The palaeomagnetically viable, long-lived and all-inclusive Rodinia supercontinent reconstruction

Evans, David A.D.

doi:10.1144/sp327.16

Cited by 226 publications

(140 citation statements)

References 244 publications

(339 reference statements)

Supporting

Mentioning

128

Contrasting

Unclassified

Order By: Relevance

“…The Abbottabad Formation, Krol Group and the Doushantou Formation are composed of similar lithofacies (mudstone, sandstone, dolomite, phosphate) and chert nodules. The Neoproterozoic-Cambrian biota record (Krol Group Lesser Himalaya, India and Doushtantuo, Dengying formations, China) suggests that palaeogeographically South China was located near India (Evans, 2009).…”

Section: Comparison With India and South Chinamentioning

confidence: 99%

Signatures of Late Neoproterozoic Gondwana assembly and Maronian glaciation in Lesser Himalaya: a palaeogeographical and stratigraphical approach

Umar¹,

Betts²,

Khan³

et al. 2015

Acta Geologica Polonica

View full text Add to dashboard Cite

Stratigraphical and sedimentological analyses of Late Neoproterozoic successions in Lesser Himalaya are combined herein with palaeogeographical considerations and comparisons with equivalent successions in India and South China. The succession starts with the Hazara Formation, which contains complete and incomplete Bouma sequences suggesting its deposition in deep marine turbidite settings. The overlying Tanawal Formation, rich in massive sandstone, shale and siltstone, was deposited in shallow marine conditions, as indicated by the presence of parallel lamination, large scale tabular, trough cross-and hummocky cross-stratifications. The Tanawal Formation facies shift laterally from proximal (south-southeast) to distal (north-northwest). The glaciogenic Tanaki Boulder Bed, overlying the Tanawal Formation, was deposited during the Maronian glaciation. It is equivalent to the Blaini Formation of India, and to the Sinian diamictites of South China. The Abbottabad Formation of Cambrian age overlies the Tanaki Boulder Bed, and is composed of dolomite, chert nodules and phosphate-rich packages; similar successions are documented in India and South China at the same stratigraphical interval. The similarities of the Neoproterozoic successions of Lesser Himalaya (both in Pakistan and India) and South China suggests their possible proximity during the break-up of Rodinia and the assembly of the Gondwana Supercontinent.

show abstract

Section: Comparison With India and South Chinamentioning

confidence: 99%

Signatures of Late Neoproterozoic Gondwana assembly and Maronian glaciation in Lesser Himalaya: a palaeogeographical and stratigraphical approach

Umar¹,

Betts²,

Khan³

et al. 2015

Acta Geologica Polonica

View full text Add to dashboard Cite

show abstract

“…One possibility is an increased flux of light hydrothermal source-derived Si into the oceans associated with Neoproterozoic breakup of Rodinia (e.g. Dalziel, 1997;Pisarevsky et al, 2003;Evans, 2009). However, this does not explain why values begin to decline as early as 1.2 Ga.…”

Section: Toward Understanding the Temporal Variation In The Si Isotopmentioning

confidence: 99%

Si isotope variability in Proterozoic cherts

Chakrabarti

Knoll

Jacobsen

et al. 2012

Geochimica et Cosmochimica Acta

View full text Add to dashboard Cite

We report Si-isotopic compositions of 75 sedimentologically and petrographically characterized chert samples with ages ranging from $2600 to 750 Ma using multi-collector inductively coupled plasma mass spectrometry. d 30 Si values of the cherts analyzed in this study show a $7& range, from À4.29 to +2.85. This variability can be explained in part by (1) simple mixing of silica derived from continental (higher d 30 Si) and hydrothermal (lower d 30 Si) sources, (2) multiple mechanisms of silica precipitation and (3) Rayleigh-type fractionations within pore waters of individual basins.We observe $3& variation in peritidal cherts from a single Neoproterozoic sedimentary basin (Spitsbergen). This variation can be explained by Rayleigh-type fractionation during precipitation from silica-saturated porewaters. In some samples, postdissolution and reprecipitation of silica could have added to this effect. Our data also indicate that peritidal cherts are enriched in the heavier isotopes of Si whereas basinal cherts associated with banded iron formations (BIF) show lower d 30 Si. This difference could partly be due to Si being derived from hydrothermal sources in BIFs. We postulate that the difference in d 30 Si between non-BIF and BIF cherts is consistent with the contrasting genesis of these deposits. Low d 30 Si in BIF is consistent with laboratory experiments showing that silica adsorbed onto Fe-hydroxide particles preferentially incorporates lighter Si isotopes.Despite large intrabasinal variation and environmental differences, the data show a clear pattern of secular variation. Low d 30 Si in Archean cherts is consistent with a dominantly hydrothermal source of silica to the oceans at that time. The monotonically increasing d 30 Si from 3.8 to 1.5 Ga appears to reflect a general increase in continental versus hydrothermal sources of Si in seawater, as well as the preferential removal of lighter Si isotopes during silica precipitation in iron-associated cherts from silica-saturated seawater. The highest d 30 Si values are observed in 1.5 Ga peritidal cherts; in part, these enriched values could reflect increasing sequestration of light silica during soil-forming processes, thus, delivering relatively heavy dissolved silica to the oceans from continental sources. The causes behind the reversal in trend towards lower d 30 Si in cherts younger than 1.5 Ga old are less clear. Cherts deposited 1800-1900 Ma are especially low d 30 Si, a possible indication of transiently strong hydrothermal input at this time.

show abstract

“…The assembly of Amazonia and Laurentia has been related to both oblique or orthogonal collision, dependent in part on the relative positions of these cratons before and after collision (e.g., Dalziel, 1997;Evans, 2013;Johansson, 2009;Park, 1992;Pisarevsky et al, 2014;Pisarevsky et al, 2003;Tohver et al, 2004b). Some models have questioned whether Amazonia was the colliding element or even if there was collisional orogenesis (Dalziel et al, 2000;Evans, 2009;Santos et al, 2008).…”

Section: Introductionmentioning

confidence: 99%