Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA
Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. La...
Ausführliche Beschreibung
Autor*in: |
Wayne, David M. [verfasserIn] |
---|
Format: |
Artikel |
---|---|
Sprache: |
Englisch |
Erschienen: |
1992 |
---|
Schlagwörter: |
---|
Systematik: |
|
---|
Anmerkung: |
© Springer-Verlag 1992 |
---|
Übergeordnetes Werk: |
Enthalten in: Contributions to mineralogy and petrology - Springer-Verlag, 1966, 109(1992), 3 vom: Jan., Seite 408-420 |
---|---|
Übergeordnetes Werk: |
volume:109 ; year:1992 ; number:3 ; month:01 ; pages:408-420 |
Links: |
---|
DOI / URN: |
10.1007/BF00283328 |
---|
Katalog-ID: |
OLC2070509834 |
---|
LEADER | 01000caa a22002652 4500 | ||
---|---|---|---|
001 | OLC2070509834 | ||
003 | DE-627 | ||
005 | 20230402225047.0 | ||
007 | tu | ||
008 | 200820s1992 xx ||||| 00| ||eng c | ||
024 | 7 | |a 10.1007/BF00283328 |2 doi | |
035 | |a (DE-627)OLC2070509834 | ||
035 | |a (DE-He213)BF00283328-p | ||
040 | |a DE-627 |b ger |c DE-627 |e rakwb | ||
041 | |a eng | ||
082 | 0 | 4 | |a 550 |q VZ |
084 | |a 13 |2 ssgn | ||
084 | |a TE 1000 |q VZ |2 rvk | ||
100 | 1 | |a Wayne, David M. |e verfasserin |4 aut | |
245 | 1 | 0 | |a Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA |
264 | 1 | |c 1992 | |
336 | |a Text |b txt |2 rdacontent | ||
337 | |a ohne Hilfsmittel zu benutzen |b n |2 rdamedia | ||
338 | |a Band |b nc |2 rdacarrier | ||
500 | |a © Springer-Verlag 1992 | ||
520 | |a Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction. | ||
650 | 4 | |a Zircon | |
650 | 4 | |a Granitic Gneiss | |
650 | 4 | |a Isotopic Systematic | |
650 | 4 | |a Metamorphic Zircon | |
650 | 4 | |a Augen Gneiss | |
700 | 1 | |a Sinha, A. Krishna |4 aut | |
700 | 1 | |a Hewitt, David A. |4 aut | |
773 | 0 | 8 | |i Enthalten in |t Contributions to mineralogy and petrology |d Springer-Verlag, 1966 |g 109(1992), 3 vom: Jan., Seite 408-420 |w (DE-627)129068721 |w (DE-600)1616-0 |w (DE-576)014400367 |x 0010-7999 |7 nnns |
773 | 1 | 8 | |g volume:109 |g year:1992 |g number:3 |g month:01 |g pages:408-420 |
856 | 4 | 1 | |u https://doi.org/10.1007/BF00283328 |z lizenzpflichtig |3 Volltext |
912 | |a GBV_USEFLAG_A | ||
912 | |a SYSFLAG_A | ||
912 | |a GBV_OLC | ||
912 | |a SSG-OLC-GEO | ||
912 | |a SSG-OPC-GGO | ||
912 | |a GBV_ILN_11 | ||
912 | |a GBV_ILN_21 | ||
912 | |a GBV_ILN_22 | ||
912 | |a GBV_ILN_30 | ||
912 | |a GBV_ILN_31 | ||
912 | |a GBV_ILN_40 | ||
912 | |a GBV_ILN_65 | ||
912 | |a GBV_ILN_70 | ||
912 | |a GBV_ILN_2004 | ||
912 | |a GBV_ILN_2010 | ||
912 | |a GBV_ILN_2015 | ||
912 | |a GBV_ILN_2018 | ||
912 | |a GBV_ILN_2027 | ||
912 | |a GBV_ILN_4012 | ||
912 | |a GBV_ILN_4046 | ||
912 | |a GBV_ILN_4082 | ||
912 | |a GBV_ILN_4103 | ||
912 | |a GBV_ILN_4112 | ||
912 | |a GBV_ILN_4125 | ||
912 | |a GBV_ILN_4302 | ||
912 | |a GBV_ILN_4305 | ||
912 | |a GBV_ILN_4306 | ||
912 | |a GBV_ILN_4311 | ||
912 | |a GBV_ILN_4319 | ||
912 | |a GBV_ILN_4323 | ||
936 | r | v | |a TE 1000 |
951 | |a AR | ||
952 | |d 109 |j 1992 |e 3 |c 01 |h 408-420 |
author_variant |
d m w dm dmw a k s ak aks d a h da dah |
---|---|
matchkey_str |
article:00107999:1992----::ifrnilepneficnpiooisseaisoeaopimcosltooibudraeapermhhpvle |
hierarchy_sort_str |
1992 |
publishDate |
1992 |
allfields |
10.1007/BF00283328 doi (DE-627)OLC2070509834 (DE-He213)BF00283328-p DE-627 ger DE-627 rakwb eng 550 VZ 13 ssgn TE 1000 VZ rvk Wayne, David M. verfasserin aut Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA 1992 Text txt rdacontent ohne Hilfsmittel zu benutzen n rdamedia Band nc rdacarrier © Springer-Verlag 1992 Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction. Zircon Granitic Gneiss Isotopic Systematic Metamorphic Zircon Augen Gneiss Sinha, A. Krishna aut Hewitt, David A. aut Enthalten in Contributions to mineralogy and petrology Springer-Verlag, 1966 109(1992), 3 vom: Jan., Seite 408-420 (DE-627)129068721 (DE-600)1616-0 (DE-576)014400367 0010-7999 nnns volume:109 year:1992 number:3 month:01 pages:408-420 https://doi.org/10.1007/BF00283328 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-GEO SSG-OPC-GGO GBV_ILN_11 GBV_ILN_21 GBV_ILN_22 GBV_ILN_30 GBV_ILN_31 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_2004 GBV_ILN_2010 GBV_ILN_2015 GBV_ILN_2018 GBV_ILN_2027 GBV_ILN_4012 GBV_ILN_4046 GBV_ILN_4082 GBV_ILN_4103 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4302 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4311 GBV_ILN_4319 GBV_ILN_4323 TE 1000 AR 109 1992 3 01 408-420 |
