texture (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>f). Larger pumice clasts are flattened and warped around subhedral, angular quartz and feldspar phenocrysts, whereas smaller glass shards are flattened and aligned. Glass shards are recrystallized into aggregates of acicular alkali feldspar and/or quartz oriented perpendicular of the margins of the shards (the axiolithic texture). Samples Hy2 and Gr1 (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig5">5</a>e), very similar in thin sections, are characterised by less distinctive flattening and alignment of glass shard and pumice, due to less pronounced welding and/or stronger recrystallization obscuring other textural features.</p><h3 class="c-article__sub-heading" id="Sec9">Zircon characteristics and SHRIMP dating</h3><p>Representative cathodoluminescence (CL) images of the studied zircons are shown in Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig6">6</a>. SHRIMP analytical results are reported in Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>. Figures <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig7">7</a>, <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig8">8</a>, and <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig9">9</a> show selected plots illustrating the results for the analysed samples. In all samples, each analytical spot (except two) was located in a separate zircon crystal.</p><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-6" data-title="Fig. 6"><figure><figcaption><b id="Fig6" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 6</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/6" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig6_HTML.jpg?as=webp"><img aria-describedby="Fig6" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig6_HTML.jpg" alt="figure 6" loading="lazy" width="685" height="967"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-6-desc"><p>Selected CL images of zircon crystals from the dated samples with analytical spots and dates obtained. Sample number, locations of analytical spots and dates obtained are indicated</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/6" data-track-dest="link:Figure6 Full size image" aria-label="Full size image figure 6" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-7" data-title="Fig. 7"><figure><figcaption><b id="Fig7" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 7</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/7" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig7_HTML.png?as=webp"><img aria-describedby="Fig7" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig7_HTML.png" alt="figure 7" loading="lazy" width="685" height="830"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-7-desc"><p>Results of dating shown in selected diagrams (depending on sample). <b>a</b> Sample Lo1, Tera–Wasserburg concordia diagram. <b>b</b> Sample Go1, Tera–Wasserburg concordia diagram. <b>c</b>–<b>f</b> sample Pu2, relative probability plot and Tera–Wasserburg concordia diagrams for three subpopulations of zircon crystals</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/7" data-track-dest="link:Figure7 Full size image" aria-label="Full size image figure 7" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-8" data-title="Fig. 8"><figure><figcaption><b id="Fig8" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 8</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/8" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig8_HTML.png?as=webp"><img aria-describedby="Fig8" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig8_HTML.png" alt="figure 8" loading="lazy" width="685" height="903"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-8-desc"><p>Results of dating shown in selected diagrams (depending on sample). <b>a</b>, <b>b</b> Sample Tl1, relative probability plot and Tera–Wasserburg concordia diagram for a subpopulation of zircon crystals. <b>c</b>, <b>d</b> Sample Wl1, relative probability plot and Tera–Wasserburg concordia diagram for a subpopulation of zircon crystals. <b>e</b> Sample Mi1, Tera–Wasserburg concordia diagram</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/8" data-track-dest="link:Figure8 Full size image" aria-label="Full size image figure 8" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-9" data-title="Fig. 9"><figure><figcaption><b id="Fig9" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 9</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/9" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig9_HTML.png?as=webp"><img aria-describedby="Fig9" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig9_HTML.png" alt="figure 9" loading="lazy" width="685" height="559"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-9-desc"><p>Results of dating shown in selected diagrams (depending on sample). <b>a</b>, <b>b</b> Sample Gr1, Tera–Wasserburg concordia diagram and mean age plot. <b>c</b> Sample Mi2, Tera–Wasserburg concordia diagram. <b>d</b> Sample Hy2, Tera–Wasserburg concordia diagram</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/9" data-track-dest="link:Figure9 Full size image" aria-label="Full size image figure 9" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><p>The zircon population recovered from the Lo1 sample of the ŁR is very homogeneous (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig6">6</a>). The crystals are prismatic, their length varies between 100 and 200 μm and the width from 50 up to 80 μm with the aspect ratio ranging from 1.85 to 2.5. They are dark and brown or transparent and pale-coloured (yellow). Almost all are characterised by the presence of growth, oscillatory zoning which is slightly visible in CL images. Zircons with evidence of dissolution and with inherited cores are not observed. The crystals were analysed in 22 spots (Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>a). The crystals have moderate U and Th contents (264–1361 ppm and 125–940 ppm, respectively). The Th/U ratio ranges from 0.37 up to 0.8. The SHRIMP results are concordant and the calculated concordia age for this sample is 298.4 ± 1.5 Ma (<i>n</i> = 21, MSWD = 0.45, probability = 0.5; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig7">7</a>a).</p><p>Zircons from the second sample of the ŁR, Go1, also represent a uniform population and are similar in shape and appearance to the sample Lo1 (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig6">6</a>). The size of zircon crystals varies between 100 and 220 μm in length and up to 50 μm (rarely 140 μm) in width with the aspect ratio from 1.6 to 2.1. The zircons are dark or brownish and rarely yellowish and transparent. They are prismatic with weak concentric zoning. Results from 19 analytical spots (Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>b) show that U and Th contents vary from 275 up to 1822 ppm and from 153 up to 799 ppm, respectively. The Th/U ratio is typical of igneous zircons and ranges from 0.55 to 0.82. The obtained results for 18 analytical spots are concordant and the calculated concordia age is 292.6 ± 1.9 Ma (<i>n</i> = 19, MSWD = 1.2, probability = 0.27; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig7">7</a>b). A single older crystal analysed shows the <sup>206</sup>Pb/<sup>238</sup>U age of 497 Ma.</p><p>The zircon crystals from the sample Pu2 of the bedded tuffs and lapilli tuffs do not form a homogeneous population. The sample contains transparent, pale-coloured as well as dark crystals. The zircons are mostly anhedral crystals and crystal fragments and the largest ones exceed 250 μm in length (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig6">6</a>). Some zircon grains are rounded or slightly rounded. In CL images a wide spectrum of textures is observed, such as oscillatory or growth zoning, sector zoning as well as inherited cores with evidence of dissolution. Data from 82 analytical spots (Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>c) indicate that the studied zircons have low or moderate U and Th contents (25–696 ppm and 8–262 ppm, respectively). The Th/U ratio is variable and ranges from 0.02 up to 1.3. Most of the analysed crystals have Carboniferous ages (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig7">7</a>c), where three concordant subpopulations can be observed. The concordia age calculated for the youngest subpopulation is 324.7 ± 1.7 Ma with very high MSWD and low probability (<i>n</i> = 14, MSWD = 5, probability = 0.029; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig7">7</a>d), whereas for the older subpopulation the concordia age is 333.5 ± 2.3 Ma with MSWD = 1.1 and probability = 0.15 (<i>n</i> = 19; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig7">7</a>e). The oldest subpopulation concordia age is 343.3 ± 3.7 Ma with overestimated MSWD and very high probability (<i>n</i> = 8, MSWD = 0.00097, probability = 0.98; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig7">7</a>f). The other, older crystals, which make up ca. 40% of the analysed zircons (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig7">7</a>c), show ages of ca. 450–490, 530–570, 600, 680, 1850, 2050, 2150 and 2600 Ma.</p><p>The zircons from sample Tl1 of the massive nonwelded tuffs do not form a uniform population. The sample contains transparent, pale-coloured as well as dark zircons. The anhedral zircon grains or their fragments are up to 200 μm in length (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig6">6</a>) and sometimes rounded or slightly rounded. There are oscillatory- or sector-zoned crystal as well as crystals with inherited cores or opaque minerals inclusions. Some crystals have evidence of dissolution. The analysed zircons (52 spots; Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>d) are characterised by low or moderate U and Th contents (32–696 ppm and 20–262 ppm, respectively). The Th/U ratio is variable, from 0.02 up to 1.3, which is typical for zircon of magmatic as well as metamorphic origin. The obtained zircon ages are very diverse (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig8">8</a>a). There are rare, relatively young crystals with ages of 287 to 302 Ma (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig8">8</a>a and Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>d), as well as an older subpopulation for which the concordia age is 321.2 ± 2.5 Ma (<i>n</i> = 7, MSWD = 2.7; probability = 0.1; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig8">8</a>b). However, the dominant zircon crystals provide older ages of ca. 330–340, 350–370, 490–510, 540–590, 640–680 Ma with single crystals dated at 946, 1600, 1850, 2000, 2100, 2250, 3086 Ma (Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>d).