FISCHERPLOTS: An Excel spreadsheet for computing Fischer plots of accommodation change in cyclic carbonate successions in both the time and depth domains

Husinec, Antun; Basch, Danko; Rose, Brett; Read, J. Fred

doi:10.1016/j.cageo.2007.02.004

Cited by 30 publications

(27 citation statements)

References 16 publications

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“…The Fischer plot has been widely used as a graphical method to illustrate long-term accommodation changes by graphing cumulative departures from the mean cycle thickness as a function of time or cycle number (Fischer 1964;Goldhammer et al 1987;Read and Goldhammer 1988;Sadler et al 1993;Husineca et al 2008;Bosence et al 2009). A minimum of 50 cycles is recommended for this data analysis.…”

Section: Cycle Stacking Patterns and Accommodation Changementioning

confidence: 99%

Depositional facies and stratal cyclicity of dolomites in the Lower Qiulitag Group (Upper Cambrian) in northwestern Tarim Basin, NW China

Zhang

Chen

Zhou

et al. 2014

Facies

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and accommodation variations revealed by Fischer plots, six larger-scale third-order depositional sequences (Sq1-Sq6) are recognized. These sequences generally consist of a lower transgressive and an upper regressive systems tract. The transgressive tracts are dominated by thickerthan-average cycles, indicating an overall accommodation increase, whereas the regressive tracts are characterized by thinner-than-average peritidal cycles, indicating an overall accommodation decrease. The sequence boundaries are characterized by transitional zones of stacked thinner-than-average cycles, rather than by a single surface. These sequences can further be grouped into lowerorder sequence sets: the lower and upper sequence sets. The lower sequence set, including Sq1-Sq3, is characterized by peritidal facies-dominated sequences and a progressive decrease in accommodation space, indicating a longer-term fall in sea level. In contrast, the upper sequence set (Sq4-Sq6) is characterized by subtidal facies-dominated sequences and a progressive increase in accommodation space, indicating a longer-term rise in sea level.

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Section: Cycle Stacking Patterns and Accommodation Changementioning

confidence: 99%

Depositional facies and stratal cyclicity of dolomites in the Lower Qiulitag Group (Upper Cambrian) in northwestern Tarim Basin, NW China

Zhang

Chen

Zhou

et al. 2014

Facies

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“…Process Example Algeo and Wilkinson (1988) Fluctuations in sediment production 'Vagaries' in sediment deposition record of eustasy within the Milankovich interval. Such plots have subsequently been extensively used, purporting to depict third-order fluctuations in sea-level (Read & Goldhammer, 1988), oscillations in sea level in subtidal cycles (Osleger & Read, 1991), variations in accommodation space (Bosence et al, 2009;Goldhammer et al, 1993;Husinec, Baschb, Rose, & Read, 2008), variations in filled accommodation space, deviation from expected cycle behaviour (warped into the depth domain; Day, 1997), etc. Criticism of such interpretation has followed apace (Boss & Rasmussen, 1995a, 1995bBurgess & Wright, 2003;Eberli, 2013).…”

Section: Referencementioning

confidence: 99%

Lateral facies variations in the Triassic Dachstein platform: A challenge for cyclostratigraphy

Samankassou

Enos

2019

The Depositional Record

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The Triassic Dachstein platform limestone at Steinernes Meer, Salzburg, Austria, includes 611 m of limestone with 222 peritidal cycles overlain by 273 m of subtidal, non‐cyclic and weakly cyclic limestone. Cycle patterns include both shoaling and deepening upward, symmetrical, truncated, and couplets without a depth vector. Beds are laterally discontinuous, and cycle bounding surfaces are laterally variable in the studied strata. Of 558 subtidal and intertidal beds measured, 121 (21.7%) disappear laterally. An additional 73 beds (13.1%) show significant (>10%) lateral variations in thickness. Mean thickness variation is 49%. Both lateral variations and terminations appear to lack a spatial vector. Disappearances toward the inferred platform interior (west) total 10% of the beds. East, toward the platform margin, 11.6% of the beds disappear. Thickness changes occur in 6.5% of beds in each direction. The lack of lateral continuity of beds precludes a simple allocyclic forcing model and is consistent with a non‐eustatic component to stratification. Erosion of intertidal intervals is the process that can be most readily documented. Non‐uniform rates of production, transport and distribution of sediments, superposed on stratigraphic sequences driven by eustasy, probably also contributed to the complex cycle patterns recorded in the Dachstein. Such composites of autocyclic and extrabasinal factors should not be uncritically interpreted as exclusive records of orbital forcing. Lateral discontinuities and thickness variations would also produce inaccuracies in spectral analysis of thickness patterns, typically conducted in search of ‘Milankovich frequencies’, as well as in construction of Fischer plots to analyse long‐period oscillations in accommodation. Any section subjected to cycle analysis should be examined for lateral changes, to the extent permitted by the exposures, in order to produce the most complete (composite) section possible.