spelling |
10.1007/BF00283328 doi (DE-627)OLC2070509834 (DE-He213)BF00283328-p DE-627 ger DE-627 rakwb eng 550 VZ 13 ssgn TE 1000 VZ rvk Wayne, David M. verfasserin aut Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA 1992 Text txt rdacontent ohne Hilfsmittel zu benutzen n rdamedia Band nc rdacarrier © Springer-Verlag 1992 Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction. Zircon Granitic Gneiss Isotopic Systematic Metamorphic Zircon Augen Gneiss Sinha, A. Krishna aut Hewitt, David A. aut Enthalten in Contributions to mineralogy and petrology Springer-Verlag, 1966 109(1992), 3 vom: Jan., Seite 408-420 (DE-627)129068721 (DE-600)1616-0 (DE-576)014400367 0010-7999 nnns volume:109 year:1992 number:3 month:01 pages:408-420 https://doi.org/10.1007/BF00283328 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-GEO SSG-OPC-GGO GBV_ILN_11 GBV_ILN_21 GBV_ILN_22 GBV_ILN_30 GBV_ILN_31 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_2004 GBV_ILN_2010 GBV_ILN_2015 GBV_ILN_2018 GBV_ILN_2027 GBV_ILN_4012 GBV_ILN_4046 GBV_ILN_4082 GBV_ILN_4103 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4302 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4311 GBV_ILN_4319 GBV_ILN_4323 TE 1000 AR 109 1992 3 01 408-420 |
allfields_unstemmed |
10.1007/BF00283328 doi (DE-627)OLC2070509834 (DE-He213)BF00283328-p DE-627 ger DE-627 rakwb eng 550 VZ 13 ssgn TE 1000 VZ rvk Wayne, David M. verfasserin aut Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA 1992 Text txt rdacontent ohne Hilfsmittel zu benutzen n rdamedia Band nc rdacarrier © Springer-Verlag 1992 Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction. Zircon Granitic Gneiss Isotopic Systematic Metamorphic Zircon Augen Gneiss Sinha, A. Krishna aut Hewitt, David A. aut Enthalten in Contributions to mineralogy and petrology Springer-Verlag, 1966 109(1992), 3 vom: Jan., Seite 408-420 (DE-627)129068721 (DE-600)1616-0 (DE-576)014400367 0010-7999 nnns volume:109 year:1992 number:3 month:01 pages:408-420 https://doi.org/10.1007/BF00283328 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-GEO SSG-OPC-GGO GBV_ILN_11 GBV_ILN_21 GBV_ILN_22 GBV_ILN_30 GBV_ILN_31 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_2004 GBV_ILN_2010 GBV_ILN_2015 GBV_ILN_2018 GBV_ILN_2027 GBV_ILN_4012 GBV_ILN_4046 GBV_ILN_4082 GBV_ILN_4103 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4302 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4311 GBV_ILN_4319 GBV_ILN_4323 TE 1000 AR 109 1992 3 01 408-420 |
allfieldsGer |
10.1007/BF00283328 doi (DE-627)OLC2070509834 (DE-He213)BF00283328-p DE-627 ger DE-627 rakwb eng 550 VZ 13 ssgn TE 1000 VZ rvk Wayne, David M. verfasserin aut Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA 1992 Text txt rdacontent ohne Hilfsmittel zu benutzen n rdamedia Band nc rdacarrier © Springer-Verlag 1992 Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction. Zircon Granitic Gneiss Isotopic Systematic Metamorphic Zircon Augen Gneiss Sinha, A. Krishna aut Hewitt, David A. aut Enthalten in Contributions to mineralogy and petrology Springer-Verlag, 1966 109(1992), 3 vom: Jan., Seite 408-420 (DE-627)129068721 (DE-600)1616-0 (DE-576)014400367 0010-7999 nnns volume:109 year:1992 number:3 month:01 pages:408-420 https://doi.org/10.1007/BF00283328 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-GEO SSG-OPC-GGO GBV_ILN_11 GBV_ILN_21 GBV_ILN_22 GBV_ILN_30 GBV_ILN_31 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_2004 GBV_ILN_2010 GBV_ILN_2015 GBV_ILN_2018 GBV_ILN_2027 GBV_ILN_4012 GBV_ILN_4046 GBV_ILN_4082 GBV_ILN_4103 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4302 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4311 GBV_ILN_4319 GBV_ILN_4323 TE 1000 AR 109 1992 3 01 408-420 |
allfieldsSound |