</p><p>Zircon crystals from the second sample of the massive nonwelded tuffs (Wl1), similar to the sample Tl1, do not represent a homogeneous assemblage. The crystals are slightly rounded to rounded but fragments of crystals are found as well. The crystals vary from transparent and colourless through pale-coloured to almost completely dark. The length of crystals ranges from 40 to 90 μm, rarely up to 180 μm. In CL (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig6">6</a>), there is a notable spectrum of zoning textures, from typical growth zoning to sector zoning. There are also crystals with distinctive inherited cores. Several crystals of likely metamorphic origin show evidence of dissolution. The zircon crystals analysed in 32 spots (Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>e) have diverse contents of U and Th (45–1339 ppm and 8–679 ppm, respectively) as well as Th/U ratios (0.02–1.24). Half of the analysed crystals have Permian or Carboniferous ages, where two intervals of higher frequency can be observed, clustering around ca. 302 Ma (5 crystals) and 327 Ma (10 crystals; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig8">8</a>c, d). The concordia age calculated for the latter, more numerous subpopulation, is 327.2 ± 2.2 Ma (<i>n</i> = 8, MSWD = 9.9, probability = 0.002; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig8">8</a>d). The other, older zircons provide variable ages of ca. 330–340, 470–490, 490–510, 513, 540–560, 620 and 913 Ma (Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>e).</p><p>Compared to the two samples characterised above, the zircon population in the third sample of the nonwelded tuffs, Mi1, is very homogeneous. The length of zircon crystals varies between 160 and 220 μm and the typical width is about 80 μm, with the aspect ratio ranging from 2 to 2.75. Generally, these are dark and brown to transparent and pale-coloured, prismatic crystals. Oscillatory zoning is visible in CL images. Inherited cores are not observed. Some crystals have apatite inclusions. The zircons studied in 44 analytical spots (Tab. <a data-track="click" data-track-label="link" data-track-action="table anchor" href="/article/10.1007/s00531-024-02474-y#Tab1">1</a>f) have moderate U and Th contents (399–893 ppm and 100–576 ppm, respectively). The Th/U ratio ranging from 0.46 up to 0.83 is typical of igneous zircons. The calculated concordia age for this sample is 297.2 ± 0.9 Ma (<i>n</i> = 34, MSWD = 1.5, probability = 0.6; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig8">8</a>e).</p><p>The zircon crystals from the sample Gr1 of massive, welded tuffs represent a homogeneous population. The crystals are transparent, pale coloured or dark brownish, prismatic, with weak oscillatory zoning in CL images (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig6">6</a>). The length of crystals varies between 120 and 200 μm and the width from 60 up to 80 μm, with the aspect ratio ranging from 2 up to 2.5. The studied zircons (38 analytical spots; Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>g) have moderate U and Th contents of 291–483 ppm and 131–361 ppm, respectively. Their Th/U ratios ranging from 0.48 up to 0.82 are typical of igneous zircons. Although the results obtained are quite concordant, it was not possible to calculate the concordia age (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig9">9</a>a). However, the calculated mean <sup>206</sup>Pb/<sup>238</sup>U age is 300.5 ± 2.0 Ma with slightly overestimated MSWD and very high probability (<i>n</i> = 38, MSWD = 0.43, probability = 0.999; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig9">9</a>b).</p><p>The zircons crystals from the second sample of massive, welded tuffs (Mi2) are similar to the previous sample. The zircon population is homogeneous and contains transparent, pale coloured or dark brownish prismatic crystals with weak oscillatory zoning in CL images (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig6">6</a>). The size of crystals varies between 120 and 200 μm in length and between 60 to 80 μm in width, with the aspect ratio in the range of 2–2.5. Analysis in 22 spots (Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>h) shows that the U and Th contents vary from 377 up to 1091 ppm and from 158 up to 754 ppm, respectively. The Th/U ratio ranging from 0.46 up to 0.78 is typical of igneous zircons. The results are concordant and the calculated concordia age is 300.5 ± 1.4 Ma (<i>n</i> = 22, MSWD = 6.5, probability = 0.011; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig9">9</a>c).</p><p>Zircon crystals from the third sample of massive, welded tuffs (Hy2) are similar to the two other samples discussed above. The zircon population is homogeneous and contains transparent, pale-coloured or brownish, prismatic crystals with weak oscillatory or sector zoning in CL images. The length of crystals varies between 120 and 200 μm and the width from 60 up to 80 μm, with the aspect ratio from 2 to 2.5. The zircon crystals have low U and Th contents (133–384 ppm and 94–352 ppm, respectively; Supp. Tab. <a data-track="click" data-track-label="link" data-track-action="supplementary material anchor" href="/article/10.1007/s00531-024-02474-y#MOESM1">1</a>i). The Th/U ratio ranges from 0.47 up to 0.7, which is typical of igneous zircon. The SHRIMP results are concordant and the calculated concordia age for this sample is 298.0 ± 1.6 Ma (<i>n</i> = 13, MSWD = 6, probability = 0.014; Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig9">9</a>d).</p></div></div></section><section data-title="Discussion"><div class="c-article-section" id="Sec10-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="Sec10">Discussion</h2><div class="c-article-section__content" id="Sec10-content"><h3 class="c-article__sub-heading" id="Sec11">Emplacement age of the Góry Suche Rhyolitic Tuffs and Łomnica Rhyolites</h3><p>Zircon assemblages in three of the analysed samples: Pu2, Tl1, Wl1, are heterogeneous in terms of textural and geochemical features. Relatively young crystals dated at ca. 287–310 Ma are rare and much older crystals strongly predominate (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig10">10</a>). The younger zircons possibly provide some information on the emplacement age of the tuffs, but the predominant, old crystals are clearly xenocrysts of various origins (see the next section below). Zircon assemblages in the other six samples are much more homogeneous and their CL features as well as U and Th contents and ratios are typical of zircon crystallised from silicic magma. Zircon xenocrysts were not identified in these samples with exception of a single crystal in sample Go1. Zircon crystals in five of these samples (Lo1, Go1, Mi1, Mi2, Hy2) provide well-defined concordia ages, whereas for one sample (Gr1) a mean age was obtained. These ages, in the range of 300.5 ± 2.0 Ma–292.6 ± 1.9 Ma, are plotted in a simplified log of the GSRT (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig4">4</a>) and against the international chronostratigraphic scale (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig11">11</a>).</p><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-10" data-title="Fig. 10"><figure><figcaption><b id="Fig10" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 10</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/10" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig10_HTML.png?as=webp"><img aria-describedby="Fig10" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig10_HTML.png" alt="figure 10" loading="lazy" width="685" height="467"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-10-desc"><p>Probability density plots of zircon ages determined in samples Pu2, Tl1, Wl1. Two younger age groups of xenocrysts (see text) are indicated by yellow shading</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/10" data-track-dest="link:Figure10 Full size image" aria-label="Full size image figure 10" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-11" data-title="Fig. 11"><figure><figcaption><b id="Fig11" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 11</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/11" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig11_HTML.png?as=webp"><img aria-describedby="Fig11" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig11_HTML.png" alt="figure 11" loading="lazy" width="685" height="604"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-11-desc"><p>The results of SHRIMP U–Pb zircon dating reported in this paper shown against the International Chronostratigraphic Scale (ICS: Cohen et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2013" title="Cohen KM, Finney SC, Gibbard PL, Fan J-X (2013) The ICS international chronostratigraphic chart. Episodes 36:199–204" href="/article/10.1007/s00531-024-02474-y#ref-CR27" id="ref-link-section-d17672574e1921">2013</a>, updated) and the Western European lithostratigraphic subdivision (WE: after Oplustil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e1924">2016a</a>). Other datings of Permo-Carboniferous volcanic rocks of the Intra-Sudetic Basin, the North-Sudetic Basin as well as selected granites are plotted for comparison</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/11" data-track-dest="link:Figure11 Full size image" aria-label="Full size image figure 11" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><p>A possible issue in further interpretation are the uncertainties on the ages obtained. The typical precision and accuracy of zircon U–Pb SHRIMP ages are around 1% (2σ) (e.g., Schaltegger et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2015" title="Schaltegger U, Schmidt AK, Horstwood MSA (2015) U–Th–Pb zircon geochronology by ID-TIMS, SIMS, and laser ablation ICP-MS: recipes, interpretations, and opportunities. Chem Geol 402:98–110" href="/article/10.1007/s00531-024-02474-y#ref-CR85" id="ref-link-section-d17672574e1938">2015</a>; Magee et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2023" title="Magee CW, Bodorkos S, Lewis J, Crowley JL, Wall CJ, Friedman RM (2023) Examination of the accuracy of SHRIMP U-Pb geochronology based on samples dated by both SHRIMP and CA-TIMS. Geochronology 5:1–19" href="/article/10.1007/s00531-024-02474-y#ref-CR59" id="ref-link-section-d17672574e1941">2023</a>), whereas the uncertainties discussed here tend to be lower. However, in our samples Lo1, Go1, Mi1, Mi2, Gr1, Hy2, the analysed crystals show moderate uranium contents, favourable for relatively low analytical errors in individual spots. The zircon populations are homogeneous in terms of textural and chemical features and this reduces spread in measurements. We have also measured a large number of crystals in each of the samples (mean <i>n</i> = 25) and this improves the data set for concordia or mean age calculations. We consider that all these factors contribute to the quality of the results obtained and to the relatively low uncertainties.