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“…Each SBZ separates a relatively thick succession of metre-scale restricted shallow subtidal cycles that generally thin upward. Upward-thinning cycles in shallow-water facies are generally considered an indicator of decreasing accommodation space (Read & Goldhammer, 1988;Sadler et al, 1993;Husinec et al, 2008) and suggest that the overall (third-order) rate of sea-level rise was decelerating while these cycles were deposited. These subtidal intervals between SBZs are considered most representative of the highstand systems tract (HST), which was deposited as the rate of sea-level rise decelerated, and restricted lagoonal sediments began accumulating in the inner ramp ( Fig.…”

Section: Inner Rampmentioning

confidence: 99%

Discontinuity surfaces and microfacies in a storm‐dominated shallow Epeiric Sea, Devonian Cedar Valley Group, Iowa

Brady

Bowie

2017

The Depositional Record

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Discontinuity surfaces develop in carbonate successions in response to a range of environmental changes and represent an integral part of the stratigraphic record. In Palaeozoic shallow epeiric basins that are typified by extremely slow subsidence and intermittent sedimentation, discontinuity surfaces may represent the majority of the time-rock record. A depositional and sequence-stratigraphic model was developed through microfacies analysis and discontinuity surface characterization using three cores in a proximal to distal transect across the Middle to Upper Devonian Iowa Basin. Twelve microfacies are recognized, spanning supratidal to deep subtidal facies tracts. A total of 105 discontinuity surfaces were documented and classified as either submarine omission surfaces, subaerial exposure surfaces or submarine erosional surfaces. Omission surfaces increase in frequency basinward, indicating increased sediment starvation in the offshore direction. Exposure surfaces increase in frequency shoreward, indicating more frequent subaerial exposure in a shallower setting. Erosional surfaces are dominant in the inner and middle ramp and interpreted as the base of storm beds (tempestites); these surfaces are rare in the outer ramp due to its generally deeper setting below storm wave base. Moreover, discontinuity surfaces exhibit systematic groupings stratigraphically (vertically) across the three localities spanning the Devonian carbonate ramp. Zones of either exposuredominated, erosion-dominated or omission-dominated surfaces were recognized and correlated with their landward or basinward equivalents (along with shifts in major facies belts) and interpreted in a sequence-stratigraphic context. This study highlights the importance of including a detailed characterization of both depositional facies and non-depositional discontinuity surfaces in order to better understand the stratigraphic history of a basin. The framework of analysis provided here is particularly useful for marine carbonate strata deposited in epeiric basins, which are especially common in the Palaeozoic and where nondeposition and erosion occur frequently, but can also be applied to other geological time periods and settings.

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FISCHERPLOTS: An Excel spreadsheet for computing Fischer plots of accommodation change in cyclic carbonate successions in both the time and depth domains

Cited by 30 publications

References 16 publications

Depositional facies and stratal cyclicity of dolomites in the Lower Qiulitag Group (Upper Cambrian) in northwestern Tarim Basin, NW China

Depositional facies and stratal cyclicity of dolomites in the Lower Qiulitag Group (Upper Cambrian) in northwestern Tarim Basin, NW China

Lateral facies variations in the Triassic Dachstein platform: A challenge for cyclostratigraphy

Discontinuity surfaces and microfacies in a storm‐dominated shallow Epeiric Sea, Devonian Cedar Valley Group, Iowa

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