10.1007/BF00283328 doi (DE-627)OLC2070509834 (DE-He213)BF00283328-p DE-627 ger DE-627 rakwb eng 550 VZ 13 ssgn TE 1000 VZ rvk Wayne, David M. verfasserin aut Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA 1992 Text txt rdacontent ohne Hilfsmittel zu benutzen n rdamedia Band nc rdacarrier © Springer-Verlag 1992 Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction. Zircon Granitic Gneiss Isotopic Systematic Metamorphic Zircon Augen Gneiss Sinha, A. Krishna aut Hewitt, David A. aut Enthalten in Contributions to mineralogy and petrology Springer-Verlag, 1966 109(1992), 3 vom: Jan., Seite 408-420 (DE-627)129068721 (DE-600)1616-0 (DE-576)014400367 0010-7999 nnns volume:109 year:1992 number:3 month:01 pages:408-420 https://doi.org/10.1007/BF00283328 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-GEO SSG-OPC-GGO GBV_ILN_11 GBV_ILN_21 GBV_ILN_22 GBV_ILN_30 GBV_ILN_31 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_2004 GBV_ILN_2010 GBV_ILN_2015 GBV_ILN_2018 GBV_ILN_2027 GBV_ILN_4012 GBV_ILN_4046 GBV_ILN_4082 GBV_ILN_4103 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4302 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4311 GBV_ILN_4319 GBV_ILN_4323 TE 1000 AR 109 1992 3 01 408-420 |
language |
English |
source |
Enthalten in Contributions to mineralogy and petrology 109(1992), 3 vom: Jan., Seite 408-420 volume:109 year:1992 number:3 month:01 pages:408-420 |
sourceStr |
Enthalten in Contributions to mineralogy and petrology 109(1992), 3 vom: Jan., Seite 408-420 volume:109 year:1992 number:3 month:01 pages:408-420 |
format_phy_str_mv |
Article |
institution |
findex.gbv.de |
topic_facet |
Zircon Granitic Gneiss Isotopic Systematic Metamorphic Zircon Augen Gneiss |
dewey-raw |
550 |
isfreeaccess_bool |
false |
container_title |
Contributions to mineralogy and petrology |
authorswithroles_txt_mv |
Wayne, David M. @@aut@@ Sinha, A. Krishna @@aut@@ Hewitt, David A. @@aut@@ |
publishDateDaySort_date |
1992-01-01T00:00:00Z |
hierarchy_top_id |
129068721 |
dewey-sort |
3550 |
id |
OLC2070509834 |
language_de |
englisch |
fullrecord |
<?xml version="1.0" encoding="UTF-8"?><collection xmlns="http://www.loc.gov/MARC21/slim"><record><leader>01000caa a22002652 4500</leader><controlfield tag="001">OLC2070509834</controlfield><controlfield tag="003">DE-627</controlfield><controlfield tag="005">20230402225047.0</controlfield><controlfield tag="007">tu</controlfield><controlfield tag="008">200820s1992 xx ||||| 00| ||eng c</controlfield><datafield tag="024" ind1="7" ind2=" "><subfield code="a">10.1007/BF00283328</subfield><subfield code="2">doi</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(DE-627)OLC2070509834</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(DE-He213)BF00283328-p</subfield></datafield><datafield tag="040" ind1=" " ind2=" "><subfield code="a">DE-627</subfield><subfield code="b">ger</subfield><subfield code="c">DE-627</subfield><subfield code="e">rakwb</subfield></datafield><datafield tag="041" ind1=" " ind2=" "><subfield code="a">eng</subfield></datafield><datafield tag="082" ind1="0" ind2="4"><subfield code="a">550</subfield><subfield code="q">VZ</subfield></datafield><datafield tag="084" ind1=" " ind2=" "><subfield code="a">13</subfield><subfield code="2">ssgn</subfield></datafield><datafield tag="084" ind1=" " ind2=" "><subfield code="a">TE 1000</subfield><subfield code="q">VZ</subfield><subfield code="2">rvk</subfield></datafield><datafield tag="100" ind1="1" ind2=" "><subfield code="a">Wayne, David M.</subfield><subfield code="e">verfasserin</subfield><subfield code="4">aut</subfield></datafield><datafield tag="245" ind1="1" ind2="0"><subfield code="a">Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA</subfield></datafield><datafield tag="264" ind1=" " ind2="1"><subfield code="c">1992</subfield></datafield><datafield tag="336" ind1=" " ind2=" "><subfield code="a">Text</subfield><subfield code="b">txt</subfield><subfield code="2">rdacontent</subfield></datafield><datafield tag="337" ind1=" " ind2=" "><subfield code="a">ohne Hilfsmittel zu benutzen</subfield><subfield code="b">n</subfield><subfield code="2">rdamedia</subfield></datafield><datafield tag="338" ind1=" " ind2=" "><subfield code="a">Band</subfield><subfield code="b">nc</subfield><subfield code="2">rdacarrier</subfield></datafield><datafield tag="500" ind1=" " ind2=" "><subfield code="a">© Springer-Verlag 1992</subfield></datafield><datafield tag="520" ind1=" " ind2=" "><subfield code="a">Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction.</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Zircon</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Granitic Gneiss</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Isotopic Systematic</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Metamorphic Zircon</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Augen Gneiss</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Sinha, A. Krishna</subfield><subfield code="4">aut</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Hewitt, David A.</subfield><subfield code="4">aut</subfield></datafield><datafield tag="773" ind1="0" ind2="8"><subfield code="i">Enthalten in</subfield><subfield code="t">Contributions to mineralogy and petrology</subfield><subfield code="d">Springer-Verlag, 1966</subfield><subfield code="g">109(1992), 3 vom: Jan., Seite 408-420</subfield><subfield code="w">(DE-627)129068721</subfield><subfield code="w">(DE-600)1616-0</subfield><subfield code="w">(DE-576)014400367</subfield><subfield code="x">0010-7999</subfield><subfield code="7">nnns</subfield></datafield><datafield tag="773" ind1="1" ind2="8"><subfield code="g">volume:109</subfield><subfield code="g">year:1992</subfield><subfield code="g">number:3</subfield><subfield code="g">month:01</subfield><subfield code="g">pages:408-420</subfield></datafield><datafield tag="856" ind1="4" ind2="1"><subfield code="u">https://doi.org/10.1007/BF00283328</subfield><subfield code="z">lizenzpflichtig</subfield><subfield code="3">Volltext</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_USEFLAG_A</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">SYSFLAG_A</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_OLC</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">SSG-OLC-GEO</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">SSG-OPC-GGO</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_11</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_21</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_22</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_30</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_31</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_40</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_65</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_70</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_2004</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_2010</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_2015</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_2018</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_2027</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4012</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4046</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4082</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4103</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4112</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4125</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4302</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4305</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4306</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4311</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4319</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4323</subfield></datafield><datafield tag="936" ind1="r" ind2="v"><subfield code="a">TE 1000</subfield></datafield><datafield tag="951" ind1=" " ind2=" "><subfield code="a">AR</subfield></datafield><datafield tag="952" ind1=" " ind2=" "><subfield code="d">109</subfield><subfield code="j">1992</subfield><subfield code="e">3</subfield><subfield code="c">01</subfield><subfield code="h">408-420</subfield></datafield></record></collection>
|
author |
Wayne, David M. |
spellingShingle |
Wayne, David M. ddc 550 ssgn 13 rvk TE 1000 misc Zircon misc Granitic Gneiss misc Isotopic Systematic misc Metamorphic Zircon misc Augen Gneiss Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA |
authorStr |
Wayne, David M. |
ppnlink_with_tag_str_mv |
@@773@@(DE-627)129068721 |
format |
Article |
dewey-ones |
550 - Earth sciences |
delete_txt_mv |
keep |
author_role |
aut aut aut |
collection |
OLC |
remote_str |
false |
illustrated |
Not Illustrated |
issn |
0010-7999 |
topic_title |
550 VZ 13 ssgn TE 1000 VZ rvk Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA Zircon Granitic Gneiss Isotopic Systematic Metamorphic Zircon Augen Gneiss |
topic |
ddc 550 ssgn 13 rvk TE 1000 misc Zircon misc Granitic Gneiss misc Isotopic Systematic misc Metamorphic Zircon misc Augen Gneiss |
topic_unstemmed |
ddc 550 ssgn 13 rvk TE 1000 misc Zircon misc Granitic Gneiss misc Isotopic Systematic misc Metamorphic Zircon misc Augen Gneiss |
topic_browse |
ddc 550 ssgn 13 rvk TE 1000 misc Zircon misc Granitic Gneiss misc Isotopic Systematic misc Metamorphic Zircon misc Augen Gneiss |
format_facet |
Aufsätze Gedruckte Aufsätze |
format_main_str_mv |
Text Zeitschrift/Artikel |
carriertype_str_mv |
nc |
hierarchy_parent_title |
Contributions to mineralogy and petrology |
hierarchy_parent_id |
129068721 |
dewey-tens |
550 - Earth sciences & geology |
hierarchy_top_title |
Contributions to mineralogy and petrology |
isfreeaccess_txt |
false |
familylinks_str_mv |
(DE-627)129068721 (DE-600)1616-0 (DE-576)014400367 |
title |
Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA |
ctrlnum |
(DE-627)OLC2070509834 (DE-He213)BF00283328-p |
title_full |
Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA |
author_sort |
Wayne, David M. |
journal |
Contributions to mineralogy and petrology |
journalStr |
Contributions to mineralogy and petrology |
lang_code |
eng |
isOA_bool |
false |
dewey-hundreds |
500 - Science |
recordtype |
marc |
publishDateSort |
1992 |
contenttype_str_mv |
txt |
container_start_page |
408 |
author_browse |
Wayne, David M. Sinha, A. Krishna Hewitt, David A. |
container_volume |
109 |
class |
550 VZ 13 ssgn TE 1000 VZ rvk |
format_se |
Aufsätze |
author-letter |
Wayne, David M. |
doi_str_mv |
10.1007/BF00283328 |
dewey-full |
550 |
title_sort |
differential response of zircon u−pb isotopic systematics to metamorphism across a lithologic boundary: an example from the hope valley shear zone, southeastern massachusetts, usa |
title_auth |
Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA |
abstract |
Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction. © Springer-Verlag 1992 |
abstractGer |
Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction. © Springer-Verlag 1992 |
abstract_unstemmed |
Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction. © Springer-Verlag 1992 |
collection_details |
GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-GEO SSG-OPC-GGO GBV_ILN_11 GBV_ILN_21 GBV_ILN_22 GBV_ILN_30 GBV_ILN_31 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_2004 GBV_ILN_2010 GBV_ILN_2015 GBV_ILN_2018 GBV_ILN_2027 GBV_ILN_4012 GBV_ILN_4046 GBV_ILN_4082 GBV_ILN_4103 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4302 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4311 GBV_ILN_4319 GBV_ILN_4323 |
container_issue |
3 |
title_short |
Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA |
url |
https://doi.org/10.1007/BF00283328 |
remote_bool |
false |
author2 |
Sinha, A. Krishna Hewitt, David A. |
author2Str |
Sinha, A. Krishna Hewitt, David A. |
ppnlink |
129068721 |
mediatype_str_mv |
n |
isOA_txt |
false |
hochschulschrift_bool |
false |
doi_str |
10.1007/BF00283328 |
up_date |
2024-07-04T01:30:55.732Z |
_version_ |
1803610127847129089 |
fullrecord_marcxml |