</p><p>Thus, the dates from four ignimbrite samples Mi2, Gr1, Hy2 and Mi1 indicate that the eruption and deposition of the GSRT occurred between 300.5 ± 2.0 and 297.2 ± 0.9 Ma. The ages of these samples only partly overlap within the relatively small uncertainties of ± 1–2 Ma reported here. A straightforward interpretation would suggest a prolonged duration of the GSRT ignimbrite volcanism of ca. 3–6 My (if uncertainties are included). However, large-scale ignimbrite-forming eruptions are geologically instantaneous events that last only weeks to months in the climax stage (Wilson <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2008" title="Wilson CJN (2008) Supereruptions and supervolcanoes: processes and products. Elements 4:29–34" href="/article/10.1007/s00531-024-02474-y#ref-CR105" id="ref-link-section-d17672574e1950">2008</a>). Such eruptions are linked to collapse calderas being part of long-lived magmatic systems that may remain active for a few million years, resulting in complex successions of pyroclastic deposits and lavas formed in several eruptions, separated by repose periods dominated by erosion, redeposition, development of soil horizons (e.g., Cas and Wright <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1987" title="Cas RAF, Wright JV (1987) Volcanic successions: modern and ancient: a geological approach to processes, products and successions. Allen and Unwin" href="/article/10.1007/s00531-024-02474-y#ref-CR24" id="ref-link-section-d17672574e1953">1987</a>). In this context, several million years of eruptive and depositional activity is not apparent in the case of GSRT. The lithological and petrographic variation of the GSRT seems relatively simple and there is no evidence of palaeosoil horizons which would delineate successive eruptive units and longer repose periods. On the other hand, there are differences between deposits in the NW and SE of the GSRT outcrop: these in the NW are thicker, more variable (widespread bedded tuffs, common welded ignimbrites) and the ignimbrite samples contain abundant juvenile zircon but no xenocrystic zircon—whereas the deposits in the SE show opposite characteristics. Some of these features may partly reflect e.g., facies variation at different distance from eruptive vents, but may also indicate the presence of separate eruptive units. Nevertheless, the spread of ages between samples Mi2, Gr1, Hy2 and Mi1 cannot be easily explained by e.g., two or more successive ignimbrite-forming eruptions. However, the presence of zircon antecrysts (i.e. older zircon crystals formed in earlier stages of crystallisation and recycled in the same magmatic system) in some of the analysed samples may offset the dates towards older ages, whereas some Pb loss from zircons in other specimens may cause a shift towards younger ages (Miller et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2007" title="Miller J, Matzel J, Miller C, Burgess S, Miller R (2007) Zircon growth and recycling during the assembly of large, composite arc plutons. J Volcanol Geotherm Res 167:282–299" href="/article/10.1007/s00531-024-02474-y#ref-CR67" id="ref-link-section-d17672574e1956">2007</a>; Schaltegger et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2015" title="Schaltegger U, Schmidt AK, Horstwood MSA (2015) U–Th–Pb zircon geochronology by ID-TIMS, SIMS, and laser ablation ICP-MS: recipes, interpretations, and opportunities. Chem Geol 402:98–110" href="/article/10.1007/s00531-024-02474-y#ref-CR85" id="ref-link-section-d17672574e1959">2015</a> and references therein). The exact reasons are hard to specify based on our data.</p><p>The two analysed ŁR samples, Lo1 and Go1, are easier for interpretation. These samples contain homogeneous zircon populations with textural and chemical features typical of zircon crystallised from silicic melts. The concordia ages suggest the emplacement of the rhyolites in two episodes at 298.4 ± 1.5 Ma and 292.6 ± 1.9 Ma. The intrusion of two separate magma batches is consistent with the presence of two subvolcanic bodies from which the samples were collected. The time span of up to ca. 9 My (including uncertainties) between the two intrusive episodes seems relatively long considering the small size and similarities of the two sills. However, our data do not show evidence of e.g., Pb loss or other disturbance of the U–Pb system, so the ages obtained are considered geologically significant. The ages are also consistent with geological evidence suggesting intrusion of the rhyolites after the deposition of the GSRT (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e1965">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e1968">b</a>).</p><p>Summing up, our SHRIMP results and the geological context indicate that GSRT ignimbrites formed between 300.5 ± 2.0 Ma and 297.2 ± 0.9 Ma. The ages obtained cluster around the Carboniferous/Permian boundary. Geological data suggest that the eruption and deposition of the GSRT was relatively simple, geologically instantaneous event, without long repose periods separating successive eruptions. The exact emplacement age of the GSRT cannot be specified precisely, but we consider that the mean age of samples Mi1, Mi2, Gr1, Hy2 of 299 Ma approximates the age of the GSRT event. The eruption of the GSRT was followed (partly overlapped?) by the emplacement of the ŁR as sills in two episodes at 298.4 ± 2.0 Ma and 292.6 ± 1.9 Ma.</p><h3 class="c-article__sub-heading" id="Sec12">Zircon xenocrysts in the Góry Suche Rhyolitic Tuffs</h3><p>Three of the analysed samples, Pu2, Tl1 and Wl1, contain zircon crystal assemblages with ages over ca. 310 Ma and heterogeneous in terms of textural features and U and Th ratios and contents, which are interpreted as xenocrysts. Probability density plots of ages determined in these samples are compared in Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig10">10</a>. The age distributions are similar and the xenocrysts can be subdivided into the following main groups:</p><ol class="u-list-style-none"> <li> <span class="u-custom-list-number">1.</span> <p>320–400 Ma (Carboniferous to Devonian), including several subgroups clustering around ca. 325, 335, 365 Ma and older, depending on sample,</p> </li> <li> <span class="u-custom-list-number">2.</span> <p>425–680 Ma (Silurian to Neoproterozoic)—in all three samples and also a single grain in Go1,</p> </li> <li> <span class="u-custom-list-number">3.</span> <p>ca. 900–1000 and 1600–2600 Ma (mainly Palaeoproterozoic)—rare crystals mainly in Pu2 and Tl1.</p> </li> </ol><p>These zircon xenocrysts can be linked to partial melting and differentiation processes that formed the silicic GSRT magma, and/or to the eruption and emplacement processes of the GSRT tephra, including mechanical interaction with the basement rocks and the intrabasinal sedimentary cover. The textural and chemical features of the zircons are indicative of magmatic as well as metamorphic origin and rounding of some grains points to derivation from sedimentary and/or metasedimentary sources. The range of ages and the characteristic lack of Mesoproterozoic zircons compares well to zircon age spectra in crystalline basement rocks outcropping around the Intra-Sudetic Basin in the Góry Sowie, Orlica-Śnieżnik and Karkonosze-Izera massifs (e.g., Jastrzębski et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2010" title="Jastrzębski M, Żelaźniewicz A, Nowak I, Murtezi M, Larionov AN (2010) Protolith age and provenance of metasedimentary rocks in Variscan allochthon units: U/Pb SHRIMP zircon data from the Orlica-Śnieżnik Dome, West Sudetes. Geol Mag 147(3):416–433" href="/article/10.1007/s00531-024-02474-y#ref-CR44" id="ref-link-section-d17672574e2024">2010</a>; Mazur et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2012" title="Mazur S, Szczepański J, Turniak K, McNaughton NJ (2012) Location of the Rheic suture in the eastern Bohemian Massif: evidence from detrital zircon data. Terra Nova 24(3):199–206" href="/article/10.1007/s00531-024-02474-y#ref-CR62" id="ref-link-section-d17672574e2027">2012</a>; Szczepański et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2020" title="Szczepański J, Turniak K, Anczkiewicz R, Gleichner P (2020) Dating of detrital zircons and tracing the provenance of quartzites from the Bystrzyckie Mts: implications for tectonic setting of the Early Palaeozoic sedimentary basin developed on the Gondwana margin. Int J Earth Sci 109:2049–2079" href="/article/10.1007/s00531-024-02474-y#ref-CR90" id="ref-link-section-d17672574e2030">2020</a>; Tabaud et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2021" title="Tabaud AS, Štípská P, Mazur S, Schulmann K, Míková J, Wong J, Sun M (2021) Evolution of a Cambro-Ordovician active margin in northern Gondwana: geochemical and zircon geochronological evidence from the Góry Sowie metasedimentary rocks, Poland. Gondwana Res 90:1–26" href="/article/10.1007/s00531-024-02474-y#ref-CR91" id="ref-link-section-d17672574e2033">2021</a>). The