Emmanuel J. Gabet and Daniel P. Miggins

ORIGINAL ARTICLE: 2020, v. 48, no. 10, p. 1023–1027, https://doi.org/10.1130/G47902.1. First published 19 June 2020

ERRATUM PUBLICATION: 2021, v. 49, no. 2, p. 238, https://doi.org/10.1130/G47902E.1. First published 31 December 2020

In the caption of Figure 1, panel D, the longitude (highlighted below) is incorrect. The correct longitude is 120.1058°W.

Figure 1. (A) Study area in the Sierra Nevada (California, USA) with lithology (Ludington et al., 2005). Circles show paleochannel sites with depths of net incision (in meters). Stars show locations of sites with volcanic deposits within canyons. (B) Cross section after Lindgren (1911). The valley (39.508°N, 120.687°W) buried by Cenozoic sediments adjacent to the modern Middle Yuba River canyon illustrates the reorganization of drainage networks after aggradation, as well as minimal net basement incision since the Eocene–early Oligocene. Actual locations of the mining tunnel, shaft, and contact between gravels and andesitic rocks are unknown but are estimated for illustrative purposes. Because the precise elevation of the paleochannel’s bed was not recorded, this site was not used in our analysis. (C) Pre-volcanic gravels (Wagner et al., 1981) near the bed of the South Fork American River demonstrate that the canyon was incised by the Eocene–early Oligocene, filled with deposits, and subsequently re-excavated. (D) Volcanic rocks (6.48 Ma) 70 m above bed of the South Fork American River (38.8019°N, 120.4311°W). (E) Canyon of the North Fork Stanislaus River. Andesitic sandstone of the Relief Peak Formation, which lies underneath 10.41 Ma Table Mountain Latite (Koerner et al., 2009), is draped over the bedrock valley wall (38.2376°N, 120.2933°W). L.—late; E.—early; Mio.—Miocene; Plio.—Pliocene; Fm.—Formation.