<?xml version="1.0" encoding="UTF-8"?><collection xmlns="http://www.loc.gov/MARC21/slim"><record><leader>01000caa a22002652 4500</leader><controlfield tag="001">OLC2070509834</controlfield><controlfield tag="003">DE-627</controlfield><controlfield tag="005">20230402225047.0</controlfield><controlfield tag="007">tu</controlfield><controlfield tag="008">200820s1992 xx ||||| 00| ||eng c</controlfield><datafield tag="024" ind1="7" ind2=" "><subfield code="a">10.1007/BF00283328</subfield><subfield code="2">doi</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(DE-627)OLC2070509834</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(DE-He213)BF00283328-p</subfield></datafield><datafield tag="040" ind1=" " ind2=" "><subfield code="a">DE-627</subfield><subfield code="b">ger</subfield><subfield code="c">DE-627</subfield><subfield code="e">rakwb</subfield></datafield><datafield tag="041" ind1=" " ind2=" "><subfield code="a">eng</subfield></datafield><datafield tag="082" ind1="0" ind2="4"><subfield code="a">550</subfield><subfield code="q">VZ</subfield></datafield><datafield tag="084" ind1=" " ind2=" "><subfield code="a">13</subfield><subfield code="2">ssgn</subfield></datafield><datafield tag="084" ind1=" " ind2=" "><subfield code="a">TE 1000</subfield><subfield code="q">VZ</subfield><subfield code="2">rvk</subfield></datafield><datafield tag="100" ind1="1" ind2=" "><subfield code="a">Wayne, David M.</subfield><subfield code="e">verfasserin</subfield><subfield code="4">aut</subfield></datafield><datafield tag="245" ind1="1" ind2="0"><subfield code="a">Differential response of zircon U−Pb isotopic systematics to metamorphism across a lithologic boundary: an example from the Hope Valley Shear Zone, southeastern Massachusetts, USA</subfield></datafield><datafield tag="264" ind1=" " ind2="1"><subfield code="c">1992</subfield></datafield><datafield tag="336" ind1=" " ind2=" "><subfield code="a">Text</subfield><subfield code="b">txt</subfield><subfield code="2">rdacontent</subfield></datafield><datafield tag="337" ind1=" " ind2=" "><subfield code="a">ohne Hilfsmittel zu benutzen</subfield><subfield code="b">n</subfield><subfield code="2">rdamedia</subfield></datafield><datafield tag="338" ind1=" " ind2=" "><subfield code="a">Band</subfield><subfield code="b">nc</subfield><subfield code="2">rdacarrier</subfield></datafield><datafield tag="500" ind1=" " ind2=" "><subfield code="a">© Springer-Verlag 1992</subfield></datafield><datafield tag="520" ind1=" " ind2=" "><subfield code="a">Abstract A detailed morphological, chemical and isotopic study of zircons from a single outcrop of two mineralogically and chemically distinct units of the late Precambrian Ponaganset gneiss was undertaken to investigate the effects of mylonitization and metamorphism on U-Pb isotopic systematics. Late Paleozoic, amphibolite-grade (approx. 600°C) mylonitization of the Ponaganset gneiss at this locality is associated with movement along the Hope Valley Shear Zone. The response of zircon to metamorphism in each gneiss unit is distinct: zircons in gray augen gneiss are uncorroded and not overgrown, whereas zircons from fluorite-bearing pink granitic gneiss are variably corroded and over 50% bear opaque overgrowths. The zircon overgrowths are chemically distinct from the primary cores, and contain high conentrations of Hf, U, HREE, and Th. Mylonite derived from the gray gneiss contains only a small population of Hf-U-rich metamorphic zircon, but zircons in the pink gneiss-derived mylonite are dominated by the Hf-U-rich metamorphic component. In terms of their U-Pb isotopic systematics, overgrowth-free zircons from both units are markedly discordant (gray, 10–20%, pink, 35%), but overgrown zircons from the pink gneiss are up to 70% discordant. Zircons from the mylonites yield younger Pb−Pb and U−Pb ages than those of the protolith gneisses, and isotopic data from each gneiss + mylonite pair define a linear array on concordia plots. Upper intercept ages of the gray gneiss (621+/−27 Ma) and the pink gneiss (635+/−50 Ma) indicate that the crystallization of both units was coeval, and the lower intercept ages (gray, 270+/−92 Ma; pink, 285+/−26 Ma) fall within the range of other published age estimates for Alleghanian metamorphism in southeastern New England (e.g., Zartman et al. 1988). New growth of zircon suggests that Zr was mobile during metamorphism. The presence of fluorite in the pink gneiss, and a discontinuity in log $$\left( {{{f_{{\text{H}}_{\text{2}} {\text{O}}} } \mathord{\left/{\vphantom {{f_{{\text{H}}_{\text{2}} {\text{O}}} } {f_{{\text{HF}}} }}} \right.