ages of the youngest xenocrysts (group 1) are similar to zircon ages in orogenic to post-orogenic, mainly Carboniferous granites in the Sudetes and in areas further south in the Bohemian Massif (e.g., Finger et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2009" title="Finger F, Gerdes A, René M, Riegler G (2009) The Saxo-Danubian Granite Belt: magmatic response to post-collisional delamination of mantle lithosphere below the south-western sector of the Bohemian Massif (Variscan orogen). Geol Carpath 60:205–212" href="/article/10.1007/s00531-024-02474-y#ref-CR33" id="ref-link-section-d17672574e2036">2009</a>; Laurent et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2014" title="Laurent A, Janoušek V, Magna T, Schulmann K, Míková J (2014) Petrogenesis and geochronology of a post-orogenic calc-alkaline magmatic association: the Žulová Pluton, Bohemian Massif. J Geosci 59:415–440" href="/article/10.1007/s00531-024-02474-y#ref-CR51" id="ref-link-section-d17672574e2040">2014</a>; Jokubauskas et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2018" title="Jokubauskas P, Bagiński B, Macdonald R, Krzemińska E (2018) Multiphase magmatic activity in the Variscan Kłodzko-Złoty Stok intrusion, Polish Sudetes: evidence from SHRIMP U-Pb zircon ages. Int J Earth Sci 107(5):1623–1639" href="/article/10.1007/s00531-024-02474-y#ref-CR46" id="ref-link-section-d17672574e2043">2018</a>). The presence of distinctive subpopulations, such as 321–327, 333, 343 Ma may indicate zircon derivation from some localised sources, like individual plutonic complexes (e.g., the plutons of the Saxo-Danubian Granite Belt dated at 330–320 Ma; Finger et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2009" title="Finger F, Gerdes A, René M, Riegler G (2009) The Saxo-Danubian Granite Belt: magmatic response to post-collisional delamination of mantle lithosphere below the south-western sector of the Bohemian Massif (Variscan orogen). Geol Carpath 60:205–212" href="/article/10.1007/s00531-024-02474-y#ref-CR33" id="ref-link-section-d17672574e2046">2009</a>). The older xenocrysts, of group 2 could have been derived from orthogneisses, originating from the Cadomian and Cambro-Ordovician granites widespread in the Sudetes (e.g., Pin et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2007" title="Pin C, Kryza R, Oberc-Dziedzic T, Mazur S, Turniak K (2007) The diversity and geodynamic significance of Late Cambrian (ca. 500 Ma) felsic anorogenic magmatism in the northern part of the Bohemian Massif: a review based on Sm-Nd isotope and geochemical data. In: Linnemann U, Nance RD, Kraft P, Zulauf G (eds) The evolution of the Rheic Ocean: from Avalonian-Cadomian active margin to Alleghenian-Variscan collision, vol 423. Geological Society of America, Special Paper, pp 209–229" href="/article/10.1007/s00531-024-02474-y#ref-CR80" id="ref-link-section-d17672574e2049">2007</a>) or from younger (meta)sedimentary rock derived from such rocks. The origin of the oldest, Palaeoproterozic xenocrysts (group 3) can be ultimately linked to older Precambrian rocks complexes of the Bohemian Massif.</p><p>The wide range of the xenocrystic zircon ages and their various possible derivation can be best explained by mixing of the GSRT tephra with zircon-bearing siliciclastic sedimentary rocks, such as the sedimentary fill of the Intra-Sudetic Basin. The Permo-Carboniferous depositional systems of the basin were supplied by detritus from both local crystalline basement complexes, as well as from more distant source areas in the south (cf. Wojewoda and Mastalerz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1989" title="Wojewoda J, Mastalerz K (1989) Ewolucja klimatu oraz allocykliczność i autocykliczność sedymentacji na przykładzie osadów kontynentalnych górnego karbonu i permu w Sudetach. Przegląd Geologiczny 37(4):173–180" href="/article/10.1007/s00531-024-02474-y#ref-CR107" id="ref-link-section-d17672574e2055">1989</a>). Although there is no direct data on zircon age spectra of the Permo-Carbonifeorus sedimentary rocks of the Intra-Sudetic Basin so far, a heterogeneous assemblage of various basement-derived zircons may be expected. The mixing of the GSRT tephra with the intrabasinal, sediments could have preferentially occurred during the explosive eruption of the GSRT from vents located inside the basin (cf. Romero et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2023" title="Romero L, Petronis MS, Awdankiewicz M, Rapprich V (2023) Emplacement of Caldera-Related Rhyolitic Ignimbrite in a Variscan post-orogenic basin—constraints from paleomagnetic and anisotropy of magnetic susceptibility data from the Permian Gory Suche Rhyolitic Tuff. AGU23, 11–15 Dec, GP11B-0469. 
 https://agu.confex.com/agu/fm23/meetingapp.cgi/Paper/1377413
 
 " href="/article/10.1007/s00531-024-02474-y#ref-CR83" id="ref-link-section-d17672574e2058">2023</a>)—such vent must have cut through the sedimentary cover. However, some of the xenocrysts may also be derived from greater depths in the underlying crystalline basement rocks. Also a post-eruptive redeposition and mixing of juvenile tephra with non-volcanic detritus in the intrabasinal alluvial system could have contributed to the wide variation in some specimens, such as Pu2. In addition, the variable zircon assemblages—with abundant zircon xenocrysts in samples from the SE and the lack of xenocrysts in samples from the NW (similar results in Awdankiewicz and Kryza <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2010" title="Awdankiewicz M, Kryza R (2010) The Góry Suche Rhyolitic Tuffs (Intra-Sudetic Basin, SW Poland): preliminary SHRIMP zircon age. Mineral Spec Pap 37:70" href="/article/10.1007/s00531-024-02474-y#ref-CR9" id="ref-link-section-d17672574e2061">2010</a>; Awdankiewicz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2011" title="Awdankiewicz H, Awdankiewicz M, Kryza R (2011) Abundant xenocrystic zircon and rare juvenile zircon in rhyolitic ignimbrites: preliminary SHRIMP data from the Lower Permian of the Intra-Sudetic Basin (SW Poland). Mineral Spec Pap 38:69–70" href="/article/10.1007/s00531-024-02474-y#ref-CR2" id="ref-link-section-d17672574e2064">2011</a>)—may reflect the presence of separate depositional units of the ignimbrites.</p><h3 class="c-article__sub-heading" id="Sec13">The age of the Góry Suche Rhyolitic Tuffs and Łomnica Rhyolites in regional context</h3><p>In Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig12">12</a> our dating results are compared to other published U–Pb zircon ages of Permo-Carboniferous volcanic rocks from Central Europe. The eruption and emplacement of the GSRT and the ŁR can be correlated to the regional "magmatic flare-up" spanning the latest Carboniferou and the early Permian (Breitkreuz and Kennedy <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999" title="Breitkreuz C, Kennedy A (1999) Magmatic flare-up at the Carboniferous/Permian boundary in the NE German Basin revealed by SHRIMP zircon ages. Tectonophysics 302:307–326" href="/article/10.1007/s00531-024-02474-y#ref-CR21" id="ref-link-section-d17672574e2078">1999</a>). The “flare-up” and the preceding Late Carboniferous volcanism included voluminous ignimbrite, caldera-related eruptions (Benek et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1996" title="Benek R, Kramer W, McCann T, Scheck M, Negendank JFW, Korich D, Huebscher HD, Bayer U (1996) Permo-Carboniferous magmatism of the Northeast German Basin. Tectonophysics 266:379–404" href="/article/10.1007/s00531-024-02474-y#ref-CR13" id="ref-link-section-d17672574e2081">1996</a>; Breitkreuz and Kennedy <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999" title="Breitkreuz C, Kennedy A (1999) Magmatic flare-up at the Carboniferous/Permian boundary in the NE German Basin revealed by SHRIMP zircon ages. Tectonophysics 302:307–326" href="/article/10.1007/s00531-024-02474-y#ref-CR21" id="ref-link-section-d17672574e2084">1999</a>). Amongst the most intensely studied is the Teplice Rhyolite—an ignimbrite fill of the Late Carboniferous Altenberg-Teplice caldera, 35 × 18 km in size. The intracaldera Teplice Rhyolite volume was estimated at min. 350 km<sup>3</sup> (DRE, Dense Rock Equivalent; Tomek et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="Tomek F, Opluštil S, Svojtka M, Špillar V, Rapprich V, Míková J (2022) Altenberg-Teplice Caldera sourced Westphalian fall tuffs in the central and western Bohemian Carboniferous basins (eastern Variscan belt). Int Geol Rev 64:441–468" href="/article/10.1007/s00531-024-02474-y#ref-CR94" id="ref-link-section-d17672574e2090">2022</a>). Using LA ICP-MS U–Pb zircon dating Casas-García et al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2019" title="Casas-García R, Rapprich V, Breitkreuz C, Svojtka M, Lapp M, Stanek K, Hofmann M, Linnemann U (2019) Lithofacies architecture, composition, and age of the Carboniferous Teplice Rhyolite (German-Czech border): Insights into the evolution of the Altenberg-Teplice Caldera. J Volcanol Geoth Res 386:106662" href="/article/10.1007/s00531-024-02474-y#ref-CR25" id="ref-link-section-d17672574e2093">2019</a>) found that the ignimbrite formed in three main eruptions over 8 My between 325 and 317 Ma. Using the same method, a narrower time span of ca. 5 My for this activity, between 318 and 313 Ma, with a peak at 314–313 Ma, was suggested by Tomek et al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="Tomek F, Opluštil S, Svojtka M, Špillar V, Rapprich V, Míková J (2022) Altenberg-Teplice Caldera sourced Westphalian fall tuffs in the central and western Bohemian Carboniferous basins (eastern Variscan belt). Int Geol Rev 64:441–468" href="/article/10.1007/s00531-024-02474-y#ref-CR94" id="ref-link-section-d17672574e2096">2022</a>). Tichomirowa et al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="Tichomirowa M, Käßner A, Repstock A, Weber S, Gerdes A, Whitehouse M (2022) New CA-ID-TIMS U–Pb zircon ages for the Altenberg-Teplice Volcanic Complex (ATVC) document discrete and coeval pulses of Variscan magmatic activity in the Eastern Erzgebirge (Eastern Variscan Belt). Int J Earth Sci 111:1885–1908" href="/article/10.1007/s00531-024-02474-y#ref-CR92" id="ref-link-section-d17672574e2099">2022</a>), based on the precise CA ID TIMS dating method, found that the Teplice rhyolite formed during a shorter time interval of 1–2 My at 314–313 Ma, with younger rhyolite dikes emplaced at 314 and 311 Ma, and the total period of dated activity of ca. 3 My.</p><div class="c-article-section__figure js-c-reading-companion-figures-item" data-test="figure" data-container-section="figure" id="figure-12" data-title="Fig. 12"><figure><figcaption><b id="Fig12" class="c-article-section__figure-caption" data-test="figure-caption-text">Fig. 12</b></figcaption><div class="c-article-section__figure-content"><div class="c-article-section__figure-item"><a class="c-article-section__figure-link" data-test="img-link" data-track="click" data-track-label="image" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/12" rel="nofollow"><picture><source type="image/webp" srcset="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig12_HTML.png?as=webp"><img aria-describedby="Fig12" src="//media.springernature.com/lw685/springer-static/image/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_Fig12_HTML.png" alt="figure 12" loading="lazy" width="685" height="581"></picture></a></div><div class="c-article-section__figure-description" data-test="bottom-caption" id="figure-12-desc"><p>The new SHRIMP ages from this study compared with published zircon ages from other Late Carboniferous–Early Permian volcanic rocks from Central Europe (data from: Breitkreuz and Kennedy <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999" title="Breitkreuz C, Kennedy A (1999) Magmatic flare-up at the Carboniferous/Permian boundary in the NE German Basin revealed by SHRIMP zircon ages. Tectonophysics 302:307–326" href="/article/10.1007/s00531-024-02474-y#ref-CR21" id="ref-link-section-d17672574e2112">1999</a>; Breitkreuz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2007" title="Breitkreuz C, Kennedy A, Geißler M, Ehling B-C, Kopp J, Muszynski A, Protas A, Stouge S (2007) Far Eastern Avalonia: its chronostratigraphic structure revealed by SHRIMP zircon ages from Upper Carboniferous to Lower Permian volcanic rocks (drill cores from Germany, Poland and Denmark). Geol Soc Am Spec Pap 423:173–190" href="/article/10.1007/s00531-024-02474-y#ref-CR22" id="ref-link-section-d17672574e2115">2007</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2009" title="Breitkreuz C, Ehling B-C, Sergeev S (2009) Chronological evolution of an intrusive/extrusive system: the Late Paleozoic Halle Volcanic Complex in the north-eastern Saale Basin (Germany). Zeitschrift der Deutschen Gesellschaft Für Geowissenschaften 160:173–190" href="/article/10.1007/s00531-024-02474-y#ref-CR19" id="ref-link-section-d17672574e2118">2009</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2021" title="Breitkreuz C, Käßner A, Tichomirowa M, Lapp M, Huang S, Stanek K (2021) The Late Carboniferous deeply eroded Tharandt Forest caldera–Niederbobritzsch granite complex: a post-Variscan long-lived magmatic system in central Europe. Int J Earth Sci 110:1265–1292" href="/article/10.1007/s00531-024-02474-y#ref-CR20" id="ref-link-section-d17672574e2121">2021</a>; Nawrocki et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2008" title="Nawrocki J, Fanning M, Lewandowska A, Polechońska O, Werner T (2008) Palaeomagnetism and the age of the Cracow volcanic rocks (S Poland). Geophys J Int 174:475–488" href="/article/10.1007/s00531-024-02474-y#ref-CR68" id="ref-link-section-d17672574e2124">2008</a>; Hoffmann et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2013" title="Hoffmann U, Breitkreuz C, Breiter K, Sergeev S, Stanek K, Tichomirowa M (2013) Carboniferous-Permian volcanic evolution in Central Europe—U/Pb ages of volcanic rocks in Saxony (Germany) and northern Bohemia (Czech Republic). Int J Earth Sci (Geologische Rundschau) 102:73–99" href="/article/10.1007/s00531-024-02474-y#ref-CR42" id="ref-link-section-d17672574e2128">2013</a>; Kryza and Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2012" title="Kryza R, Awdankiewicz M (2012) Ambiguous geological position of Carboniferous rhyodacites in the Intra-Sudetic Basin (SW Poland) clarified by SHRIMP zircon ages. Geol Q 56:55–66" href="/article/10.1007/s00531-024-02474-y#ref-CR49" id="ref-link-section-d17672574e2131">2012</a>; Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e2134">2016a</a>; Casas-García et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2019" title="Casas-García R, Rapprich V, Breitkreuz C, Svojtka M, Lapp M, Stanek K, Hofmann M, Linnemann U (2019) Lithofacies architecture, composition, and age of the Carboniferous Teplice Rhyolite (German-Czech border): Insights into the evolution of the Altenberg-Teplice Caldera. J Volcanol Geoth Res 386:106662" href="/article/10.1007/s00531-024-02474-y#ref-CR25" id="ref-link-section-d17672574e2137">2019</a>; Lützner et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2021" title="Lützner H, Tichomirowa M, Käßner A, Gaupp R (2021) Latest Carboniferous to early Permian volcano-stratigraphic evolution in Central Europe: U-Pb CA–ID–TIMS ages of volcanic rocks in the Thuringian Forest Basin (Germany). Int J Earth Sci 110:377–398" href="/article/10.1007/s00531-024-02474-y#ref-CR58" id="ref-link-section-d17672574e2140">2021</a>; Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="Awdankiewicz M (2022) Polyphase Permo-Carboniferous magmatism adjacent to the Intra-Sudetic Fault: constraints from U-Pb SHRIMP zircon study of felsic subvolcanic intrusions in the Intra-Sudetic Basin, SW Poland. Int J Earth Sci 111:2199–2224" href="/article/10.1007/s00531-024-02474-y#ref-CR6" id="ref-link-section-d17672574e2143">2022</a>; Tichomirowa et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="Tichomirowa M, Käßner A, Repstock A, Weber S, Gerdes A, Whitehouse M (2022) New CA-ID-TIMS U–Pb zircon ages for the Altenberg-Teplice Volcanic Complex (ATVC) document discrete and coeval pulses of Variscan magmatic activity in the Eastern Erzgebirge (Eastern Variscan Belt). Int J Earth Sci 111:1885–1908" href="/article/10.1007/s00531-024-02474-y#ref-CR92" id="ref-link-section-d17672574e2147">2022</a>; Tomek et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2022" title="Tomek F, Opluštil S, Svojtka M, Špillar V, Rapprich V, Míková J (2022) Altenberg-Teplice Caldera sourced Westphalian fall tuffs in the central and western Bohemian Carboniferous basins (eastern Variscan belt). Int Geol Rev 64:441–468" href="/article/10.1007/s00531-024-02474-y#ref-CR94" id="ref-link-section-d17672574e2150">2022</a>; Löcse et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2023" title="Löcse F, Schneider G, Linnemann U, Rößler R (2023) Carboniferous-Permian volcanic evolution in the mid-European Variscides: U–Pb LA-ICP-MS zircon ages, geochemical and petrographical constraints from the NW Saxonian Volcanic Basin (Germany). Z Dt Ges Geowiss (j Appl Reg Geol) 174(1):7–30" href="/article/10.1007/s00531-024-02474-y#ref-CR53" id="ref-link-section-d17672574e2153">2023</a>)</p></div></div><div class="u-text-right u-hide-print"><a class="c-article__pill-button" data-test="article-link" data-track="click" data-track-label="button" data-track-action="view figure" href="/article/10.1007/s00531-024-02474-y/figures/12" data-track-dest="link:Figure12 Full size image" aria-label="Full size image figure 12" rel="nofollow"><span>Full size image</span><svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="#icon-eds-i-chevron-right-small"></use></svg></a></div></figure></div><p>Another example is provided by the study of the Late Carboniferous Tharandt Forest Caldera (10 km across) and related ignimbrite, with the preserved intra-caldera DRE volume of 22 km<sup>3</sup> (Breitkreuz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2021" title="Breitkreuz C, Käßner A, Tichomirowa M, Lapp M, Huang S, Stanek K (2021) The Late Carboniferous deeply eroded Tharandt Forest caldera–Niederbobritzsch granite complex: a post-Variscan long-lived magmatic system in central Europe. Int J Earth Sci 110:1265–1292" href="/article/10.1007/s00531-024-02474-y#ref-CR20" id="ref-link-section-d17672574e2169">2021</a>). Precise CA-ID-TIMS ages (op. cit.) indicate that the emplacement of ignimbrites spanned at least 1.5 My (313.4–311.9 Ma). Slightly older subvolcanic intrusions (ring dikes) emplaced at 314.5 Ma extend the period of volcanic and subvolcanic activity to 2.6 My, and considering also the pre-caldera but co-genetic granites dated at 319.5 and 318.2 Ma the activity of this magmatic system spanned 7.6 My.</p><p>The two above examples illustrate the characteristic duration and timing of ignimbrite, caldera-related magmatism: overall long periods of activity of the magmatic systems (up to several millions of years) with culmination in climatic, short-lived ignimbrite eruptions (geologically instantaneous) and less voluminous pre-caldera and post-caldera, plutonic to subvolcanic and volcanic activity. In addition, our result may be compared to geochronological data on granitic plutonism in the region: granitic plutons may be considered, to some degree, as deep-level equivalents of ignimbrites and their dating constrains the timing of magma evolution in deeper parts of the magmatic systems. The Late Carboniferous granites in Erzgebirge provide a well-studied example. Tichomirowa et al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2019" title="Tichomirowa M, Käßner A, Sperner B, Lapp M, Leonhardt D, Linnemann U, Münker C, Ovtcharova M, Pfänder JA, Schaltegger U, Sergeev S, von Quadt A, Whitehouse M (2019) Dating multiply overprinted granites: The effect of protracted magmatism and fluid flow on dating systems (zircon U–Pb: SHRIMP/SIMS, LAICP-MS, CA-ID-TIMS; and Rb–Sr, Ar–Ar)—granites from the Western Erzgebirge (Bohemian Massif, Germany). Chem Geol 519(4):11–38" href="/article/10.1007/s00531-024-02474-y#ref-CR93" id="ref-link-section-d17672574e2175">2019</a>) using several U–Pb zircon dating techniques (LA ICP MS, SHRIMP, CA ID TIMS) found that the plutons were emplaced between 323 and 314 Ma spanning ca. 9 My with three intrusive episodes 1–2 My long each separated by quiescence periods lasting several million years each. A similar pattern of granitic plutonism was recognised by Turniak et al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2014" title="Turniak K, Mazur S, Domańska-Siuda J, Szuszkiewicz A (2014) SHRIMP U-Pb zircon dating for granitoids from the Strzegom-Sobótka Massif, SW Poland: constraints on the initial time of Permo-Mesozoic lithosphere thinning beneath Central Europe. Lithos 208–209:415–429" href="/article/10.1007/s00531-024-02474-y#ref-CR96" id="ref-link-section-d17672574e2178">2014</a>) using SHRIMP zircon dating in the Strzegom-Sobótka granitic massif in the Fore-Sudetic Block, close to our study area. These authors found that the massif formed during the emplacement of four magma batches in a time span of 10–15 My, with the three main batches emplaced in ca. 4 My between 302 and 296 Ma.