\kern-\nulldelimiterspace} {f_{{\text{HF}}} }}} \right)$$values obtained from biotite across the pink gneiss-gray gneiss contact indicates that dissolution and reprecipitation of zircon may be related to local variations in HF fugacity. Zircon dissolution/reprecipitation in the pink gneiss, and the lack of similar features in the contiguous gray gneiss, suggests that the degree of isotopic perturbation of zircon during metamorphism is related to bulk chemistry, fluid chemistry and/or the degree of fluid-rock interaction.</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Zircon</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Granitic Gneiss</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Isotopic Systematic</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Metamorphic Zircon</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Augen Gneiss</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Sinha, A. Krishna</subfield><subfield code="4">aut</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Hewitt, David A.</subfield><subfield code="4">aut</subfield></datafield><datafield tag="773" ind1="0" ind2="8"><subfield code="i">Enthalten in</subfield><subfield code="t">Contributions to mineralogy and petrology</subfield><subfield code="d">Springer-Verlag, 1966</subfield><subfield code="g">109(1992), 3 vom: Jan., Seite 408-420</subfield><subfield code="w">(DE-627)129068721</subfield><subfield code="w">(DE-600)1616-0</subfield><subfield code="w">(DE-576)014400367</subfield><subfield code="x">0010-7999</subfield><subfield code="7">nnns</subfield></datafield><datafield tag="773" ind1="1" ind2="8"><subfield code="g">volume:109</subfield><subfield code="g">year:1992</subfield><subfield code="g">number:3</subfield><subfield code="g">month:01</subfield><subfield code="g">pages:408-420</subfield></datafield><datafield tag="856" ind1="4" ind2="1"><subfield code="u">https://doi.org/10.1007/BF00283328</subfield><subfield code="z">lizenzpflichtig</subfield><subfield code="3">Volltext</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_USEFLAG_A</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">SYSFLAG_A</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_OLC</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">SSG-OLC-GEO</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">SSG-OPC-GGO</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_11</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_21</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_22</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_30</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_31</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_40</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_65</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_70</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_2004</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_2010</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_2015</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_2018</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_2027</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4012</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4046</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4082</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4103</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4112</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4125</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4302</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4305</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4306</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4311</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4319</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ILN_4323</subfield></datafield><datafield tag="936" ind1="r" ind2="v"><subfield code="a">TE 1000</subfield></datafield><datafield tag="951" ind1=" " ind2=" "><subfield code="a">AR</subfield></datafield><datafield tag="952" ind1=" " ind2=" "><subfield code="d">109</subfield><subfield code="j">1992</subfield><subfield code="e">3</subfield><subfield code="c">01</subfield><subfield code="h">408-420</subfield></datafield></record></collection>
|
score |
7.3975124 |