</p><p>In the case GSRT and ŁR study reported here, the spread of ages between samples Gr1 and Go1 is up to 11.8 My (including uncertainties). A comparison to the volcanic and plutonic systems discussed above shows a broad similarity in terms of duration and timing of the GSRT-ŁR activity, although our SHRIMP results are not precise enough to specify details. It is also noted that our results and those of Turniak et al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2014" title="Turniak K, Mazur S, Domańska-Siuda J, Szuszkiewicz A (2014) SHRIMP U-Pb zircon dating for granitoids from the Strzegom-Sobótka Massif, SW Poland: constraints on the initial time of Permo-Mesozoic lithosphere thinning beneath Central Europe. Lithos 208–209:415–429" href="/article/10.1007/s00531-024-02474-y#ref-CR96" id="ref-link-section-d17672574e2184">2014</a>) point to the main eruption of GSRT magmas, spanning the Carboniferous/Permian boundary, contemporaneously with the intrusion of granitic magmas in the Strzegom-Sobótka massif 50 km to the NNE (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig10">10</a>). Smaller granite intrusions of similar age of 305–295 Ma are also found in the Strzelin Massif and the Kłodzko-Złoty Stok Massif to the E and SE (Oberc-Dziedzic and Kryza <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2012" title="Oberc-Dziedzic T, Kryza R (2012) Late stage Variscan magmatism in the Strzelin Massif (SW Poland): SHRIMP zircon ages of tonalite andBt-Ms granite of the Gęsiniec intrusion. Geol Q 56:225–236" href="/article/10.1007/s00531-024-02474-y#ref-CR71" id="ref-link-section-d17672574e2190">2012</a>; Jakubauskas et al. 2018). The younger ages reported in this study, such as 292.6 ± 1.9 Ma for sample Go1, compare well to rhyolite ages from the vicinity of Wałbrzych and from the North-Sudetic Basin (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig10">10</a>). These correlations highlight the significance of voluminous silicic magmatism in the Sudetes region at the turn of Carboniferous and Permian and in the Early Permian. This magmatism can be linked to larger-scale geodynamic processes that affected the Central Europe area, in particular to the onset of Permo-Mesozoic lithospheric thinning (cf. Turniak et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2014" title="Turniak K, Mazur S, Domańska-Siuda J, Szuszkiewicz A (2014) SHRIMP U-Pb zircon dating for granitoids from the Strzegom-Sobótka Massif, SW Poland: constraints on the initial time of Permo-Mesozoic lithosphere thinning beneath Central Europe. Lithos 208–209:415–429" href="/article/10.1007/s00531-024-02474-y#ref-CR96" id="ref-link-section-d17672574e2196">2014</a>).</p><h3 class="c-article__sub-heading" id="Sec14">Stratigraphic constraints</h3><p>Our SHRIMP results rise the question about the stratigraphic position of the GSRT, the Lower Permian Volcanic Complex and the Słupiec Formation. So far the Słupiec Formation with the component volcanic units is considered early Permian in age and variably correlated to the Asselian-Sakmarian stages in the global chronostratigraphic scale (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig3">3</a>). This view is largely based on regional correlations with Carboniferous—Permian successions in adjacent basins and on biostratigraphic evidence, with only a single isotopic dating of volcanic rocks (Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e2210">2016a</a>). The SHRIMP results presented in this study for the GSRT (samples Gr1, Mi1, Mi2, Hy2) partly overlap the Vrani Hory rhyolite age determined by Opluštil et al. (op. cit.) although with a bias towards older ages (Fig. <a data-track="click" data-track-label="link" data-track-action="figure anchor" href="/article/10.1007/s00531-024-02474-y#Fig10">10</a>). This statement remains correct even considering typical SHRIMP uncertainties of 1%, i.e. ca. 3 My for ages of 300 Ma, larger than reported in this study. In addition, there are abundant volcanic rocks—not isotopically dated so far—which underlie the GSRT in the NW part of the outcrop and indicate pre-GSRT volcanism in the central part of the basin (Awdankiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1999a" title="Awdankiewicz M (1999a) Volcanism in a late Variscan intramontane trough: Carboniferous and Permian volcanic centres of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:13–47" href="/article/10.1007/s00531-024-02474-y#ref-CR3" id="ref-link-section-d17672574e2216">1999a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Awdankiewicz M (1999b) Volcanism in a late Variscan intramontane trough: the petrology and geochemistry of the Carboniferous and Permian volcanic rocks of the Intra-Sudetic Basin, SW Poland. Geol Sudet 32:83–111" href="/article/10.1007/s00531-024-02474-y#ref-CR4" id="ref-link-section-d17672574e2219">b</a>). These relationships rise some doubts on the current views on the age and stratigraphic position of the GSRT and the Słupiec Formation, which can be a few My older than assumed so far. This suggestion is evaluated below in the light of available biostratigraphic constraints. In this respect, ichnofossils and amphibian fossils, although recognised in the studied late Carboniferous-early Permian succession (e.g., Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e2223">2016a</a> and references therein) provide only general evidence, not precise enough. More informative are fish biozones and especially miospore zones.</p><p>The Intra-Sudetic Basin is one of the classic areas showing a succession of fish zones along with other basins lying in proximity (Zajíc and Štamberg <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2004" title="Zajíc J, Štamberg S (2004) Selected important fossiliferous horizons of the Boskovice Basin in the light of the new zoopaleontological data. Acta Musei Reginaehradecensis Series A 30:5–14" href="/article/10.1007/s00531-024-02474-y#ref-CR108" id="ref-link-section-d17672574e2229">2004</a>; Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e2232">2016a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Opluštil S, Schmitz M, Cleal CJ, Martínek K (2016b) A review of the Middle-Late Pennsylvanian west European regional substages and floral biozones, and their correlation to the Geological Time Scale based on new U-Pb ages. Earth Sci Rev 154:301–335" href="/article/10.1007/s00531-024-02474-y#ref-CR74" id="ref-link-section-d17672574e2235">b</a>). The GSRT are located between deposits correlated with the older <i>Acanthodes gracilis</i> and the younger <i>Xenacanthus deheni</i> zones (Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e2245">2016a</a>). The lower limit of the <i>A. gracilis</i> zone was estimated between 298.5 and 297.5 Ma based on the data from the nearby Boskovice and western Bohemia basins (Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e2251">2016a</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference b" title="Opluštil S, Schmitz M, Cleal CJ, Martínek K (2016b) A review of the Middle-Late Pennsylvanian west European regional substages and floral biozones, and their correlation to the Geological Time Scale based on new U-Pb ages. Earth Sci Rev 154:301–335" href="/article/10.1007/s00531-024-02474-y#ref-CR74" id="ref-link-section-d17672574e2254">b</a>). Our datings of the GSRT mostly precede this interval with a slight overlap. However, the <i>A. gracilis</i> zone is possibly strongly diachronous between these nearby basins. In fact, the diachronous character of the fish biozones was suggested before (Lucas et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2006" title="Lucas SG, Schneider JW, Cassinis G (2006) Non-marine Permian biostratigraphy and biochronology: an introduction. Geol Soc Lond Spec Publ 265:1–14" href="/article/10.1007/s00531-024-02474-y#ref-CR55" id="ref-link-section-d17672574e2260">2006</a>; Lucas and Shen <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2018" title="Lucas SG, Shen SZ (2018) The Permian timescale: an introduction. Geol Soc Lond Spec Publ 450:1–19" href="/article/10.1007/s00531-024-02474-y#ref-CR54" id="ref-link-section-d17672574e2264">2018</a>), as well as the environmental rather than evolutionary control over the fish assemblages (e.g., Schneider et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2000" title="Schneider JW, Hampe O, Soler-Gijón R (2000) The Late Carboniferous and Permian: aquatic vertebrate zonation in southern Spain and German basins. Courier-Forschungsinstitut Senckenberg 223:543–562" href="/article/10.1007/s00531-024-02474-y#ref-CR87" id="ref-link-section-d17672574e2267">2000</a>; Fisher et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2010" title="Fischer J, Schneider JW, Ronchi A (2010) New Hybondontoid Shark from the Permocarboniferous (Gzhelian—Asselian) of Guardia Pisano (Sardinia, Italy). Acta Palaeontol Pol 55:241–264" href="/article/10.1007/s00531-024-02474-y#ref-CR34" id="ref-link-section-d17672574e2270">2010</a>; Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e2273">2016a</a>; Pawlak et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2024" title="Pawlak W, Ploch I, Štamberg S, Raczyński P, Kiersnowski H (2024) A new early Permian actinopterygian assemblage shows environmental controls on the distribution of Paramblypterus (Intra-Sudetic Basin, Poland). Geol Q 68:12" href="/article/10.1007/s00531-024-02474-y#ref-CR78" id="ref-link-section-d17672574e2276">2024</a>). Additionally, the above estimate of the lower limit of the <i>A. gracilis</i> zone derives from the successions actually exposing no consecutiveness of <i>A. gracilis</i> zone over the underlying one <i>Sphaerolepis</i>-<i>Elonichthys</i> (Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016b" title="Opluštil S, Schmitz M, Cleal CJ, Martínek K (2016b) A review of the Middle-Late Pennsylvanian west European regional substages and floral biozones, and their correlation to the Geological Time Scale based on new U-Pb ages. Earth Sci Rev 154:301–335" href="/article/10.1007/s00531-024-02474-y#ref-CR74" id="ref-link-section-d17672574e2292">2016b</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2017a" title="Opluštil S, Jirásek J, Schmitz M, Matýsek D (2017a) Biotic changes around the radioisotopically constrained Carboniferous-Permian boundary in the Boskovice Basin (Czech Republic). Bull Geosci 92:95–122" href="/article/10.1007/s00531-024-02474-y#ref-CR75" id="ref-link-section-d17672574e2295">2017a</a>), thus it should not be treated as a direct dating of the boundary interval between them. The diachrony of the discussed fish zones appears to be reasonable due to a mountainous topography produced by the Variscan orogeny entailing physical barriers and spatial variation of the climate, being factors favourable for the modern fish provincialism (Unmack <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2001" title="Unmack PJ (2001) Biogeography of Australian freshwater fishes. J Biogeogr 28:1053–1089" href="/article/10.1007/s00531-024-02474-y#ref-CR98" id="ref-link-section-d17672574e2298">2001</a>; Griffiths et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2014" title="Griffiths D, McGonigle C, Quinn R (2014) Climate and species richness patterns of freshwater fish in North America and Europe. J Biogeogr 41:452–463" href="/article/10.1007/s00531-024-02474-y#ref-CR40" id="ref-link-section-d17672574e2302">2014</a>; Leroy et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2019" title="Leroy B, Dias MS, Giraud E, Hugueny B, Jézéquel C, Leprieur F, Oberdorff T, Tedesco PA (2019) Global biogeographical regions of freshwater fish species. J Biogeogr 46:2407–2419" href="/article/10.1007/s00531-024-02474-y#ref-CR52" id="ref-link-section-d17672574e2305">2019</a>). Climatic gradients would influence water temperature or mixing regime and thus the survivorship of offspring (Unmack <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2001" title="Unmack PJ (2001) Biogeography of Australian freshwater fishes. J Biogeogr 28:1053–1089" href="/article/10.1007/s00531-024-02474-y#ref-CR98" id="ref-link-section-d17672574e2308">2001</a>). Our results emphasise the need for a comprehensive study on environmental preferences of fish species important for stratigraphy of the continental Permo-Carboniferous successions.</p><p>The palynological data are the most useful tool in biostratigraphy of the continental sedimentary rocks of the Carboniferous and Permian turn, but the documentation for rocks of the Intrasudetic Basin is in fact poor, derived mainly from grey-coloured fine-detrital rocks occurring amongst red beds. The grey Walchia shales, occurring in the top of the Słupiec Formation, as well as other grey shale levels in underlying formations, were palynologically studied by Jerzykiewicz (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1987" title="Jerzykiewicz J (1987) Latest Carboniferous (Stephanian) and Permian (Autunian) palynological assemblages from the intrasudetic basin, southwestern Poland. Palynology 11:117–131" href="/article/10.1007/s00531-024-02474-y#ref-CR45" id="ref-link-section-d17672574e2314">1987</a>). This author included the Walchia shales in the <i>Disacites striatiti</i> miospore zone, and the lower shale horizons in the <i>Vittatina costabilis</i> zone of the standard miospore zonation by Clayton et al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1977" title="Clayton G, Coquel R, Doubinger J, Gueinn KJ, Loboziak S, Owens B, Streel M (1977) Carboniferous miospores of Western Europe—illustration and zonation. Meded Rijks Geol Dienst 29:1–72" href="/article/10.1007/s00531-024-02474-y#ref-CR26" id="ref-link-section-d17672574e2323">1977</a>), which were assigned to the Permian. Different views on the age of these older shale levels were presented by Górecka (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1969" title="Górecka T (1969) Pozycja stratygraficzna serii górnokarbońskiej z otworu wiertniczego w Rybnie na Dolnym Śląsku. Przegląd Geologiczny 17(9):431–433" href="/article/10.1007/s00531-024-02474-y#ref-CR37" id="ref-link-section-d17672574e2326">1969</a>, <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1981" title="Górecka T (1981) Wyniki badań palinostratygraficznych najmłodszego karbonu z obszaru Dolnego Śląska. Prace Naukowe Instytutu Górnictwa Politechniki Wrocławskiej. Monografie 19:1–58" href="/article/10.1007/s00531-024-02474-y#ref-CR38" id="ref-link-section-d17672574e2330">1981</a>) and Górecka-Nowak (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1989" title="Górecka-Nowak A (1989) Późnokarbońskie zespoły sporowo-pyłkowe z profilu otworu wiertniczego Unisław Śl. IG 1 (depresja śródsudecka). Prace Naukowe Instytutu Górnictwa Politechniki Wrocławskiej, 52. Studia i Materiały 19:52–77" href="/article/10.1007/s00531-024-02474-y#ref-CR39" id="ref-link-section-d17672574e2333">1989</a>), who considered them to be of Stephanian age. Further constraints are provided by the miospore data from the global stratotype of the Carboniferous/Permian boundary from Aidaralash, Kazakhstan (Dunn <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2001" title="Dunn MT (2001) Palynology of the Carboniferous-Permian boundary stratotype, Aidaralash Creek, Kazakhstan. Rev Palaeobot Palynol 116:175–194" href="/article/10.1007/s00531-024-02474-y#ref-CR30" id="ref-link-section-d17672574e2336">2001</a>). These results show that the C/P boundary is located within the <i>Disaccites striatiti</i> miospore zone of Clayton et al. (<a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1977" title="Clayton G, Coquel R, Doubinger J, Gueinn KJ, Loboziak S, Owens B, Streel M (1977) Carboniferous miospores of Western Europe—illustration and zonation. Meded Rijks Geol Dienst 29:1–72" href="/article/10.1007/s00531-024-02474-y#ref-CR26" id="ref-link-section-d17672574e2342">1977</a>). In the Intrasudetic Basin this zone has been documented in the Walchia shales (Jerzykiewicz <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 1987" title="Jerzykiewicz J (1987) Latest Carboniferous (Stephanian) and Permian (Autunian) palynological assemblages from the intrasudetic basin, southwestern Poland. Palynology 11:117–131" href="/article/10.1007/s00531-024-02474-y#ref-CR45" id="ref-link-section-d17672574e2345">1987</a>). This means that rocks of the two older formations, and probably the lower part of the Słupiec Formation, should be included to the Carboniferous, and that the boundary with the Permian is located as high up-sequence as in the Walchia shales, in the upper part of the Słupiec Formation. However, the assumption of the location of the C/P boundary within the Walchia shales level is not consistent with both the LA-ICP-MS dating of the Góry Krucze rhyolites (Opluštil et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2016a" title="Opluštil S, Schmitz M, Kachlík V, Štamberg S (2016a) Re-assessment of lithostratigraphy, biostratigraphy and volcanic history of the Late Paleozoic Intra-Sudetic, Krkonoše-Piedmont and Mnichovo Hradiště basins (Czech Republic) based on new U–Pb CA-ID-TIMS ages. Bull Geosci 91:399–432" href="/article/10.1007/s00531-024-02474-y#ref-CR73" id="ref-link-section-d17672574e2349">2016a</a>) and with the SHRIMP results presented in this contribution, which indicate that at least parts of volcanic units in the Lower Permian Volcanic Complex are indeed of early Permian age. Thus the inconsistency between the U–Pb zircon datings (too few and not precise enough) and the biostratigraphic evidence, including fish and miospore data (mostly poor/inconclusive) as well as the problem of stratigraphic position of Permo-Carboniferous formations of the Intra-Sudetic Basin require further research. Our results further suggest that the volcano-sedimentary formations of the Intra-Sudetic Basin spanning the transition of Carboniferous and Permian developed over shorter time scales than assumed so far, and thus the interrelated tectonic, volcanic and sedimentary processes in the basin were more vigorous. A dynamic basin development culminating in intense volcanism and rapidly followed by a prolonged decline in any activity was also noted in case of the North-Sudetic Basin (Awdankiewicz et al. <a data-track="click" data-track-action="reference anchor" data-track-label="link" data-test="citation-ref" aria-label="Reference 2014a" title="Awdankiewicz M, Awdankiewicz H, Rapprich V, Stárková M (2014a) A Permian andesitic tuff ring at Rožmitál (the Intra-Sudetic Basin, Czech Republic)—evolution from explosive to effusive and high-level intrusive activity. Geol Q 58:759–778" href="/article/10.1007/s00531-024-02474-y#ref-CR8" id="ref-link-section-d17672574e2352">2014a</a>).</p></div></div></section><section data-title="Conclusion"><div class="c-article-section" id="Sec15-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="Sec15">Conclusion</h2><div class="c-article-section__content" id="Sec15-content"><p>The Góry Suche Rhyolitic Tuffs (GSRT), a voluminous (ca. 100 km<sup>3</sup>), ignimbrite-dominated pyroclastic deposit, together with associated Łomnica Rhyolite sills, reflect the climax of late Palaeozoic post-orogenic volcanism in the Intra-Sudetic Basin, a large post-Variscan intracontinental trough in Central Europe. The main conclusions from our U–Pb SHRIMP zircon study of nine samples may be summarised as follows:</p><ol class="u-list-style-none"> <li> <span class="u-custom-list-number">1.</span> <p>The concordia ages in four tuff (ignimbrite) samples ranging from 300.5 ± 2.0 to 297.2 ± 0.9 Ma, together with geological evidence, indicate the eruption and deposition of the GSRT at ca. 299 Ma, close to the Carboniferous/Permian boundary. This explosive activity was followed (partly overlapped?) by the emplacement of Łomnica rhyolitic sills dated by two samples at 298.4 ± 2.0 and 292.6 ± 1.9 Ma.</p> </li> <li> <span class="u-custom-list-number">2.</span> <p>Zircon assemblages in three other tuff specimens are strongly dominated by xenocrysts of Palaeozoic and Precambrian ages, with lack of Mesoproterozoic ages typical of basement rocks in the region. The zircon xenocrysts were likely incorporated into the rhyolitic tephra during the eruption through the siliciclastic sedimentary cover in the vent area inside the basin. The spatial distribution of xenocryst-free samples in the NW and xenocryst-rich samples mostly in the SE suggests the presence of distinct depositional units of the tuffs.</p> </li> <li> <span class="u-custom-list-number">3.</span> <p>Our dating results in the context of published data on fish and miospore zones in the Late Carbonifeorus/Permian deposits of the Intra-Sudetic Basin, rise doubts on the current views on the age and stratigraphic position of the GSRT and the Słupiec Formation, which can be a few My older than assumed. Consequently, the Carboniferous/Permian boundary may be located higher in the succession than considered so far. This implies a faster than supposed evolution of the basin across the Carboniferous/Permian transition. These results highlight also the problems in correlation of Permo-Carboniferous continental volcano-sedimentary successions to the global chronostratigraphic scale.</p> </li> <li> <span class="u-custom-list-number">4.</span> <p>Our dating results correlate the rhyolitic GSRT and ŁR explosive to subvolcanic activity with the regional "magmatic flare-up" at the Carboniferous/Permian boundary. The close similarity of our tuff and rhyolite ages with those of the Strzegom-Sobótka and other granites in vicinity emphasise the significance of voluminous silicic magmatism, at both plutonic and volcanic levels, in the Sudetes at the turn of Carboniferous and Permian. This magmatism can be linked to the onset of Permo-Mesozoic lithospheric thinning under Central Europe.</p> </li> </ol></div></div></section> </div> <section data-title="Data availability"><div class="c-article-section" id="data-availability-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="data-availability">Data availability</h2><div class="c-article-section__content" id="data-availability-content"> <p>The authors confirm that the data supporting the findings of this study are available within the article and/or its supplementary materials.</p> </div></div></section><div id="MagazineFulltextArticleBodySuffix"><section aria-labelledby="Bib1" data-title="References"><div class="c-article-section" id="Bib1-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="Bib1">References</h2><div class="c-article-section__content" id="Bib1-content"><div data-container-section="references"><ul class="c-article-references" data-track-component="outbound reference" data-track-context="references section"><li class="c-article-references__item js-c-reading-companion-references-item"><p class="c-article-references__text" id="ref-CR1">Aleksandrowski P, Kryza R, Mazur S, Żaba J (1997) Kinematic data on major Variscan strike-slip faults and shear zones in the Polish Sudetes, northeast Bohemian Massif. 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V. Rapprich, M Petronis and S. Voigt are acknowledged for their help and discussions during the field work. Z. Czupyt, D. Gurba and P. Derkowski are acknowledged for their assistance in CL and SHRIMP analysis. Discussion with K. Turniak helped in interpretation of the geochronological results. Helpful reviews by F. Tomek and A. Kassner are greatly appreciated. Efficient editorial handling by U. Riller is highly acknowledged.</p></div></div></section><section aria-labelledby="author-information" data-title="Author information"><div class="c-article-section" id="author-information-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="author-information">Author information</h2><div class="c-article-section__content" id="author-information-content"><h3 class="c-article__sub-heading" id="affiliations">Authors and Affiliations</h3><ol class="c-article-author-affiliation__list"><li id="Aff1"><p class="c-article-author-affiliation__address">Institute of Geological Sciences, University of Wrocław, Plac Maksa Borna 9, 50-204, Wrocław, Poland</p><p class="c-article-author-affiliation__authors-list">Marek Awdankiewicz, Paweł Raczyński & Anna Górecka-Nowak</p></li><li id="Aff2"><p class="c-article-author-affiliation__address">Polish Geological Institute - National Research Institute, Rakowiecka 4, 00-975, Warsaw, Poland</p><p class="c-article-author-affiliation__authors-list">Magdalena Pańczyk, Izabela Ploch, Honorata Awdankiewicz & Tadeusz Peryt</p></li><li id="Aff3"><p class="c-article-author-affiliation__address">Faculty of Biology, Biological and Chemical Research Centre, Institute of Evolutionary Biology, University of Warsaw, Żwirki I Wigury 101, 02-089, Warsaw, Poland</p><p class="c-article-author-affiliation__authors-list">Wojciech Pawlak</p></li></ol><div class="u-js-hide u-hide-print" data-test="author-info"><span class="c-article__sub-heading">Authors</span><ol class="c-article-authors-search u-list-reset"><li id="auth-Marek-Awdankiewicz-Aff1"><span class="c-article-authors-search__title u-h3 js-search-name">Marek Awdankiewicz</span><div class="c-article-authors-search__list"><div class="c-article-authors-search__item c-article-authors-search__list-item--left"><a href="/search?dc.creator=Marek%20Awdankiewicz" class="c-article-button" data-track="click" data-track-action="author link - 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Peryt and I. Ploch. The concept of this study was designed by M. Awdankiewicz, I. Ploch and P. Raczyński. M. Awdankiewicz, H. Awdankiewicz, P. Raczyński and I. Ploch carried out the field work and sampling. M. Awdankiewicz and H. Awdankiewicz prepared petrographic characteristics of the samples. H. Awdankiewicz separated zircon for dating. M. Pańczyk supervised CL and SHRIMP analyses, selected analysis sites, performed data reduction of isotope results and recalculation. The manuscript was written and figures prepared by M. Awdankiewicz with contributions of M. Pańczyk (zircon characteristics and results of SHRIMP analysis with related figures and tables), W. Pawlak, I. Ploch and A. Górecka-Nowak (stratigraphic aspects). All authors contributed to the discussion of the results and commented on working versions of the manuscript. All authors read and approved the final manuscript.</p><h3 class="c-article__sub-heading" id="corresponding-author">Corresponding author</h3><p id="corresponding-author-list">Correspondence to <a id="corresp-c1" href="mailto:marek.awdankiewicz@uwr.edu.pl">Marek Awdankiewicz</a>.</p></div></div></section><section data-title="Ethics declarations"><div class="c-article-section" id="ethics-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="ethics">Ethics declarations</h2><div class="c-article-section__content" id="ethics-content"> <h3 class="c-article__sub-heading" id="FPar1">Conflict of interest</h3> <p>All Authors declare their consent to publish the results and are not aware of any financial or non-financial interests that are directly or indirectly related to the work submitted for publication.</p> </div></div></section><section data-title="Supplementary Information"><div class="c-article-section" id="Sec16-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="Sec16">Supplementary Information</h2><div class="c-article-section__content" id="Sec16-content"><div data-test="supplementary-info"><div id="figshareContainer" class="c-article-figshare-container" data-test="figshare-container"></div><p>Below is the link to the electronic supplementary material.</p><div class="c-article-supplementary__item" data-test="supp-item" id="MOESM1"><h3 class="c-article-supplementary__title u-h3"><a class="print-link" data-track="click" data-track-action="view supplementary info" data-test="supp-info-link" data-track-label="table 1" href="https://static-content.springer.com/esm/art%3A10.1007%2Fs00531-024-02474-y/MediaObjects/531_2024_2474_MOESM1_ESM.xlsx" data-supp-info-image=""><b>Table 1</b></a></h3><div class="c-article-supplementary__description" data-component="thumbnail-container"><p> SHRIMP data for the studied samples. (a) sample Lo1. (b) sample Go1. (c) sample Pu2. (d) sample Tl1. (e) sample Wl1. (f) sample Mi1. (g) sample Gr1. (h) sample Mi2. (i) sample Hy2 (XLSX 208 KB)</p></div></div></div></div></div></section><section data-title="Rights and permissions"><div class="c-article-section" id="rightslink-section"><h2 class="c-article-section__title js-section-title js-c-reading-companion-sections-item" id="rightslink">Rights and permissions</h2><div class="c-article-section__content" id="rightslink-content"> <p><b>Open Access</b> This article is licensed under a Creative Commons Attribution 4.0 International License, which permits use, sharing, adaptation, distribution and reproduction in any medium or format, as long as you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons licence, and indicate if changes were made. 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id="citeas">Cite this article</h3><p class="c-bibliographic-information__citation">Awdankiewicz, M., Pańczyk, M., Ploch, I. <i>et al.</i> Timing of post-orogenic silicic volcanism in the eastern part of the European Variscides: constraints from SHRIMP U–Pb zircon study of the Permo-Carboniferous Góry Suche Rhyolitic Tuffs (the Intra-Sudetic Basin). <i>Int J Earth Sci (Geol Rundsch)</i> (2024). https://doi.org/10.1007/s00531-024-02474-y</p><p class="c-bibliographic-information__download-citation u-hide-print"><a data-test="citation-link" data-track="click" data-track-action="download article citation" data-track-label="link" data-track-external="" rel="nofollow" href="https://citation-needed.springer.com/v2/references/10.1007/s00531-024-02474-y?format=refman&flavour=citation">Download citation<svg width="16" height="16" focusable="false" role="img" aria-hidden="true" class="u-icon"><use xmlns:xlink="http://www.w3.org/1999/xlink" 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